"VG 602 with SIRA-series electronics at Rice University, a Finnigan 252 with Kiel device at Stanford University, a VG-SIRA with automated carbonate preparation device, and a Micromass Optima with automated carbonate preparation device, the latter two at the University of Colorado, Boulder (INSTAAR)."

; climateInterpretation_seasonality changed - was originally -12 -11 1 2 3 4 5 6 7 8 9 10; archiveType changed - was originally Coral (CO)

The coral 18O record from this site reflects primarily SST; a linear regression of coral 18O versus SST yields a slope of 0.24 per mil (a€°) 18O per 1A°C, explaining 47% of the SST variance (20).

additional variability in coral 18O may arise from vari- ations in the 18O of seawater due to precip- itation, evaporation, or runoff, but at this site these changes are likely to be secondary be- cause local rainfall 18O is not strongly de- pleted from average seawater (21) and salin- ity gradients are small (22). Rainfall and SST influences are likely to be additive in terms of annual effect on coral 18O because warmer years tend to be wetter at this site.

Cole, J. E.: Tropical Pacific Forcing of Decadal SST Variability in the Western Indian Ocean over the Past Two Centuries, Science, 287(5453), 617–619, doi:10.1126/science.287.5453.617, 2000.

Tropical Pacific Forcing of Decadal SST Variability in the Western Indian Ocean over the Past Two Centuries

Auer, Gerald , Piller, Werner E. , Reuter, Markus , Harzhauser, Mathias

Auer, G., Piller, W. E., Reuter, M. and Harzhauser, M.: Correlating carbon and oxygen isotope events in early to middle Miocene shallow marine carbonates in the Mediterranean region using orbitally tuned chemostratigraphy and lithostratigraphy, Paleoceanography, 30(4), 332–352, doi:10.1002/2014pa002716, 2015.

X-radiographs were assessed from the skeleton slices to expose density banding. Chronologies were achieved by counting the well-developed density couplets. BDA 210 revealed continuous growth between 1825 and 1993, whereas BDA 215 and BDA 221 contain hiatuses. The bases of the colonies, which were separated from the upper living parts by algal growth, were 14C dated by AMS in the Leibnitz Laboratory in Kiel. Precision of Dating came to  30 years. The stratigraphy obtained from 14C dating was confirmed by the strong correspondence of the present proxy time series with a continuous 800-year coral skeletal chronology from Bermuda, presented by Patzold et al. (1998; see Fig. 3c).

Finnigan MAT 251 micro-mass spectrometer with an automatic carbonate preparation device (Kiel Device).

; climateInterpretation_seasonality changed - was originally -12 -11 -10 -9 -8 1 2 3 4 5 6 7; archiveType changed - was originally Coral (CO)

d18O (3 yr mean) calibration to SST (3 yr mean). SST is inferred from air temperature

The availability of instrumental climate data allow the comparison with the coral signal and supports the interpretation of reconstructed past temperature anomalies. The use of air temperatures is justified by the strong long-term correspondence between Bermuda SST (COADS) of a 2 latitude by 2 longitude area and Bermuda air temperature during a 40-year period.

X-radiographs were assessed from the skeleton slices to expose density banding. Chronologies were achieved by counting the well-developed density couplets. BDA 210 revealed continuous growth between 1825 and 1993, whereas BDA 215 and BDA 221 contain hiatuses. The bases of the colonies, which were separated from the upper living parts by algal growth, were 14C dated by AMS in the Leibnitz Laboratory in Kiel. Precision of Dating came to  30 years. The stratigraphy obtained from 14C dating was confirmed by the strong correspondence of the present proxy time series with a continuous 800-year coral skeletal chronology from Bermuda, presented by P�tzold et al. (1998; see Fig. 3c).

the salinity effect on the isotopic pool of the ambient seawater is considered a negligible background signal and variations in coral d18O can be attributed to be primarily driven by changes in SST.

empirical d18O-T sensitivity is approximately 4 times abiogenic experiments and many other biogenic carbonates. Consider excluding.

X-radiographs were assessed from the skeleton slices to expose density banding. Chronologies were achieved by counting the well-developed density couplets. BDA 210 revealed continuous growth between 1825 and 1993, whereas BDA 215 and BDA 221 contain hiatuses. The bases of the colonies, which were separated from the upper living parts by algal growth, were 14C dated by AMS in the Leibnitz Laboratory in Kiel. Precision of Dating came to  30 years. The stratigraphy obtained from 14C dating was confirmed by the strong correspondence of the present proxy time series with a continuous 800-year coral skeletal chronology from Bermuda, presented by Pi¿½tzold et al. (1998; see Fig. 3c).

Draschba, S., Paetzold, J. and Wefer, G.: North Atlantic climate variability since AD 1350 recorded in δ 18 O and skeletal density of Bermuda corals, International Journal of Earth Sciences, 88(4), 733–741, doi:10.1007/s005310050301, 2000.

North Atlantic climate variability since AD 1350 recorded in ? 18 O and skeletal density of Bermuda corals

Finnigan MAT 251 mass spectrometer coupled to an automated carbonate device

; climateInterpretation_seasonality changed - was originally bimonthly; archiveType changed - was originally Coral (CO)

The coral chronology is constructed by setting the maximum d18O value in  a given year equal to mid-February (consistent with the climatological  minimum in sea surface temperature) and assuming a constant coral growth  rate between February of every year. Therefore we interpolated linearly  between these fixed points for further age assignments. The resulting values  were interpolated linearly to six equally spaced values per year, providing a  bimonthly resolution.

"The coral chronology is constructed by setting the maximum d18O value in  a given year equal to mid-February (consistent with the climatological  minimum in sea surface temperature) and assuming a constant coral growth  rate between February of every year. Therefore we interpolated linearly  between these fixed points for further age assignments. The resulting values  were interpolated linearly to six equally spaced values per year, providing a  bimonthly resolution."

Felis, T., J. Patzold, Y. Loya, M. Fine, A.H. Nawar, and G. Wefer

Felis, T., Paetzold, J., Loya, Y., Fine, M., Nawar, A. H. and Wefer, G.: A coral oxygen isotope record from the northern Red Sea documenting NAO, ENSO, and North Pacific teleconnections on Middle East climate variability since the year 1750, Paleoceanography, 15(6), 679–694, doi:10.1029/1999pa000477, 2000.

A coral oxygen isotope record from the northern Red Sea documenting NAO, ENSO, and North Pacific teleconnections on Middle East climate variability since the year 1750

Tierney, Jessica E. , Abram, Nerilie J. , Anchukaitis, Kevin J. , Evans, Michael N. , Giry, Cyril , Kilbourne, K. Halimeda , Saenger, Casey P. , Wu, Henry C. , Zinke, Jens

Tierney, J. E., Abram, N. J., Anchukaitis, K. J., Evans, M. N., Giry, C., Kilbourne, K. H., Saenger, C. P., Wu, H. C. and Zinke, J.: Tropical sea surface temperatures for the past four centuries reconstructed from coral archives, Paleoceanography, 30(3), 226–252, doi:10.1002/2014pa002717, 2015.

0.07 per mil of internal laboratory standard (Solnhofen limestone)

The age model in the data set is based on the density banding of the skeleton and the seasonality in d18O, whithin each year the highest (least depleted) d18O value was tied to mid-September, which is the coldest month on average.

Kuhnert, H., Paetzold, J., Wyrwoll, K.-H. and Wefer, G.: Monitoring climate variability over the past 116 years in coral oxygen isotopes from Ningaloo Reef, Western Australia, International Journal of Earth Sciences, 88(4), 725–732, doi:10.1007/s005310050300, 2000.

; climateInterpretation_seasonality changed  was originally bimonthly; archiveType changed  was originally Coral (CO); archiveType changed  was originally Coral (CO)

; archiveType changed  was originally Coral (CO); archiveType changed  was originally Coral (CO)

Urban, F. E., Cole, J. E. and Overpeck, J. T.: Influence of mean climate change on climate variability from a 155-year tropical Pacific coral record, Nature, 407(6807), 989–993, doi:10.1038/35039597, 2000.

"isotope ratio mass spectrometer with automatic carbonate preparation system"

X-ray diffraction, petrographic thin-section, and scanning electron microscope (SEM) analyses

; climateInterpretation_seasonality changed - was originally seasonal; archiveType changed - was originally Coral (CO); archiveType changed - was originally Coral (CO)

The chronologies were subsequently developed on the basis of seasonality in skeletal d18O and d13C, supported by examination of annual skeletal density and fluorescent banding.

This tracer responds to water temperature through a temperature- dependent fractionation [;?0.2? d18O/i¿½C (19, 20)], as well as to changes in rainfall, due to the influence of isotopically light (more negative d18O) rainfall on surface ocean composition. Because SST and rainfall are intimately linked in tropical areas of strong convective rainfall such as the western equatorial Pacific, the two factors combine to produce an enhanced climatic signal in coral skeletal d18O.

This tracer responds to water temperature through a temperature- dependent fractionation [~ -0.2 permil d18O/degree C (19, 20)], as well as to changes in rainfall, due to the influence of isotopically light (more negative d18O) rainfall on surface ocean composition. Because SST and rainfall are intimately linked in tropical areas of strong convective rainfall such as the western equatorial Pacific, the two factors combine to produce an enhanced climatic signal in coral skeletal d18O.

Tudhope, A.W.; Chilcott, C.P.; McCulloch, M.T.; Cook, E.R.; Chappell, J.; Ellam, R.M.; Lea, D.W.; Lough, J.M.; Shimmield, G.B.

Tudhope, A. W.: Variability in the El Nino-Southern Oscillation Through a Glacial-Interglacial Cycle, Science, 291(5508), 1511–1517, doi:10.1126/science.1057969, 2001.

Variability in the El Nino-Southern Oscillation Through a Glacial-Interglacial Cycle

Note: floating fossil coral sections have greater uncertainty in absolute temperature for palaeoclimate reconstructions (NJA)

The d18O of the samples was measured at the Fachbereich Geowissenschaften, Universita�t Bremen, on a Finnigan MAT 251 mass spectrometer, calibrated against the NBS-19 standard. Data are corrected for the usual isobaric interferences and are reported in x versus V-PDB.

X-ray diffraction (XRD) and measurements of Mg/Ca. Additional investigations were carried out on thin sections ratios.

; climateInterpretation_seasonality changed - was originally monthly; archiveType changed - was originally Coral (CO)

The top and base of the core section were U/Th-dated (measured at the Institut fur Umweltphysik, Heidelberg, Germany), with a precision of i¿½15 yr. The midpoint of the top dated sample is 14 density band couplets above the profile for geochemical measurements, and the midpoint of the bottom dated sample is seven band couplets below the profile (Fig. 2). In other words, the age model within the chronology is based on the annual banding. According to band couplet counts and the number of annual cycles in the d18O, the U/Th-dated sections differ in age by 104 yr, while the difference is 130 yr according to their radiometric dates (base: 1499, top: 1629 AD). To remove the surplus of 26 yr we adjusted the radiometric ages by adding 13 yr to the bottom and subtracting 13 yr from the top sample age. Therefore, individual years in our record are correct with respect to their positions within the time series, but they do not necessarily match calendar years. Years in the isotopic record are defined by cyclic variations in d18O, which are assumed to be annual, with each cycle spanning ca. 2.5-4 mm core length. Subannual dating is based on the annual d18O cycles, where the most positive d18O value in each cycle is assigned to the coldest average month, which, for Bermuda, is March. This introduces a non-cumulative error of approximately i¿½1 month. The ages of other sampling points were linearly interpolated according to their spatial distances along the sampling profile.

The mean annual cycles of d18O and the Sr/Ca ratios suggest temperature amplitudes of only 40-50% of the 8.4i¿½C in recent temperatures. The results indicated by the proxies appear unrealistically low, and we believe that the data sets do not capture the full annual amplitude, despite a sampling resolution of more than 12 samples per annual skeletal growth increment.

This coral was not directly calibrated since the top is not modern. They used other calibrations (Porites), and not from Diploria labyrinthiformis. Using more recent Goodkin calibration would be applicable to this coral. "we used calibrations from the Atlantic and Pacific Oceans. For estimating temperatures from coral skeletal d18O we used the gradient of the temperature to N18O equation of Leder et al. (1996) obtained from Florida corals (4.52i¿½C per mil in d18O).

The top and base of the core section were U/Th-dated (measured at the Institut fur Umweltphysik, Heidelberg, Germany), with a precision of �15 yr. The midpoint of the top dated sample is 14 density band couplets above the profile for geochemical measurements, and the midpoint of the bottom dated sample is seven band couplets below the profile (Fig. 2). In other words, the age model within the chronology is based on the annual banding. According to band couplet counts and the number of annual cycles in the d18O, the U/Th-dated sections differ in age by 104 yr, while the difference is 130 yr according to their radiometric dates (base: 1499, top: 1629 AD). To remove the surplus of 26 yr we adjusted the radiometric ages by adding 13 yr to the bottom and subtracting 13 yr from the top sample age. Therefore, individual years in our record are correct with respect to their positions within the time series, but they do not necessarily match calendar years. Years in the isotopic record are defined by cyclic variations in d18O, which are assumed to be annual, with each cycle spanning ca. 2.5-4 mm core length. Subannual dating is based on the annual d18O cycles, where the most positive d18O value in each cycle is assigned to the coldest average month, which, for Bermuda, is March. This introduces a non-cumulative error of approximately �1 month. The ages of other sampling points were linearly interpolated according to their spatial distances along the sampling profile.

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally monthly; paleoData_variableName changed - was originally Sr_Ca; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Coral (CO)

Kuhnert, Henning , Patzold, Jorgen , Schnetger, Bernhard , Wefer, Gerold

Kuhnert, H., Paetzold, J., Schnetger, B. and Wefer, G.: Sea-surface temperature variability in the 16th century at Bermuda inferred from coral records, Palaeogeography, Palaeoclimatology, Palaeoecology, 179(3-4), 159–171, doi:10.1016/s0031-0182(01)00410-2, 2002.

Sea-surface temperature variability in the 16th century at Bermuda inferred from coral records

Chronological assignments for the record were generally straightforward, because of the clear seasonal cycle in d18O and the especially clear expression of annual growth bands. The seasonal extremes were an- chored to April and September of each year

in the Indonesian coral records, coral d18O is more heavily infuenced by rainfall variability

Charles, C. D., Cobb, K., Moore, M. D. and Fairbanks, R. G.: Monsoon–tropical ocean interaction in a network of coral records spanning the 20th century, Marine Geology, 201(1-3), 207–222, doi:10.1016/s0025-3227(03)00217-2, 2003.

Monsoon?tropical ocean interaction in a network of coral records spanning the 20th century

anchoring seasonal maxima and minima of the d18O depth series to March and October of each year. Crosschecks on the age assignments were available through examination of the annual growth bands and the strong semi-annual carbon isotope signal

The annual variability of the Bunaken coral d18O refects the seasonal cycle of both salinity and temperature in the surrounding seawater

The annual variability of the Bunaken coral d18O refects the seasonal cycle of both salinity and temperature in the surrounding seawater. The characteristics and correlations of the Bunaken Island coral d18O record strongly suggestthat it monitors the air-sea interaction associatedwith Southeast Asian summer monsoon.

The annual variability of the Bunaken coral d18O refects the seasonal cycle of both salinity and temperature in the surrounding seawater: "in the Indonesian coral records, coral d18O is more heavily infuenced by rainfall variability." The characteristics and correlations of the Bunaken Island coral d18O record strongly suggestthat it monitors the air-sea interaction associatedwith Southeast Asian summer monsoon.

Finnigan MAT 252 stable isotope mass spectrometer equipped with a Fairbanks carbonate preparation device

; climateInterpretation_seasonality changed - was originally subannual; archiveType changed - was originally Coral (CO); archiveType changed - was originally Coral (CO)

0.12 permil, std deviation of offsets between overlapping colonies

d18O tied to warmest month (Aug) and coolest month (Feb), linear interpolation used to obtain dates between

ENSO variability is the dominant source of d18O variability in the Palmyra fossil-coral d18O records

; archiveType changed - was originally Coral (CO); archiveType changed - was originally Coral (CO)

NB9  SB8  SB13  SB3  SB6  SB5  CH5  CH9  SB7  SB17  NB12  spl14  spl17

El Nino/Southern Oscillation and tropical Pacific climate during the last millennium

Cobb, K. M., Charles, C. D., Cheng, H. and Edwards, R. L.: El Nino/Southern Oscillation and tropical Pacific climate during the last millennium, Nature, 424(6946), 271–276, doi:10.1038/nature01779, 2003.

Cobb, Kim M. , Charles, Christopher D. , Cheng, Hai , Kastner, Miriam , Edwards, R.Lawrence

Wieczorek, M. A. and Zuber, M. T.: The composition and origin of the lunar crust: Constraints from central peaks and crustal thickness modeling, Geophysical Research Letters, 28(21), 4023–4026, doi:10.1029/2001gl012918, 2001.

Diploastrea heliopora specie; test regarding Diploasrea sampling strategy over the first 50 mm

Multiprep carbonate inlet system and the resulting CO  gas was analyzed with a Micromass Optima triple-collecting mass spectro- meter

The d18O  were tuned to the SST record by assigning the lowest (highest) d18O values of each year to the highest (lowest) SST. Age assignments were then linearly interpolated between these two annual anchor points using the Arand software package (P. Howell, personal commu- nication, 2002). A continuous monthly SST data set is available only as far back as 1970, so for age assignments before 1970 the lowest (highest) d18O and Sr/Ca values were assigned to March (August), March and August being the average times of highest and lowest SST, respectively, between 1970 and 1997

Bagnato, S., B.K. Linsley, S.S. Howe, G.M. Wellington, J. Salinger

Bagnato, S., Linsley, B. K., Howe, S. S., Wellington, G. M. and Salinger, J.: Evaluating the use of the massive coralDiploastrea helioporafor paleoclimate reconstruction, Paleoceanography, 19(1), n/a–n/a, doi:10.1029/2003pa000935, 2004.

automated carbonate device (Micromass Multiprep) attached to a mass spectrometer (Micromass Optima).

Age determination was carried out by matching the oxygen isotope record mainly reflects the seasonal SST cycle of 1a€“2 C at this location and indicates that the core provides a continuous record from 1957 to 1999.  Positive anomalies agreed with the timing of known El Nino events (when SSTs are cooler in this region)

oxygen isotope record mainly reflects the seasonal SST cycle of 1a€“2 C at this location

Age determination was carried out by matching the oxygen isotope record mainly reflects the seasonal SST cycle of 1–2 C at this location and indicates that the core provides a continuous record from 1957 to 1999.  Positive anomalies agreed with the timing of known El Nino events (when SSTs are cooler in this region)

Need to aquire data from authors. NCDC only has data with respect to depth

Inoue, M., A. Suzuki, M. Nohara, H. Kan, A. Edward, and H. Kawahata.

Inoue, M., Suzuki, A., Nohara, M., Kan, H., Edward, A. and Kawahata, H.: Coral skeletal tin and copper concentrations at Pohnpei, Micronesia: possible index for marine pollution by toxic anti-biofouling paints, Environmental Pollution, 129(3), 399–407, doi:10.1016/j.envpol.2003.11.009, 2004.

Kilbourne et al., 2004, and Kilbourne et al., 2004, (10.1029/2004PA001033, 10.1029/2003PA000944) both report on the same data.

University of South Florida, College of Marine Science using a ThermoFinnigan Delta Plus XL dual-inlet mass spectrometer with an attached Kiel carbonate preparation device.

; climateInterpretation_seasonality changed - was originally subannual

Time was assigned to the Sr/Ca and coral d18O depth series by matching Sr/Ca minima with SST maxima (and vice versa), using AnalySeries software [Paillard et al., 1996].

This paper examines three methods of determining d18Osw and salinity from coral d18O and Sr/Ca. The give similar resutls and are very dependant on SSS data source for calibration.

In this study we use the G&D-SSS data [Gouriou and Delcroix, 2002] rather than a hindcast model SSS such as that available from NCEP in 1 by 1 degree grid boxes (Behringer et al. [1998]; hereafter referred to as NCEP-SSS) because the former consists of actual salinity measurements.total salinity range over a 20-year period is >3 times larger in G&DSSS than in NCEP-SSS model output (cf., 1.91 versus 0.51). Such large differences in the SSS between these two data sets imply that the SSS data set used for calibrating a measured coral proxy can strongly affect the outcome of the calibration. Three different methods for reconstructing SSSrelated dw variations are compared in this paper.

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally subannual; paleoData_variableName changed - was originally Sr_Ca

Kilbourne 2004 has two paper that report on the same modern data

Malo Channel, Espiritu Santo Island - Stable Isotope and Elemental Data

Kilbourne, K. H., Quinn, T. M., Taylor, F. W., Delcroix, T. and Gouriou, Y.: El Nino-Southern Oscillation-related salinity variations recorded in the skeletal geochemistry of aPoritescoral from Espiritu Santo, Vanuatu, Paleoceanography, 19(4), n/a–n/a, doi:10.1029/2004pa001033, 2004.

El Nino-Southern Oscillation-related salinity variations recorded in the skeletal geochemistry of a Porites coral from Espiritu Santo, Vanuatu

used in Tierney et al, as a composite with HR_156; the original records are provided here rather than composites

0.04 per mil for d18O based on analyses of 657 (13.5%) rep- licate samples.

tied the annual minima in d18O to February (on average the warmest month) and maximum  d18O to August/September (on average the coolest months). And comparing the d18O  records to Nino3.4 (central equatorial Pacific region bounded by 5i¿½S?5i¿½N and 120i¿½?170i¿½W) SST anomaly (SSTa)

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally monthly; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Coral (CO)

Linsley B. K., G. M. Wellington, D. P. Schrag, L. Ren, M. J. Salinger, A. W. Tudhope

Wellington, G. M., Schrag, D. P., Ren, L., Salinger, M. J., Tudhope, A. W. and Linsley, B. K.: Geochemical evidence from corals for changes in the amplitude and spatial pattern of South Pacific interdecadal climate variability over the last 300 years, Climate Dynamics, 22(1), 1–11, doi:10.1007/s00382-003-0364-y, 2004.

Tracking the extent of the South Pacific Convergence Zone since the early 1600s

Combined influenced of SST and SSS on the d18O signal - with SST leading seasoanl variability and SSS interannual and decadal varaibility (Linsley et al., 2006)

Micromass Optima gas source mass spectrometer with an individual acid reaction vessel system

Close inspection of each X-ray and reproducibility between 2 cores

Linsley, B.K., A. Kaplan, Y. Gouriou, J. Salinger, P.B. deMenocal, G.M. Wellington, and S.S. Howe. 2006. Tracking the extent of the South Pacific Convergence Zone since the early 1600s. Geochemistry, Geophysics, Geosystems, 7, Q05003. doi: 10.1029/2005GC001115

Finnigan MAT251 mass spectrometer with automated carbonate (Kiel) prep device

Interannual variability in the MS01 coral d18O for 1910a€“ 1997 is clearly dominated by changes in d18Ow because SSTs reconstructed from the coral d18O span 5C [Gagan et al., 1998], while the GOSTA SST range is only 1C (Figure 1). Comparison of local SSTs and rainfall with the coral d18O record shows that d18O increases when SST and rainfall decrease during El NinEœo events

Interannual variability in the MS01 coral d18O for 1910-1997 is clearly dominated by changes in d18Ow because SSTs reconstructed from the coral d18O span 5C [Gagan et al., 1998], while the GOSTA SST range is only 1C (Figure 1). Comparison of local SSTs and rainfall with the coral d18O record shows that d18O increases when SST and rainfall decrease during El Nino events.

McGregor, H. V. and Gagan, M. K.: Western Pacific coral δ18O records of anomalous Holocene variability in the El Nino-Southern Oscillation, Geophysical Research Letters, 31(11), n/a–n/a, doi:10.1029/2004gl019972, 2004.

automated carbonate preparation device (Kiel device) + Finnigan Mat 252 mass spectrometer

A simple chronology based on these density bands in both corals temporally aligned anomalous 18O-depleted years precisely in the same years (e.g., 1972?1973, 1982? 1983). During these years, there were noted positive precipitation and/or SST anomalies. We then assigned February 15 to the most negative isotopic values. This is, on average, the wettest month. We then interpolated linearly between the anchor points to obtain bimonthly records of coral y18O.

We find strong correlations between coral y18O, precipitation, and OLR, but also between coral y18O and SST

Core piM correlates more strongly with precipitation and OLR than COI-5  (Table 1). Note that years of high rainfall coincide with years of large negative coral y18O anomalies in the wet season (and high amplitudes of the annual cycle,

However, over the entire time interval compared, maximum variations of mean summer SST are 1jC, which would account for approximately 0.20x in coral y18O (Juillet- Leclerc and Schmidt, 2001). Over the same period, mean summer coral y18O varies by as much as 0.7x (piM) and 0.4x (COI-5) (Fig. 4); i.e., the maximum SST contribution to the coral isotopic signal is 29% (piM) and 50% (COI-5).

However, over the entire time interval compared, maximum variations of mean summer SST are 1jC, which would account for approximately 0.20x in coral y18O (Juillet- Leclerc and Schmidt, 2001). Over the same period, mean summer coral y18O varies by as much as 0.7x (piM) and 0.4x (COI-5) (Fig. 4); i.e., the maximum SST contribution to the coral isotopic signal is 29% (piM) and 50% (COI-5)

Core GIM correlates more strongly with precipitation and OLR than COI-5 (Table 1). Note that years of high rainfall coincide with years of large negative coral y18O anomalies in the wet season (and high amplitudes of the annual cycle,

Need to aquire data for core GIM from authors, NCDC only has core COI5

Pfeiffer, M., Dullo, W.-C. and Eisenhauer, A.: Variability of the Intertropical Convergence Zone recorded in coral isotopic records from the central indian Ocean (Chagos Archipelago), Quaternary Research, 61(3), 245–255, doi:10.1016/j.yqres.2004.02.009, 2004.

d18Osw is probably the primary control on d18O of the coral at this site; authors found positive relation btwn 18O and temperature, opposite the expected

"Online carbonate preparation line (Carbo-Kiel-single sample acid bath)  connected to a Finnigan Mat 252 masspectrometer"

0.06 per mil of internal laboratory standard (NBS19) of 267 samples

A first chronology was developed based on the density bands evident in the X-rays, which are presumed to represent one year of growth (Figure 4). The age model was then refined using the strong annual cycle in coral d18O (Figures 5 and 6). The heaviest isotopic value in any given year was assigned to 1 September, which is, on average, the coldest month. We then interpolated linearly between these anchor points into 12 equidistant points per year for the monthly, and 6 points per year for the bimonthly resolved series

Pfeiffer, M., Timm, O., Dullo, W.-C. and Podlech, S.: Oceanic forcing of interannual and multidecadal climate variability in the southwestern Indian Ocean: Evidence from a 160 year coral isotopic record (La Reunion, 55°E, 21°S), Paleoceanography, 19(4), n/a–n/a, doi:10.1029/2003pa000964, 2004.

We use the pronounced seasonal cycle in d18O and Sr/Ca to develop the final chronology of the coral core and assigned the highest d18O and Sr/Ca values to august 15 of each year, which is on average the coldest month. [...] The d18O and Sr/Ca time series were interpolated linearly into 6 and 12 equi- distant points for any given year between these anchor points using the Analyseries software,.083 to 0.167 yrs,chronological,months,on a seasonal scale coral d18O  and Sr/Ca at this location primarily reflects SST variability (Fig. 5; Table 1). "

A correlation of seasonal mean rainfall anomalies derived from the NCEP/NCAR reanalysis data set (1948-1995; averaged over 3545E, 20-30S; http://www. cdc.noaa.gov/cdc/data.ncep.reanalysis.derived.html) with coral d18O shows a clear relationship during austral summer (NDJF) significant above the 90% level (Fig. 6). This also holds for a correlation with South African summer rainfall averaged over 25-30E and 15-25S (significant N95%) (Fig. 6). Thus, summer coral d18O is also related to changes in the regional hydrologic (P/E) balance

We use the pronounced seasonal cycle in d18O and Sr/Ca to develop the final chronology of the coral core and assigned the highest d18O and Sr/Ca values to august 15 of each year, which is on average the coldest month. [...] The d18O and Sr/Ca time series were interpolated linearly into 6 and 12 equi- distant points for any given year between these anchor points using the Analyseries software|.083 to 0.167 yrs|chronological|months|on a seasonal scale coral d18O  and Sr/Ca at this location primarily reflects SST variability (Fig. 5; Table 1). "

Ifaty reef and Tulear Reef mean annual oxygen isotope records, 1660-1994

Zinke, J., Dullo, W.-C., Heiss, G. A. and Eisenhauer, A.: ENSO and Indian Ocean subtropical dipole variability is recorded in a coral record off southwest Madagascar for the period 1659 to 1995, Earth and Planetary Science Letters, 228(1-2), 177–194, doi:10.1016/j.epsl.2004.09.028, 2004.

ENSO and Indian Ocean subtropical dipole variability is recorded in a coral record off southwest Madagascar for the period 1659 to 1995

automated carbonate device (Kiel III, Finnigan MAT) attached to a Finnigan MAT Delta S mass spectrometer

SEM and X-ray diffraction on skeletal fragments at intervals of ~10cm

maximum and minimum ?18Ocoral values in a given year were assigned to February and August; linear interpolation between these fixed tie points

These results suggest that changes in Guam ?18Ocoral are mainly influenced by SST and SSS variations on seasonal and interannual timescales.

The d18Ocoral anomaly is significantly correlated with SST anomaly (SSTA) (r = -0.69 and p < 0.01) and SSS anomaly (SSSA) (r = 0.49 and p < 0.01). These results suggest that changes in Guam d18Ocoral are mainly influenced by SST and SSS variations on seasonal and interannual timescales.

an older version of this record can be found at: https://www.ncdc.noaa.gov/cdo/f?p=519:1:::::P1_study_id:1898

Asami, R.; Yamada, T.; Iryu, Y.; Quinn, T.M.; Meyer, C.P.; Paulay, G.

Asami, R.: Interannual and decadal variability of the western Pacific sea surface condition for the years 1787–2000: Reconstruction based on stable isotope record from a Guam coral, Journal of Geophysical Research, 110(C5), doi:10.1029/2004jc002555, 2005.

Interannual and decadal variability of the western Pacific sea surface condition for the years 1787?2000: Reconstruction based on stable isotope record from a Guam coral

Composite of CO04BAFI00A and the rest of the 4F1 record - 2 diploastra records

; climateInterpretation_seasonality changed - was originally annual; archiveType changed - was originally Coral (CO)

"The d18O  were tuned to the SST record by assigning the lowest (highest) d18O values of each year to the highest (lowest) SST. Age assignments were then linearly interpolated between these two annual anchor points using the Arand software package (P. Howell, personal commu- nication, 2002). A continuous monthly SST data set is available only as far back as 1970, so for age assignments before 1970 the lowest (highest) d18O and Sr/Ca values were assigned to March (August), March and August being the average times of highest and lowest SST, respectively, between 1970 and 1997"

Bagnato, S., Linsley, B. K., Howe, S. S., Wellington, G. M. and Salinger, J.: Coral oxygen isotope records of interdecadal climate variations in the South Pacific Convergence Zone region, Geochemistry, Geophysics, Geosystems, 6(6), doi:10.1029/2004gc000879, 2005.

Coral oxygen isotope records of interdecadal climate variations in the South Pacific Convergence Zone region

 METHOD: ICP-MS, Inductively coupled plasma - mass spectrometry? From Pangaea metadata, not described in paper.

Missing "isotope interpretation1,2,3" fields. -BK DMT: Resolved 1/14

The age model for the record is based on the seasonal banding pattern, as seen in the X-radiographs, and the annual cycles in the skeletal geochemistry. To be consistent with earlier work [Kuhnert et al., 2002], we used the cyclicity in d18O (which is not further discussed) rather than that in Sr/Ca (the resulting age models are almost identical). The heaviest value in each annual cycle was assigned to March, which is the coldest month on average; i.e., the chronology uses one tie point per year. Ages for the other sampling points were interpolated according to their positions along the sampling profile. An equidistant (monthly) time series was interpolated from the original Sr/Ca data and was used as the base for further calculations.

This is a Sr/Ca paper, the d18O data is not reported in the paper so is it "peer reviewed" but just used for time assignment.  The data is on the Pangaea web site but not NOAA.

Kuhnert, H., Crueger, T. and Paetzold, J.: NAO signature in a Bermuda coral Sr/Ca record, Geochemistry, Geophysics, Geosystems, 6(4), n/a–n/a, doi:10.1029/2004gc000786, 2005.

Micromass Optima mass spectrometer with a Micromass Isocarb automated preparation system

; climateInterpretation_seasonality changed - was originally monthly, bimonthly; archiveType changed - was originally Coral (CO)

chronology constructed using seasonal cycles in d18O as well as density couplets in xrays. "we assigned the most enriched value of d18O in each cycle to consecutive Augusts (the average coldest month) down core. We inter- polated linearly between age-assigned d18O data points (sequential Augusts) to assign intra-annual ages, using programs in the ARAND software package (available at http://www.ncdc.noaa.gov/paleo/softlib/arand/arand.html) (P. Howell, personal communication, 1998). "

The coral captures approximately 60% of the full range of annual SST (4i¿½C = 0.88%).

Damassa, T. D., Cole, J. E., Barnett, H. R., Ault, T. R. and McClanahan, T. R.: Enhanced multidecadal climate variability in the seventeenth century from coral isotope records in the western Indian Ocean, Paleoceanography, 21(2), n/a–n/a, doi:10.1029/2005pa001217, 2006.

Enhanced multidecadal climate variability in the seventeenth century from coral isotope records in the western Indian Ocean

used in Tierney et al, as a composite with HR_157; the original records are provided here rather than composites

Linsley, B.K. , A. Kaplan, Y. Gouriou, J. Salinger, P.B. deMenocal, G.M. Wellington, S.S. Howe

Linsley, B. K., Kaplan, A., Gouriou, Y., Salinger, J., deMenocal, P. B., Wellington, G. M. and Howe, S. S.: Tracking the extent of the South Pacific Convergence Zone since the early 1600s, Geochemistry, Geophysics, Geosystems, 7(5), n/a–n/a, doi:10.1029/2005gc001115, 2006.

Thermo- FinniganTM DeltaPlus mass spectrometer coupled to a Kiel device

The high-resolution samples were line- arly interpolated to 12 ??monthly?? values for comparison to climate reconstructions

"The high-resolution samples were line- arly interpolated to 12 ??monthly?? values for comparison to climate reconstructions"

Moses, C. S., Swart, P. K. and Rosenheim, B. E.: Evidence of multidecadal salinity variability in the eastern tropical North Atlantic, Paleoceanography, 21(3), doi:10.1029/2005pa001257, 2006.

Evidence of multidecadal salinity variability in the eastern tropical North Atlantic

Annual extension rates based on sclerochronology were measured on X-radiograph positive prints from the beginning of one high-density band to the beginning of the next

The average interannual ?18O variability at Tobago represents a ?SST of ~1.0i¿½C from one year to the next, about 3.5 times the instrumental ?SST value. This disagreement implies that there are significant interannual changes in salinity responsible for the ?18O of the corals from Tobago.

The average interannual d18O variability at Tobago represents a SST of ~1.0C from one year to the next, about 3.5 times the instrumental deltaSST value. This disagreement implies that there are significant interannual changes in salinity responsible for the d18O of the corals from Tobago.

Stable isotope and luminescence data for Montastaea faveolata andSidereastrea siderea from Buccoo Reef, Tobago

Proceedings of the 10th International Coral Reef Symposium (Okinawa)

Stable isotope and growth records in corals from the island of Tobago: Not simply a record of the Orinoco

Age models were constructed using the AnalySeries program [Paillard et al., 1996]. We used tie points to connect the lowest (highest) d18O values to the warmest (coolest) temperatures in the instrumental SST record to establish each year.The use of coral Sr/Ca values instead of coral d18O values to construct the age model results produces a similar chronology. The geochemical data were then interpolated to give monthly d18O values. The geochemically based age models were confirmed via comparison with ages determined by counting of skeletal density-band couplets in the X-ray images of the coral slab.

Coral d18O variations at Rabaul are likely driven by the combined variations in SST and seawater d18O (and hence SSS) given the general climatology of the WPWP

Coral d18O variations are modestly correlated with SST variations over their common period of overlap (1970? 1993), both in terms of the monthly and monthly anomaly time series

The monthly coral d18O anomaly time series at Rabaul yields no significant correlation with the instrumental SSS record, despite the fact that similar coral records from Fiji [Le Bec et al., 2000] and Vanuatu [Kilbourne et al., 2004] have been demonstrated to reflect SSS variations. It is possible that the monthly coral d18O anomaly record does reflect local SSS variability at Rabaul and the observed low correlation between these two variables results from differences between the ship-track SSS record and the actual SSS variability at Rabaul

Quinn, T. M., Taylor, F. W. and Crowley, T. J.: Coral-based climate variability in the Western Pacific Warm Pool since 1867, Journal of Geophysical Research, 111(C11), doi:10.1029/2005jc003243, 2006.

Coral-based climate variability in the Western Pacific Warm Pool since 1867

both temperature and seawater isotopic composition effect d18O in the Flinders coral record. Δδ18O explains 65% of the variance
displayed by the δ18O signature

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally annual; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Coral (CO)

Calvo, Eva , Marshall, John F. , Pelejero, Carles , McCulloch, Malcolm T. , Gagan, Michael K. , Lough, Janice M.

Calvo, E., Marshall, J. F., Pelejero, C., McCulloch, M. T., Gagan, M. K. and Lough, J. M.: Interdecadal climate variability in the Coral Sea since 1708 A.D., Palaeogeography, Palaeoclimatology, Palaeoecology, 248(1-2), 190–201, doi:10.1016/j.palaeo.2006.12.003, 2007.

Interdecadal climate variability in the Coral Sea since 1708 A.D.

Finnigan MAT-251 mass spectrometer coupled to an automated Kiel carbonate device

IOD  upwelling  cools  the ambient  SST  and  decreases  rainfall,  both  of  which  increase coral d18O.

Abram, N.J., M.K. Gagan, J.E. Cole, W.S. Hantoro, and M. Mudelsee

Abram, N. J., Gagan, M. K., Cole, J. E., Hantoro, W. S. and Mudelsee, M.: Recent intensification of tropical climate variability in the Indian Ocean, Nature Geoscience, 1(12), 849–853, doi:10.1038/ngeo357, 2008.

Recent intensification of tropical climate variability in the Indian Ocean

Finnigan MAT 253 isotope ratio mass spectrometer coupled to a Kiel III carbonate device at WHOI

Age models were developed using density banding visible in the X radiographs to identify the calendar year. X radiographs for these corals have been previously published [Goodkin, 2007; Goodkin et al., 2007, 2005]. Some error is expected within this age model because of years of very little or no growth, not visible on the X ray and also not clearly discernible in the seasonal cycles of Sr/Ca. While there is the potential for error generated by noise in the Sr/Ca or the annual band counting to result in the inappropriate addition of a year, the majority of age model error will arise because of missing years, generating a bias in which coral bands are assigned to artificially recent (younger) dates. For example, if the coral did not grow in 1950, 1949 would be inappropriately assigned the date 1950, and similarly for all coral years prior to 1950 (1781?1949). Such age model bias is suspected during the early to mid-1800s when growth rates were extremely slow for an extended period of time and hiatuses in growth may have occurred [Goodkin et al., 2005].

However, the long-term trends in the raw d18O and Sr/Ca data provide a strong indication that the ocean surface waters near Bermuda were fresher during the LIA, even if we cannot quantitatively partition the temperature and salinity signals. Over the course of the 200-year record, long-term trends in mean annual and wintertime dOc (0.0003%/a and < 0.0001%/a, respectively) are effectively flat (Figures 4a and 4b). If dOc were purely a result of SST, and SST is increasing through time, a strong negative trend would be visible in the dOc records [McConnaughey, 1989a, 1989b].

we show that with the present coral record and relatively short calibration data set, we are unable to derive a robust, statistically significant separation of the salinity and temperature signals within the coral d18O.

There are several factors that may prevent the quantification of these relationships, the most likely being the lack of large changes in SSS documented in the instrumental data. Over the length of the Hydrostation S record, salinity (mean annual and winter) has a range of only 0.3 psu, too small to establish a significant relationship for these proxies, given representation error (noise) in the coral and instrumental records.

Goodkin, Nathalie F. , Hughen, Konrad A. , Doney, Scott C. , Curry, William B.

Goodkin, N. F., Hughen, K. A., Doney, S. C. and Curry, W. B.: Increased multidecadal variability of the North Atlantic Oscillation since 1781, Nature Geoscience, 1(12), 844–848, doi:10.1038/ngeo352, 2008.

Increased multidecadal variability of the North Atlantic Oscillation since 1781

The overlapping parts of sampling transects along different thecal walls were used to assess the reproducibility of the oxygen isotopic signal. Reproducibility is excellent (RSD =1.45%, n = 39).

Chronology was developed on the basis of the seasonal cycle in coral ?18O, and by counting the well-developed annual density bands. The coral ?18O-record extends from 1918 to 2004. The measured skeletal d18O minimum (maximum) was assigned to the month September (February) which represents the average seasonal SST maximum (minimum) at the study site. Linear interpolation was used in order to obtain monthly resolution for statistical analysis.

~1?2 months in any given year, no errors given for annual chronology

Hetzinger 2006 calibration and general d18O to SST slope for corals used (-0.2)

However, the magnitude of the multidecadal variations in coral d18O is larger than expected based on SST alone. The standard deviation of the smoothed SST index shown in Figure 1B is 0.12i¿½C (based on SST from the HadISSTv.1.1 database; Rayner et al., 2003), while the standard deviation of coral !18O is 0.06?, which would correspond to 0.3 i¿½C, assuming well-established relationships. Hence, ~50% of the amplitude is due to variations in d18Oseawater. The d18Oseawater contribution is estimated by calculating the d18Oresidual (i.e., by subtracting the SST component from measured coral d18O; for details see GSA Data Repository). Figure 1C compares the d18Oresidual with a regional precipitation index computed from weather stations in the southeastern Caribbean, which includes the study site. The d18Oresidual and precipitation are highly correlated at low frequencies, implying that multidecadal d18Oseawater variations are primarily atmosphere-driven (r = ?0.46; 1923?1998; and r = ?0.67 for detrended values).

Hetzinger, S., Pfeiffer, M., Dullo, W.-C., Keenlyside, N., Latif, M. and Zinke, J.: Caribbean coral tracks Atlantic Multidecadal Oscillation and past hurricane activity, Geology, 36(1), 11, doi:10.1130/g24321a.1, 2008.

Caribbean coral tracks Atlantic Multidecadal Oscillation and past hurricane activity

Kilbourne 2007, 2008, and 2010 are all the same coral with radiocarbon 2007 and new coral in 2010 extending record to 1479.

Counting annual density bands provided an age model for these samples. The exact position of the annual banding over core breaks was reconstructed by stacking the coral slabs together into round core sections with spacers representing the material lost in cutting the cores and with a life-size copy of the X-radiograph taped to the microdrilled slab. The two pieces of core were joined by aligning the corallites of each section, and the X-radiographs on both sides of the core break were marked exactly where they met. Once the breaks were aligned, we used the X-radiographs to count density bands multiple times. We estimate an error of i¿½1 year at the bottom of the core.

The regression equations presented here are not meant as a quantitative calibration of the Monastraea faveolata paleothermometer, because we do not have monthly seawater d18O during 1993a€“ 2004, but is instead intended to demonstrate the high correlation of d18O to temperature at this site, and that it is reasonable to apply the Leder et al. [1996] calibration slope to these data. Weber and Woodhead [1972] proposed that each coral species has its own carbonate d18Oa€temperature relationship because of the influence of metabolic effects on the d18Oa€temperature relationship. Leder et al. [1996] conducted a thorough calibration study for Montastraea faveolata, utilizing thermister data from next to the coral, regular seawater d18O measurements, and skeletal staining to provide independent time control. Their equation is SST (AºC) = 5.33 a€“ 4.519 (A±0.19) (delta c - delta w)

They use calibration from other studies with this coral species, Montastraea faveolata or annularis (the same coral), 0.22 per mil per degree C [Leder et al., 1996]. In Kilbourne 2010, "centenniala€scale variability appears to be driven by temperature".

Counting annual density bands provided an age model for these samples. The exact position of the annual banding over core breaks was reconstructed by stacking the coral slabs together into round core sections with spacers representing the material lost in cutting the cores and with a life-size copy of the X-radiograph taped to the microdrilled slab. The two pieces of core were joined by aligning the corallites of each section, and the X-radiographs on both sides of the core break were marked exactly where they met. Once the breaks were aligned, we used the X-radiographs to count density bands multiple times. We estimate an error of �1 year at the bottom of the core.

10.1029/2008PA001598, 10.1029/2010gc003171, 10.1007/s00382-007-0224-2

Kilbourne, K. H., Quinn, T. M., Webb, R., Guilderson, T., Nyberg, J. and Winter, A.: Paleoclimate proxy perspective on Caribbean climate since the year 1751: Evidence of cooler temperatures and multidecadal variability, Paleoceanography, 23(3), n/a–n/a, doi:10.1029/2008pa001598, 2008.

Kilbourne, K. H., Quinn, T. M., Webb, R., Guilderson, T., Nyberg, J. and Winter, A.: Coral windows onto seasonal climate variability in the northern Caribbean since 1479, Geochemistry, Geophysics, Geosystems, 11(10), n/a–n/a, doi:10.1029/2010gc003171, 2010.

; climateInterpretation_seasonality changed - was originally bimonthly

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally bimonthly; paleoData_variableName changed - was originally Sr_Ca

Felis, T., Suzuki, A., Kuhnert, H., Dima, M., Lohmann, G. and Kawahata, H.: Subtropical coral reveals abrupt early-twentieth-century freshening in the western North Pacific Ocean, Geology, 37(6), 527–530, doi:10.1130/g25581a.1, 2009.

Subtropical coral reveals abrupt early-twentieth-century freshening in the western North Pacific Ocean

Finnigan MAT252 isotope ratio mass   spectrometer equipped with a Kiel III Carbonate Device

Nakamura, N., Kayanne, H., Iijima, H., McClanahan, T. R., Behera, S. K. and Yamagata, T.: Mode shift in the Indian Ocean climate under global warming stress, Geophysical Research Letters, 36(23), doi:10.1029/2009gl040590, 2009.

Mode shift in the Indian Ocean climate under global warming stress

GV IsoprimeMultiprep mass spectrometer, Horiba JobinYvon Ultima 2C ICPOES

Chronology is built by tying lowest d18O values to Aug, when FanningSST are at their warmest, and tying the highest d18O values to Feb, when Fanning SST are coolest. Ages are interpolated for dates between tie-points

d18Osw derived using Ren et al., 2002 method, with Sr/CaSST slope of 0.06 mmol/mol/permilC and d18OSST slope of 0.21 permil/permilC

Nurhati, I. S., Cobb, K. M., Charles, C. D. and Dunbar, R. B.: Late 20th century warming and freshening in the central tropical Pacific, Geophysical Research Letters, 36(21), doi:10.1029/2009gl040270, 2009.

Hetzinger 2006 is  the calibration paper and Hetzinger 2010 is the full reconstruction with interpretation. Confirmed the data reported for both studies on NOAA web site is the identical.

overlapping parts of sampling transects along different thecal walls were compared for proxy validation. The reproducibility is excellent (RSD is 1.88% for d18O; n = 24)

age model was established on the basis of the pronounced seasonal cycle in the Sr/Ca record. The maximum (minimum) Sr/Ca was tied to March (September), which is on average the coolest (warmest) month in the study area. The coral d18O and Sr/Ca time series were linearly interpolated between these anchor points using the Analyseries software [Paillard et al., 1996] to obtain monthly proxy time series.

Both geochemical proxies show a significant correlation with instrumental SST over a 41-year time period on both monthly and mean annual scales. We obtained proxy-SST calibrations that are consistent with previously published studies using other coral species from different regions. Hetzinger 2006 10.1029/2006GC001347

Correlation and regression assesed with SODA SST, ERSST V2.0, and local air temperature for 1958-1999 for monthly values, extreme values only (max-min mehtod), and annual mean. ERSST extreme values had the correlation, this could be due to subannual dating uncertaincies and linear interpolation to monthly values. Calibration detailed in Hetzinger 2006, 10.1029/2006GC001347

Hetzinger, S. , M. Pfeiffer , W.-C. Dullo , D. Garbe-Schi¿½nberg , J. Halfar

Hetzinger, S., Pfeiffer, M., Dullo, W.-C., Garbe-Schoenberg, D. and Halfar, J.: Rapid 20th century warming in the Caribbean and impact of remote forcing on climate in the northern tropical Atlantic as recorded in a Guadeloupe coral, Palaeogeography, Palaeoclimatology, Palaeoecology, 296(1-2), 111–124, doi:10.1016/j.palaeo.2010.06.019, 2010.

Tropical sea surface temperatures for the past four centuries reconstructed from coral archives

d18Osw (residuals calculated from coupled SrCa and d18O measurements)

interannual d18OSW variations can largely be explained by months-long changes in precipitation minus evaporation and zonal advection

On interannual timescales, Palmyra d18Osw is significantly correlated with ENSO variability (R=-049 for Eastern Pacific Warming, R=-0.19 for Central Pacific Warming), reflecting ENSO related changes in local precipitation and ocean advection. On decadal time-scales, d18Osw likely reflects salinity changes due to larger processes such as PDO.

d18Osw derived using Ren et al., 2002 method, with Sr/CaSST slope of 0.09 mmol/mol/permilC and d18OSST slope of 0.21 permil/permilC

Duplicate of modern coral d18O in CO03COPM01A, also included in composite record Ocean2kHR_139

Nurhati, I. S., Cobb, K. M. and Di Lorenzo, E.: Decadal-Scale SST and Salinity Variations in the Central Tropical Pacific: Signatures of Natural and Anthropogenic Climate Change, Journal of Climate, 24(13), 3294–3308, doi:10.1175/2011jcli3852.1, 2011.

DecadalScale SST and Salinity Variations in the Central Tropical Pacific: Signatures of Natural and Anthropogenic Climate Change

Thermo-Finnigan MAT253 Isotope Ratio Mass Spectrometer (IRMS), with a Kiel IV Carbonate Device, and on a Thermo-Finnigan Delta V Plus IRMS with Gasbench II (GB II) connected to a Conflo IV, both at the Analytical Laboratory for Paleoclimate Studies (ALPS) at the Jackson School of Geosciences, University of Texas at Austin. The precision of the Kiel IV/MAT253 IRMS for samples in this study is 0.05? for d18O and 0.03? for d13C (1s), as estimated via multiple analyses of a carbonate standard (n = 224), which is consistent with longterm precision for this instrument of 0.06? for d18O and 0.03? for d13C. The precision of the GB II/Delta V Plus IRMS is 0.07? for d18O and 0.03? for d13C (1s), as estimated via multiple analyses of the same carbonate standard (n = 25), which is consistent with long-term precision for this instrument of 0.07? for d18O and 0.03? for d13C. Replicate coral samples analyzed on both mass spectrometers yield similar results (mean difference = 0.03? for d18O and 0.12? for d13C; n = 35).

Yes, results are only reported to a depth of 200 cm as a result of diagenetic alteration at the bottom of the core, which is visible as dark patches in the Xradiographs and large excursions, as well as the lack of an annual cycle in the geochemical time series.

Geochemical variations versus depth were converted to variations versus time using AnalySeries software [Paillard et al., 1996]. Geochemical variations in d18O were used to determine a first-order age model, with the maximum intra-annual peaks in d18O being assigned as the coldest month of the year (August), beginning with the year 2007, when the living coral was cored. This first-order age model places d18O variations in the time domain, with uneven time increments (Dt). A second-order age model, with a monthly Dt, was created using the AnalySeries software program, which was verified by comparing years with anomalous d18O values to known ENSO events where possible. This second-order age model is the final age model used in all plots and data analysis.

We develop and test a transfer function constructed using linear regression analysis of SBV coral d18Oanomaly variations and instrumental SSS over the period 1970?2007 CE [Thirumalai et al., 2011]. We performed a calibration-verification exercise (Figure 6) between d18Oanomaly and SSS at SBV to assess the robustness of the transfer function [Quinn and Sampson, 2002]. The slopes in equations (1)?(3) are within error of each other; however, the intercepts are slightly different. Despite this small difference, the similarity of the lines (Figure S2) provides confidence that the transfer function developed in this study can be used to reconstruct past changes in salinity at this locality based on coral d18O variations. We also note that there is a signal in the residuals, which likely reflects a small temperature component in the coral d18O anomaly signal (Figure 6, bottom), most likely due to the small changes in seasonality over this time period (Figure 4c).

We found that the correlations with d18O are 0.72 (with total pseudocoral), 0.47 (with SST component), and 0.68 (with SSS component), p < 0.01 for all three (Figure S1), indicating that SSS changes represent a larger fraction of the variance in the coral d18Oanomaly signal than SST changes, as expected from the larger magnitude of interannual SSS variations at this site. Testing several different percent contributions of SSS and SST to create the pseudocoral, we determined that a combination of 35% SST and 65% SSS results in the closest representation to the observed coral d18Oanomaly values. This was calculated by creating a pseudocoral that consisted of percent SST/SSS contributions that ranged from 100/0% to 0/100%, in increments of 5% (i.e., 100/0, 95/5, 90/10a€¦ 5/95, 0/100). The pseudocoral consisting of 35/65% gave the highest correlation with the measured d18O time series, which provides the percent contributions of SST and SSS to the time series. This relationship was determined over the period 1970a€“2007, and is limited by the length of the instrumental SSS data set. We assume stationarity in the proportional contributions of SST and SSS to the coral d18O signal because SSS data needed to evaluate this assumption are lacking in the pre- 1970 period. However, the assumption of stationarity of a proxy-instrumental relationship developed over the instrumental time period affects all proxy-based climate reconstructions that extend beyond the instrumental period. Thus, lacking additional instrument data and/or another independent SST- or SSS-only proxy there is no easy way to reduce the uncertainty of the empirically derived proxy relationship over the calibration-verification interval.

This study used two cores from the same colony but give data for the colony only

Gorman, Meaghan K. , Quinn, Terrence M. , Taylor, Frederick W. , Partin, Judson W. , Cabioch, Guy , Austin, James A. , Pelletier, Bernard , Ballu, Vali¿½rie , Maes, Christophe , Saustrup, Steffen

Gorman, M. K., Quinn, T. M., Taylor, F. W., Partin, J. W., Cabioch, G., Austin, J. A., Pelletier, B., Ballu, V., Maes, C. and Saustrup, S.: A coral-based reconstruction of sea surface salinity at Sabine Bank, Vanuatu from 1842 to 2007 CE, Paleoceanography, 27(3), n/a–n/a, doi:10.1029/2012pa002302, 2012.

A coral-based reconstruction of sea surface salinity at Sabine Bank, Vanuatu from 1842 to 2007 CE

counting annual density bands in x-rays from known collection date

We found some evidence that skeletal stable isotopic composition may be affected by symbiont clade and suggest this is an important topic for future investigation. If different Symbiodinium clades leave consistent signatures in skeletal geochemical composition, the signature will provide a method to quantify past symbiont shuffling events, important for understanding how corals are likely to respond to climate change.

Carilli, J. E., Charles, C. D., Garren, M., McField, M. and Norris, R. D.: Baseline shifts in coral skeletal oxygen isotopic composition: a signature of symbiont shuffling?, Coral Reefs, 32(2), 559–571, doi:10.1007/s00338-012-1004-y, 2013.

El Nino events bring warmer and rainier conditions to the Northern Line Islands, conditions which constructively act to decrease coral d18O. The opposite climatic effects occur during cool La Nina extremes, driving an increase in coral d18O. Modern Line Islands coral d18O records are high- ly correlated to the regional-scale NINO3.4 index (defined as the average of instrumental SSTs from 5S to 5N, and from 120 to 170W).

interannual d18O variability has a correlation of -0.85 with SST

Relative chronologies were constructed by assigning the maximum ?18O point for a given year to January 15th and linearly interpolating ?18O datapoints in between these tie points, following the procedure outlined in Cobb et al., 2002 for the Palmyra modern and fossil corals U/Th dates used to estimate absolute ages

El Nino events bring warmer and rainier conditions to the Northern Line Islands, conditions which constructively act to decrease coral d18O. The opposite climatic effects occur during cool La Nina extremes, driving an increase in coral d18O.

Modern Line Islands coral d18O records are high- ly correlated to the regional-scale NIi¿½O3.4 index (defined as the average of instrumental SSTs from 5i¿½S to 5i¿½N, and from 120i¿½ to 170i¿½W)

Cobb, K. M., Westphal, N., Sayani, H. R., Watson, J. T., Di Lorenzo, E., Cheng, H., Edwards, R. L. and Charles, C. D.: Highly Variable El Nino–Southern Oscillation Throughout the Holocene, Science, 339(6115), 67–70, doi:10.1126/science.1228246, 2013.

Deng, Wenfeng; Wei, Gangjian; Xie, Luhua; Wang, Zhibing; Zheng, Ti; Liu, Ying

Variations in the Pacific Decadal Oscillation since 1853 in a coral record from the northern South China Sea

Deng, W., Wei, G., Xie, L., Ke, T., Wang, Z., Zeng, T. and Liu, Y.: Variations in the Pacific Decadal Oscillation since 1853 in a coral record from the northern South China Sea, Journal of Geophysical Research: Oceans, 118(5), 2358–2366, doi:10.1002/jgrc.20180, 2013.

Wet and cold climate conditions recorded by coral geochemical proxies during the beginning of the first millennium CE in the northern South China Sea

Xiao, H., Deng, W., Chen, X., Wei, G., Zeng, T. and Zhao, J.: Wet and cold climate conditions recorded by coral geochemical proxies during the beginning of the first millennium CE in the northern South China Sea, Journal of Asian Earth Sciences, 135, 25–34, doi:10.1016/j.jseaes.2016.12.012, 2017.

The data on the NOAA web site combines the two cores together into one long record, the dead coral cores spans 1411-1644 with some overlap and the modern coral spans 1915-1944. The Geology paper and supplemental data do not have much methods information and I downloaded Kellys dissertaion but it is just the published papers. I am familar with the Quinns lab procedures so I filled in information where I could. This is one of the few coral records that spans the earlier part of the LIA so it is important to include even if it is not continous. Kelly has another coral record in her dissertaion for the Medieval Climate Anomaly from Tasmaloum, Vanuatu (15.6i¿½S, 166.9i¿½E), and I am not sure her status with publishing this work but I will ask Terry.

Thermo-Finnigan MAT253 Isotope Ratio Mass Spectrometer (IRMS), with a  Kiel IV Carbonate Device, and on a Thermo-Finnigan Delta V Plus IRMS  with Gasbench II (GB II) connected to a Conflo IV, both at the Analytical Laboratory for Paleoclimate Studies (ALPS) at the Jackson  School of Geosciences, University of Texas at Austin. Longterm precision for this instrument of 0.06? for d18O and 0.03? for d13C. The precision of the  GB II/Delta V Plus IRMS is  long-term precision for this instrument of  0.07? for d18O and 0.03? for d13C. Internal standards testing confirms that isotopic values are consistent between the two instruments.

The geochemical age model was shifted within error of the 230Th dates (Table DR1) to match the timing of the 1578 CE El Nii¿½o event known from historical records (Ortlieb, 2000). The U-th dates have errors of 2-4 year for the fossil corals and the 20th century corals had U-Th erros of 3-5 years.

~1-2 months in any given year, no errors given for annual chronology

The geochemical age model was shifted within error of the 230Th dates (Table DR1) to match the timing of the 1578 CE El Ni�o event known from historical records (Ortlieb, 2000). The U-th dates have errors of 2-4 year for the fossil corals and the 20th century corals had U-Th erros of 3-5 years.

Hereid, K. A., Quinn, T. M., Taylor, F. W., Shen, C.-C., Lawrence Edwards, R. and Cheng, H.: Coral record of reduced El Nino activity in the early 15th to middle 17th centuries, Geology, 41(1), 51–54, doi:10.1130/g33510.1, 2012.

Finnigan MAT 251 mass spectrometer with Kiel Carbonate Device, arian Vista-PRO Simultaneous ICP-OES

Sr/Ca data to monthly SST from the 2i¿½ i¿½ 2i¿½ grid square centered on 4i¿½N, 172i¿½E from the extended reconstructed SST version 3b (ERSSTv3b) data product [Smith et al., 2008; ttp://www.esrl.noaa.gov/psd] [?] Annual Sr/Ca maxima were tied to the coolest points in the SST record using Analyseries [Paillard et al., 1996]. The resulting spacing of Sr/Ca data remained relatively constant throughout the record, and the chronology was verified against growth band counts from the X-radiograph. After converting depth to time in Analyseries, Sr/Ca were interpolated to six equally spaced samples per year using ARAND time series analysis software [Howell, 2001], corresponding  to bimonthly resolution for the length of the record.

coral-based d18Osw is poorly correlated to local rainfall, and likely reflects ocean advection

d18Osw derived using centering method described in Cahyarini et al., 2008, with Sr/Ca-SST slope of -0.084 mmol/mol/?C and d18O-SST slope of -0.22 ?/?C

ENSO dominates d18O on interannual timescales. On decadal and longer timescales, larger scale processes such as PDO likely influence d18O.

The full Butaritari coral Sr/Ca and d18O (Figures 3b and 3c) are well correlated with SST from the 2° x 2° grid cell centered on 4°N, 172°E in ERSSTv3b (R = 0.58 for Sr/Ca and 0.39 for d18O, p < 0.05 on detrended bimonthly data).

Carilli, J. E., McGregor, H. V., Gaudry, J. J., Donner, S. D., Gagan, M. K., Stevenson, S., Wong, H. and Fink, D.: Equatorial Pacific coral geochemical records show recent weakening of the Walker Circulation, Paleoceanography, 29(11), 1031–1045, doi:10.1002/2014pa002683, 2014.

several distinct postive anomalies between 1977 and 1986 should be interpreted with caution. Authors note that these anomalies could be attributed to vital effects or diagensis and should be reproduced with additional cores from Timor

Thermo Finnigan Gasbench II Delta Plus & Spectro Ciros Inductively
Coupled Plasma Optical Emission Spectrophotometer (ICP-OES)

0.06 ‰ (1 sigma) relative to NBS19 for d18O & 60.15% (1 sigma) for Sr/Ca

Sr/Ca tie points to warmest (Dec) and coolest (Aug) months; linear interpolation using Analyseries

coral based d18Osw/SSS lags the precipitation by several months, "Thus, SSS may also be influenced by ocean advection in the nearby seas."

Timor d18Osw shows higher SSS during the NW monsoon (September to February). The coral-based SSS record also confirms a delayed response of seawater freshening, which lags the wettest months by several months.

removed SST contribution on coral d18O using the centering method, with slopes of -0.04 mmol/mol/?C and -0.21 ?/?C

d18O is influenced by multiple environmental parameters (i.e., SST, d18Osw, and SSS, the latter controlled by the P-E balance and oceanic advection) in the Indonesian region

Annual values are most enriched (September) or depleted (March) in between annual SST and SSS maxima and minima, suggesting both contribute to Timor coral d18O

Annual values are most enriched or depleted in between annual SST and SSS maxima and minima, suggesting both contribute to Timor coral d18O

Need to get this dataset from the Authors, they only put raw d18O on NCDC

Cahyarini, S. Y., Pfeiffer, M., Nurhati, I. S., Aldrian, E., Dullo, W.-C. and Hetzinger, S.: Twentieth century sea surface temperature and salinity variations at Timor inferred from paired coral δ18O and Sr/Ca measurements, Journal of Geophysical Research: Oceans, 119(7), 4593–4604, doi:10.1002/2013jc009594, 2014.

Twentieth century sea surface temperature and salinity variations at Timor inferred from paired coral δ18O and Sr/Ca measurements

Cahyarini, S.Y.; Pfeiffer, M.; Nurhati, I.S.; Aldrian, E.; Dullo, W.-C.; Hetzinger, S.

We developed age models by visually comparing coral banding with seasonal d18O and d13C cycles. Dark regions of the coral X-ray positives corresponded with minima in d18O and d13C. We then associated local d18O and d13C minima with March, based on the mean Palau SSS and SST climatology. We converted samples to monthly resolution by performing linear interpolations between chronological anchor points.

Although empirically determined regression slopes are similar to published SST?d18OCRL fractionation values for P. lutea, in both instances, the per cents of explained variance in the regressions are small. This suggests that factors such as SSS are contributing to Palau d18OCRL variability in the pre-instrumental period.

Although empirically determined regression slopes are similar to published SST-d18OCRL fractionation values for P. lutea, in both instances, the percents of explained variance in the regressions are small. This suggests that factors such as SSS are contributing to Palau d18OCRL variability in the pre-instrumental period.

Although empirically determined regression slopes are similar to published SST-d18OCRL fractionation values for P. lutea, in both instances, the per cents of explained variance in the regressions are small. This suggests that factors such as SSS are contributing to Palau d18OCRL variability in the pre-instrumental period.

see Osborne et al. (2013) for discrepancies in the UC composite.

We developed age models by visually comparing coral banding with seasonal d18O and d13C cycles. Dark regions of the coral X-ray positives corresponded with minima in d18O and d13C. We then associated local d18O and d13C minima with March, based on the mean Palau SSS and SST climatology. We converted samples to monthly resolution by performing linear interpolations between chronological anchor points.The UC record is based upon a composite of the living and deceased colonies assembled by ?wiggle matching? chronologies for the period of overlap

Osborne, M.C.; Dunbar, R.B.; Mucciarone, D.A.; Druffel, E.R.M.; Sanchez-Cabeza, J.-A.

Osborne, M. C., Dunbar, R. B., Mucciarone, D. A., Druffel, E. and Sanchez-Cabeza, J.-A.: A 215-yr coral δ18O time series from Palau records dynamics of the West Pacific Warm Pool following the end of the Little Ice Age, Coral Reefs, 33(3), 719–731, doi:10.1007/s00338-014-1146-1, 2014.

A 215-yr coral δ18O time series from Palau records dynamics of the West Pacific Warm Pool following the end of the Little Ice Age

Micromass Optima isotope ratio mass spectrometer coupled to a Multiprep carbonate inlet system at UMR 5805 EPOC

The age of colony CF1B was determined by 230Th/U-dating following established methodology (Edwards et al., 1987; Shen et al., 2002).Three dates were performed at the top, middle, and bottom of the CF1B core. All ages were corrected for the effect of detrital Th contamination assuming a bulk earth 232Th/238U weight ratio of 3.8 for the detritus and 230Th, 234U, and 238U in secular equilibri- um. The reliability of the determined 230Th/U-ages was verified using established criteria such as initial 234U/238U in agreement with 234U/ 238U of modern seawater (i.e., 146 i¿½ 3?) (Shen et al., 2008).,5 years,U/Th error,month,,,,,,,,,,,,,,,,,,,,,,,,,Fossil coral - this record was used to determine the variability of d18Osw by deconvoluing the d18O signal using Sr/Ca data,,https://docs.google.com/spreadsheets/d/1MjIjGINZkkCuTq4taZWDJS0Ddmx_knTJApUoI8PiNao Ocean2kHR_026,CO14ZIHO,Ocn_154,CO14ZIHO01A,coral,zinke2014corals,Zinke, J. , Rountrey, A. , Feng, M. , Xie, S.-P. , Dissard, D. , Rankenburg, K. , Lough, J.M. , McCulloch, M.T.,2014,10.1038/ncomms4607,Zinke, J., A. Rountrey, M. Feng, S.P. Xie, D. Dissard, K. Rankenburg, J. Lough, and M.T. McCulloch. 2014. Corals record long-term Leeuwin Current variability including Ningaloo Nii¿½o/Nii¿½a since 1795. Nature Communications, 5, 3607. doi: 10.1038/ncomms4607,,,,,,Zinke, J.,zinke2014ocean2khrDataCitation,World Data Center for Paleoclimatology, ,Ocean2kHR-IndianAbrolhosZinke2014HAB10A,dataCitation,https://www.ncdc.noaa.gov/paleo/study/16316,-28.4589,113.749,-8,Houtman Abrolhos,1848,2010,x_18O,?,?18O of the coral skeleton,; climateInterpretation_seasonality changed - was originally 1 2 3 4 5 6 7 8 9 10 11 12,coral carbonate,T,sea_surface,1 2 3 4 5 6 7 8 9 10 11 12,negative,,,seawater,1,We used the published bimonthly coral d18O record of Kuhnert et al.12 as our reference coral because the presence of seasonal cycles provided the best age control for all cores.The age model of the new corals was determined by assigning 1 year of growth to a couplet of high- and low-density banding in X-ray-positive prints cross-checked with luminescence banding. The high-density bands were equivalent to summer and low density to winter. The coral d18O record of Kuhnert et al. was averaged annually (January?December), and then each individual annually resolved coral proxy record was normalized to its variance relative to the 1900?1993 reference period. We used the COFECHA tool to aid in cross-dating the annual time series. We aligned the new annually resolved Sr/Ca and d18O records (normalized relative to the 1900?1993 reference period) with the Kuhnert et al. annual time series, and averaged all records to form a composite chronology that extends from 1795 to 2010."

The age of colony CF1B was determined by 230Th/U-dating following established methodology (Edwards et al., 1987; Shen et al., 2002).Three dates were performed at the top, middle, and bottom of the CF1B core. All ages were corrected for the effect of detrital Th contamination assuming a bulk earth 232Th/238U weight ratio of 3.8 for the detritus and 230Th, 234U, and 238U in secular equilibri- um. The reliability of the determined 230Th/U-ages was verified using established criteria such as initial 234U/238U in agreement with 234U/ 238U of modern seawater (i.e., 146 � 3?) (Shen et al., 2008).,5 years,U/Th error,month,,,,,,,,,,,,,,,,,,,,,,,,,Fossil coral - this record was used to determine the variability of d18Osw by deconvoluing the d18O signal using Sr/Ca data,,https://docs.google.com/spreadsheets/d/1MjIjGINZkkCuTq4taZWDJS0Ddmx_knTJApUoI8PiNao Ocean2kHR_026,CO14ZIHO,Ocn_154,CO14ZIHO01A,coral,zinke2014corals,Zinke, J. , Rountrey, A. , Feng, M. , Xie, S.-P. , Dissard, D. , Rankenburg, K. , Lough, J.M. , McCulloch, M.T.,2014,10.1038/ncomms4607,Zinke, J., A. Rountrey, M. Feng, S.P. Xie, D. Dissard, K. Rankenburg, J. Lough, and M.T. McCulloch. 2014. Corals record long-term Leeuwin Current variability including Ningaloo Ni�o/Ni�a since 1795. Nature Communications, 5, 3607. doi: 10.1038/ncomms4607,,,,,,Zinke, J.,zinke2014ocean2khrDataCitation,World Data Center for Paleoclimatology, ,Ocean2kHR-IndianAbrolhosZinke2014HAB10A,dataCitation,https://www.ncdc.noaa.gov/paleo/study/16316,-28.4589,113.749,-8,Houtman Abrolhos,1848,2010,x_18O,?,?18O of the coral skeleton,; climateInterpretation_seasonality changed - was originally 1 2 3 4 5 6 7 8 9 10 11 12,coral carbonate,T,sea_surface,1 2 3 4 5 6 7 8 9 10 11 12,negative,,,seawater,1,We used the published bimonthly coral d18O record of Kuhnert et al.12 as our reference coral because the presence of seasonal cycles provided the best age control for all cores.The age model of the new corals was determined by assigning 1 year of growth to a couplet of high- and low-density banding in X-ray-positive prints cross-checked with luminescence banding. The high-density bands were equivalent to summer and low density to winter. The coral d18O record of Kuhnert et al. was averaged annually (January?December), and then each individual annually resolved coral proxy record was normalized to its variance relative to the 1900?1993 reference period. We used the COFECHA tool to aid in cross-dating the annual time series. We aligned the new annually resolved Sr/Ca and d18O records (normalized relative to the 1900?1993 reference period) with the Kuhnert et al. annual time series, and averaged all records to form a composite chronology that extends from 1795 to 2010."

Wu, H. C., Moreau, M., Linsley, B. K., Schrag, D. P. and Correge, T.: Investigation of sea surface temperature changes from replicated coral Sr/Ca variations in the eastern equatorial Pacific (Clipperton Atoll) since 1874, Palaeogeography, Palaeoclimatology, Palaeoecology, 412, 208–222, doi:10.1016/j.palaeo.2014.07.039, 2014.

GasBench II coupled with Delta XL Isotope Ratio Mass Spectrometer (Thermo Fisher Scientific)

; climateInterpretation_seasonality changed - was originally 1 2 3 4 5 6 7 8 9 10 11 12; archiveType changed - was originally Coral (CO)

0.1 per mil of internal laboratory standard (NBS18, NBS19, L-SVEC)

We used the published bimonthly coral d18O record of Kuhnert et al.12 as our reference coral because the presence of seasonal cycles provided the best age control for all cores.The age model of the new corals was determined by assigning 1 year of growth to a couplet of high- and low-density banding in X-ray-positive prints cross-checked with luminescence banding. The high-density bands were equivalent to summer and low density to winter. The coral d18O record of Kuhnert et al. was averaged annually (January?December), and then each individual annually resolved coral proxy record was normalized to its variance relative to the 1900?1993 reference period. We used the COFECHA tool to aid in cross-dating the annual time series. We aligned the new annually resolved Sr/Ca and d18O records (normalized relative to the 1900?1993 reference period) with the Kuhnert et al. annual time series, and averaged all records to form a composite chronology that extends from 1795 to 2010.

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally 1 2 3 4 5 6 7 8 9 10 11 12; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Coral (CO)

Houtman Abrolhos, East Wallaby Islands, mean annual oxygen isotope and Sr/Ca records, 1795-2010

Zinke, J. , Rountrey, A. , Feng, M. , Xie, S.-P. , Dissard, D. , Rankenburg, K. , Lough, J.M. , McCulloch, M.T.

Zinke, J., Rountrey, A., Feng, M., Xie, S.-P., Dissard, D., Rankenburg, K., Lough, J. M. and McCulloch, M. T.: Corals record long-term Leeuwin current variability including Ningaloo Nino/Nina since 1795, Nature Communications, 5(1), doi:10.1038/ncomms4607, 2014.

should isotope interpretation 2 = Salinity_water? DMT: Fixed 1/14

; climateInterpretation_seasonality changed - was originally 3 4 5 6 7 8 9 10 11 12 13 14; archiveType changed - was originally Coral (CO)

d18O mirrors interannual and decadal variability in regional SST since 1854 in ERSST, since 1850 in HadSST3 and since 1870 in HadSST1

d18O mirrors interannual and decadal variability in regional SST since 1854 in ERSST, since 1850 in HadSST3 and since 1870 in HadSST2

Zinke, J., Loveday, B. R., Reason, C. J. C., Dullo, W.-C. and Kroon, D.: Madagascar corals track sea surface temperature variability in the Agulhas Current core region over the past 334 years, Scientific Reports, 4(1), doi:10.1038/srep04393, 2014.

Madagascar corals track sea surface temperature variability in the Agulhas Current core region over the past 334 years

Thermo MAT-253 mass spectrometer coupled to a Kiel-IV carbonate device

assigning the annual ?18O maximum to the month of the climatological SST minimum at both sites; linear interpolation between annual tie points and resampled to generate monthly series

ocean-atmosphere climate coupling acts to enhance the IOD-related climate signal captured by coral ?18O over that expected from SST anomalies alone

The annual range in coral ?18O is larger than expected based on SST alone, using published coral ?18O-SST dependencies of between 0.17??i¿½C?1 and 0.23??i¿½C?1 [Gagan et al., 2012]. Previous studies in the Mentawai Islands chain have shown that ocean-atmosphere climate coupling acts to enhance the IOD-related climate signal captured by coral ?18O over that expected from SST anomalies alone [Abram et al., 2007, 2008]. The sharp 18O enrichments that characterize the winter isotopic maximum in the South Pagai coral similarly support an additional and complementary rainfall modulation of the coral record during the IOD season.

Nerilie J. Abram, Bronwyn C. Dixon, Madelaine G. Rosevear, Benjamin Plunkett, Michael K. Gagan, Wahyoe S. Hantoro and Steven J. Phipps

Abram, N. J., Dixon, B. C., Rosevear, M. G., Plunkett, B., Gagan, M. K., Hantoro, W. S. and Phipps, S. J.: Optimized coral reconstructions of the Indian Ocean Dipole: An assessment of location and length considerations, Paleoceanography, 30(10), 1391–1405, doi:10.1002/2015pa002810, 2015.

The paper does not assess correlation between d18O and SST due to lack of instrumental SST and upwelling. My assessment of the data shows a 0.36 correlation between coral D18O and coral Sr/Ca suggesting temp rependcany is low. This suggest the coral d18O is primary a salinity signal. note the authors also provide a coral d18Osw data set.

Deng, Wenfeng; Liu, Xi; Chen, Xuefei; Wei, Gangjian; Zeng, Ti; Xie, Luhua; Zhao, Jian-xin

A comparison of the climates of the Medieval Climate Anomaly, Little Ice Age, and Current Warm Period reconstructed using coral records from the northern South China Sea

Deng, W., Liu, X., Chen, X., Wei, G., Zeng, T., Xie, L. and Zhao, J.: A comparison of the climates of the Medieval Climate Anomaly, Little Ice Age, and Current Warm Period reconstructed using coral records from the northern South China Sea, Journal of Geophysical Research: Oceans, 122(1), 264–275, doi:10.1002/2016jc012458, 2017.

Data did not have age model, K. DeLong did on in Analyseries with one tie point per year for inclusion in database. Checked the age model against figure in paper.

isotope interpretation1 should this be d18O of seawater? -BK DMT: No, I double checked the paper.  d18O is primarily temp at this site

Finnigan MAT-252 gas-sourced mass spectrometer housed at the Institute of Earth Environment, Chinese Academy of Science, Xi’an, China. The results are expressed using delta (d) notation relative to the Vienna Pee Dee Belemnite (V-PDB) standard. Stable isotope precision for d18O determined by analysis of the Chinese national standard calcite sample GBW04405 over the course of 2 months was 60.09& (1r; n5138)

monthly coral d18O data to reconstruct a KC transport record with annual to
interannual resolution for the interval 1953–2004. The field site is located in southern Taiwan on the western
flank of the upstream KC. Increased (reduced) KC transport would generate strong (weak) upwelling,
resulting in relatively high (low) local coral d18O.

On average, SSS values vary from 33.5 psu in the wet season to 34.4 psu in the dry season, yielding a small seasonal variability of only 0.9 psu or less [Shen et al., 2005b]. The seasonal change in bay water d18O was only 0.2060.05& in 1993 and 1995 [Shen et al., 2005b], accounting for <17% of the seasonal d18Ocoral variation. A negligible correlation (R520.03) between precipitation and d18Ocoral is observed (supporting information Figure S2). Hence, the d18Ocoral data primarily reflect seasonal SST changes of about 58C (IGOSS SST; Figure

Xiaohua Li , Yi Liu , Yi-Chia Hsin , Weiguo Liu, Zhengguo Shi , Hong-Wei Chiang , and Chuan-Chou Shen

Coral record of variability in the upstream Kuroshio Current during 1953-2004

Li, X., Liu, Y., Hsin, Y.-C., Liu, W., Shi, Z., Chiang, H.-W. and Shen, C.-C.: Coral record of variability in the upstream Kuroshio Current during 1953-2004, Journal of Geophysical Research: Oceans, 122(8), 6936–6946, doi:10.1002/2017jc012944, 2017.

Check data set name; "isotope interpretation1,2,3" is missing. -BK DMT (12/30/19): Resolved!

Authors calculated the contribution of SST to the δ18Ocoral signal, using a δ18O-SST slope of 0.18‰/°C (Gagan et al., 1998) and a range of published δ18O-SSS slopes (Moore, 1995; Fairbanks et al., 1997; Gorman et al., 2012; Morimoto et al., 2002; Conroy et al., 2017; Table S1 and supporting information text). They estimate that SST has a 29–39% inﬂuence on the δ18Ocoral, supporting that SSS drives the δ18Ocoral signal. Authors therefore used seasonal SSS tie points to develop the age model.

Murty, Sujata; Goodkin, Nathalie; Halide, Halmar; Natawidjaja, Danny; Suwargadi, Bambang; Suprihanto, Imam; Prayudi, Dudi; Switzer, Adam; Gordon, Arnold

Monthly and Bimonthly d18O measurements of a Porites coral collected from Doangdoangan Besar in the southern Makassar Strait. The d18O data were determined using isotope ratio mass spectrometry (IRMS)

Climatic Influences on Southern Makassar Strait Salinity Over the Past Century

Murty, S. A., Goodkin, N. F., Halide, H., Natawidjaja, D., Suwargadi, B., Suprihanto, I., Prayudi, D., Switzer, A. D. and Gordon, A. L.: Climatic Influences on Southern Makassar Strait Salinity Over the Past Century, Geophysical Research Letters, 44(23), 11,967–11,975, doi:10.1002/2017gl075504, 2017.

National Oceanic and Atmospheric Administration, Division of Climate Observations, U.S. Department of Commerce

isotope interpretation1,2,3 are missing. -BK DMT: added for all isotope variables in this data series

Time axis is in the csv file, but formatting issue during LiPD conversion

Salinity variability for the past half century are qualitatively captured in the Palaui Diploastrea δ18Oc, showing a freshening trend consistent with Porites δ18Oc, instrumental SSS, and coral-based records within the IndoPaciﬁc region. However, a robust Diploastrea δ18Oc and SSS calibration at interannual timescales was not achieved as a result of the competing SST and SSS inﬂuences dampening the δ18Oc signal and compounding effects of continuing coral calciﬁcation during different seasons. Diploastrea δ18Oc should be useful in places where there is high salinity range (mean annual salinity >~1.5 psu) and where SST and SSS signals combine to enlarge the δ18Oc amplitude as previously investigated in the central and South Paciﬁc regions.

Diploastrea heliopora
 Sr/Ca and δ18
O records from northeast Luzon, Philippines: An assessment of interspecies coral proxy calibrations and climate controls of sea surface temperature and salinity

Ramos, R. D., Goodkin, N. F., Siringan, F. P. and Hughen, K. A.: Diploastrea heliopora Sr/Ca and δ18O records from northeast Luzon, Philippines: An assessment of interspecies coral proxy calibrations and climate controls of sea surface temperature and salinity, Paleoceanography, 32(4), 424–438, doi:10.1002/2017pa003098, 2017.

Wu, H.C., T. Felis, D. Scholz, C. Giry, M. Kölling, K.P. Jochum, and S.R. Scheffers

Changes to Yucatán Peninsula precipitation associated with salinity and temperature extremes of the Caribbean Sea during the Maya civilization collapse

Wu, H. C., Felis, T., Scholz, D., Giry, C., Koelling, M., Jochum, K. P. and Scheffers, S. R.: Changes to Yucatan Peninsula precipitation associated with salinity and temperature extremes of the Caribbean Sea during the Maya civilization collapse, Scientific Reports, 7(1), doi:10.1038/s41598-017-15942-0, 2017.

Xiao, Hangfang; Deng, Wenfeng; Chen, Xuegei; Wei, Gangjian; Zheng, Ti; Zhao, Jian-xin

Micromass Optima gas-source triplecollector mass spectrometer in the Stable Isotope Ratio Mass Spectrometer (SIRMS) Laboratory at the University at Albany, State University of New York. Over TF1 analytical time, the long-term precision of NBS-19 (laboratory standard) d18O was 0.05& (N 5 123) and the average difference between replicates was 0.049& (N 5 96).

Dassié, Emilie P. Hasson, Audrey Khodri, Myriam Lebas, Nicolas Linsley, Braddock K.

Spatiotemporal Variability of the South Pacific Convergence Zone Fresh Pool Eastern Front from Coral-Derived Surface Salinity Data

Dassie, E. P., Hasson, A., Khodri, M., Lebas, N. and Linsley, B. K.: Spatiotemporal Variability of the South Pacific Convergence Zone Fresh Pool Eastern Front from Coral-Derived Surface Salinity Data, Journal of Climate, 31(8), 3265–3288, doi:10.1175/jcli-d-17-0071.1, 2018.

Finnigan MAT 253 mass spectrometer at the Royal NIOZ, Netherlands.

Hennekam, Rick Zinke, Jens van Sebille, Erik ten Have, Malou Brummer, Geert-Jan A. Reichart, Gert-Jan

Cocos (Keeling) Corals Reveal 200 Years of Multidecadal Modulation of Southeast Indian Ocean Hydrology by Indonesian Throughflow

Hennekam, R., Zinke, J., van Sebille, E., ten Have, M., Brummer, G.-J. A. and Reichart, G.-J.: Cocos (Keeling) Corals Reveal 200 Years of Multidecadal Modulation of Southeast Indian Ocean Hydrology by Indonesian Throughflow, Paleoceanography and Paleoclimatology, 33(1), 48–60, doi:10.1002/2017pa003181, 2018.

Thermo Scientific MAT-253 mass spectrometer equipped with a CARBO Kiel IV device

Row 155 and 156 look the same- and both appear to be chronology data DMT: Both are d18O-SST data calculated & reported by authors

Hennekam, R., J. Zinke, E. van Sebille, M. ten Have, G.-J.A. Brummer, and G.-J. Reichart

Tracking Interannual- to Multidecadal-Scale Climate Variability in the Atlantic Warm Pool Using Central Caribbean Coral Data

Von Reumont, J., Hetzinger, S., Garbe-Schoenberg, D., Manfrino, C. and Dullo, C.: Tracking Interannual- to Multidecadal-Scale Climate Variability in the Atlantic Warm Pool Using Central Caribbean Coral Data, Paleoceanography and Paleoclimatology, 33(4), 395–411, doi:10.1002/2018pa003321, 2018.

Finnigan MAT-251 mass spectrometer with an automated Carousel-48-carbonate device

Ages for samples were assigned on the basis of well-defined density banding, assuming that the base of the dense band coresponds to February and that extensions rates between these points are linear

Linear least squares regressions of four of the tracers (δ18O, δ13O, Ba/Ca, Cd/Ca) against Peruvian SST show highly significant correlations(p<0.0001). Over the annual, biennial, and ENSO (3.8 years) frequency bands, cross‐spectral comparisons show even stronger coherency, with SST frequently accounting for 70–80% of the variance in these tracers.

Shen G.T., J. E. Cole, D. W. Lea, L. J. Linn, T. A. McConnaughey, R. G. Fairbanks

Shen, G. T., Cole, J. E., Lea, D. W., Linn, L. J., McConnaughey, T. A. and Fairbanks, R. G.: Surface ocean variability at Galapagos from 1936-1982: Calibration of geochemical tracers in corals, Paleoceanography, 7(5), 563–588, doi:10.1029/92pa01825, 1992.

Finnigan  MAT  251  mass  spectrometer  with  an  automated  Carousel-48  carbonate  device

"We obtained excellent replication of...regions of overlap between cores and in slabs where two transects were sampled"

Ages were determined independently for the two cores on the basis of seasonal d13C variability, which is supported by radiometric and density-banding observations of young Tarawa corals.  We normalized the records, spliced them together using diagnostic density and isotopic patterns, and interpolated them to monthly resolution for statistical analysis

At Tarawa, results from an ongoing monitoring program confirm that intenst rainfall alters the d18O and salinity of the surface mixed layer.  Shallow-growing corals incorporate this isotopic shift in the d18O of their aragonite skeletons.

Correlation of Tarawa d18O record with local SST on monthly (0.62), seasonal (0.67) and annual (0.78) timescales compared to local rainfall on monthly (0.39 or 0.59), seasonal (0.47 or 0.66), and annual (0.59 or 0.80) timescales.

Cole, J. E., Fairbanks, R. G. and Shen, G. T.: Recent Variability in the Southern Oscillation: Isotopic Results from a Tarawa Atoll Coral, Science, 260(5115), 1790–1793, doi:10.1126/science.260.5115.1790, 1993.

The Southern Oscillation recorded in the d18O of corals from Tarawa Atoll

Pavona gigantae - Original data - Dumbar et al., 1994 and updated version Druffel et al., 2015     https://www.ncdc.noaa.gov/cdo/f?p=519:1:::::P1_STUDY_ID:18255  https://www.ncdc.noaa.gov/cdo/f?p=519:1:::::P1_STUDY_ID:16971

Finnigan MAT252 mass spectrometer coupled to a KIEL III carbonate device

The annual UR-87 chronology is based on counts of dense bands observed in X radiograph positive prints as well as stable isotope profiles

 The annual UR-87 chronology is based on counts of dense bands observed in X radiograph positive prints as well as stable isotope profiles

Dunbar, R. B., Wellington, G. M., Colgan, M. W. and Glynn, P. W.: Eastern Pacific sea surface temperature since 1600 A.D.: The δ18O record of climate variability in Galapagos Corals, Paleoceanography, 9(2), 291–315, doi:10.1029/93pa03501, 1994.

Automated carbonate reaction device (Kiel Device) connected to a Finnigan Mat 252 mass spectrometer

Heiss, G.A. 1994. Coral reefs in the Red Sea: Growth, production and stable isotopes. GEOMAR Report, 32:1-141.

At decadal time scale the d18O signal is only influenced by d18Osw (Salinity and precipitation), NO influence of Temperature

VG Micromass 602E mass spectrometer upgraded with SIRA series electronics

; climateInterpretation_seasonality changed - was originally subannual; archiveType changed - was originally Coral (CO)

cross-checking the annual d18O variation against the annual dense bands counted from the positive X-rays as well as setting the lowest d18O value in a given year equal to November

Linsley, B. K., Dunbar, R. B., Wellington, G. M. and Mucciarone, D. A.: A coral-based reconstruction of Intertropical Convergence Zone variability over Central America since 1707, Journal of Geophysical Research, 99(C5), 9977, doi:10.1029/94jc00360, 1994.

A coral-based reconstruction of Intertropical Convergence Zone variability over Central America since 1707

automatic carbonate preparation system +VG Isogas Prism mass spectrometer.

In our corals we used a combination of distinctive skeletal fluorescent banding (visible under illumination with longwave UV light; Fig. 2) to provide an initial chronology. The accuracy of this chronology was subsequently verified on a year-byyear basis by consideration of the annual cycle in skeletal d18O

There is a good visual match between the smoothed coral record and the similarly smoothed Madang rainfall record for the period from the late 1950s onwards (Fig. 3B). Periods of low rainfall coincide with deposition of isotopically heavy skeleton.... Periods of high amplitude of annual cycle tend to coincide in both records, and these periods tend to occur during the El Nifio phase of the Southern Oscillation. These results suggest that, although relatively small in absolute terms, the observed variations in the amplitude of the coral dI80 annual cycle (about 0.l-0.2 permil) may be attributed mainly to variations in rainfall.

inter-annual temperature variations are related to the SO activity, and, although relatively small, these will tend to magnify the SO signal in 
the coral d18O.

Tudhope, A.W.; Shimmield, G.B.; Chilcott, C.P.; Jebb, M.; Fallick, A.E.; Dalgleish, A.N.

Tudhope, A. W., Shimmield, G. B., Chilcott, C. P., Jebb, M., Fallick, A. E. and Dalgleish, A. N.: Recent changes in climate in the far western equatorial Pacific and their relationship to the Southern Oscillation; oxygen isotope records from massive corals, Papua New Guinea, Earth and Planetary Science Letters, 136(3-4), 575–590, doi:10.1016/0012-821x(95)00156-7, 1995.

Recent changes in climate in the far western equatorial Pacific and their relationship to the Southern Oscillation; oxygen isotope records from massive corals, Papua New Guinea

The study was 4 samples per year but data is given as annual average values on NOAA web site. The original meta data on NOAA states there are four files, vanuatu.xls (Microsoft Excel Workbook), vanuatu.2yr.txt, vanuatu.4yr.txt, vanuatu.annual.txt (Tab-delimited text), but these appear to be missing from NOAA web site now. I have a copy archived of these files (kdelong@lsu.edu).

MAT 251 mass spectometer coupled with a CarboKiel carbonate extraction device at the University of Michigan

Sampling resolution is four samples per year, one sample in the middle of each density band. The 0.5 mm diameter, discrete point sampling strategy used in this study creates samples that are a homogeneous mixture of-26 (7 mm/year) to -20 (9 mm/year) days of skeletal growth, assuming a linear extension rate. (Quinn et al, 1993). Isotope sampling methods were also identical to Quinn et al. [1993], with new samples being midway between the original samples reported in that study.

This sample was collected alive at < 1 m water depth (Quinn 1993). Comparison of the d180 with SST and rainfall records indicates a correlation of 0.71 and 0.54, respectively, over the 13-year interval where data overlaps (Fig. 2). Just as in the precipitation and SST comparison, the correlation is much higher at the annual cycle (coherence of 0.95). There is also a slight suggestion of coherence at the El Nino time scale, but the calibration time series is too short to draw any definitive conclusions. Since the 0.71 correlation between SST and d180 explains only half the variance in the SST record, other factors are obviously responsible for the d180 variations. (Quinn 1996)

Comparison of the d180 with SST and rainfall records indicates a correlation of 0.71 and 0.54, respectively, over the 13-year interval where data overlaps (Fig. 2). Just as in the precipitation and SST comparison, the correlation is much higher at the annual cycle (coherence of 0.95). There is also a slight suggestion of coherence at the El Nino time scale, but the calibration time series is too short to draw any definitive conclusions. Since the 0.71 correlation between SST and d180 explains only half the variance in the SST record, other factors are obviously responsible for the d180 variations.

Quinn et al., 1996, SST/d180 calibration for Platygyra has been estimated at 0.266 per mil d18 per degree C [Weber and Woodhead 1972]

The original meta data on NOAA states there are four files, vanuatu.xls (Microsoft Excel Workbook), vanuatu.2yr.txt, vanuatu.4yr.txt, vanuatu.annual.txt (Tab-delimited text), but these appear to be missing from NOAA web site now. I have a copy archived of these files (kdelong@lsu.edu).

Quinn, T. M., Taylor, F. W. and Crowley, T. J.: A 173 year stable isotope record from a tropical south pacific coral 0, Quaternary Science Reviews, 12(6), 407–418, doi:10.1016/s0277-3791(05)80005-8, 1993.

New stable isotope results from a 173-year coral from Espiritu Santo, Vanuatu

Quinn, T. M., Crowley, T. J. and Taylor, F. W.: New stable isotope results from a 173-year coral from Espiritu Santo, Vanuatu, Geophysical Research Letters, 23(23), 3413–3416, doi:10.1029/96gl03169, 1996.

The authors note that their coral was not sampled optimally for intra-annual variabilty and their sampling method did not capture the seasonal cycle (Leder et al., 1996). The authors also note that they may have sampled off the thecal wall and may have included endothecal material what would have represented different time intervals. Montastraea annularis (may actually be M. faveolata; this coral definition varies with time) reproduces in the summer and they deposit a high denisty band, which Swart assumes in July. It is possible this coral does not grow at a constant rate and slows its extention in the warmer summer months, thus the annual mean d18O could be bias towards non-summer months. Examining this annual d18O record versus monthly SST and SSS, similar to tree-ring studies may provide further insight on how to interprete this record.

MAT 251 mass spectometer with an automated carbonate device, no pretreatment used , reactions at 90 degrees C.

should "isotope interpretation1" = Salinity_water? -BK . DMT:  Authors interpret in terms of summer precip.

Counting annual density bands provided an age model for these samples assuming high density band is July. Data linearly interpolated to monthly for less than 12 samples per year and used rectanglar interpolation for years with more than 12 samples. From NOAA wb site: The skeleton was sampled at about 10-15 samples a year and  these data have been pooled to construct the annual means.

when precipitation is greater than average, precipitation is inversely correlated with d18O reflecting the input of isotopical depleted precipitation, and vice versa reflectin ghte input of isotopically heavy weaters from the Everglades.

Swart, P. K., Dodge, R. E. and Hudson, H. J.: A 240-Year Stable Oxygen and Carbon Isotopic Record in a Coral from South Florida: Implications for the Prediction of Precipitation in Southern Florida, PALAIOS, 11(4), 362, doi:10.2307/3515246, 1996.

Tierney, Jessica E.,Abram, Nerilie J.,Anchukaitis, Kevin J.,Evans, Michael N.,Giry, Cyril,Kilbourne, K. Halimeda,Saenger, Casey P.,Wu, Henry C.,Zinke, Jens

This coral species is Solenastrea bournoni, one not used in coral climate reconstructions, and it is located in a complex system of Florida Bay where waters from the Everglades enter the ocean and ther eare high rates of evaporation. The d18O system is not additive but subtractive for SSS and SST. Swart 1999 revisited this coral colony and they collect a new core from the same colony. Hudson 1989 gives a map with the coral location, which is 24degrees 55 minutes, and ~80 degrees and between 40 and 50 minutes, about 44 minutes nu my eye. Swart 1999 NOAA has different corrdinates for this coral 25 0N, 80 36W, Looking at Google earth and Hudsons map, the Swart 1999 corrdinates incorrect, they should be 24 degrees 55 minutes N, and ~80 degrees, 43.5 minutes W

MAT 251 mass spectometer, reactions at 90 degrees C. All data have been corrected for the usual isobaric interferences.

In South Florida, the dense band forms in the late summer, but it is generally thought that there is as much as a i¿½ two month variation in timing. By counting the number of bands in a coral, the age can be assessed. Errors in age interpretation arise when dense bands are indistinct or when so-called "stress bands", resulting from events such as temperature extremes, occur. Generally speaking, a year in which a stress band forms may actually contain two dense bands or a thicker dense band which is a combination of the stress and normal dense band. Although it is possible to misinterpret a stress band as an annual band, the annual bands can be recognized by their regular spacing. Therefore, density changes can still provide a clear annual chronology.

Florida bay experiences more evaporation in the summer thus d18O is not additive, warm dry summers, cold wet winters.

The higher skeletal d18O value reflects the high d180 value of the Bay  water itself (Lloyd, 1964; Swart et al., 1989), which is enriched in d18O as a result of evaporation and the input of 1so enriched freshwater  from the Everglades (Meyers et al., 1993). Salinity values are the highest during the summer, as a result of evaporation, and lower during the winter when the Bay becomes dominated by water from the Gulf of Mexico and the Florida Reef Tract. These changes in salinity should be manifested in the 6180 of the coral, but as the maximum enrichment in the water occurs during the warmest portion of the year (the summer), the temperature and salinity effects tend to counteract each other, thereby reducing the observed range of oxygen isotopic variation seen in the coral.

In South Florida, the dense band forms in the late summer, but it is generally thought that there is as much as a � two month variation in timing. By counting the number of bands in a coral, the age can be assessed. Errors in age interpretation arise when dense bands are indistinct or when so-called "stress bands", resulting from events such as temperature extremes, occur. Generally speaking, a year in which a stress band forms may actually contain two dense bands or a thicker dense band which is a combination of the stress and normal dense band. Although it is possible to misinterpret a stress band as an annual band, the annual bands can be recognized by their regular spacing. Therefore, density changes can still provide a clear annual chronology.

Swart 1999 NOAA has different corrdinates for this coral 25 0N, 80 36W, Looking at Google earth and Hudsons map, the Swart 1999 corrdinates incorrect, they should be 24 degrees 55 minutes N, and ~80 degrees, 43.5 minutes W

10.1016/0031-0182(95)00078-X, 10.1016/0168-9622(91)90055-2, 10.1002/2014PA002717

Swart, P. K., Healy, G. F., Dodge, R. E., Kramer, P., Hudson, J. H., Halley, R. B. and Robblee, M. B.: The stable oxygen and carbon isotopic record from a coral growing in Florida Bay: a 160 year record of climatic and anthropogenic influence, Palaeogeography, Palaeoclimatology, Palaeoecology, 123(1-4), 219–237, doi:10.1016/0031-0182(95)00078-x, 1996.

Swart, P. K., Burns, S. J. and Leder, J. J.: Fractionation of the stable isotopes of oxygen and carbon in carbon dioxide during the reaction of calcite with phosphoric acid as a function of temperature and technique, Chemical Geology: Isotope Geoscience section, 86(2), 89–96, doi:10.1016/0168-9622(91)90055-2, 1991.

 automatic carbonate prepa- ration device (optimized for efficient throughput of samples)  attached  to  a  Finnegan  MAT252  gas source mass spectrometer

used the d18O cycle to count annual layers; assigned the high d18O extremes to Aug 1 of every year and interpolated linearly between these tie points.  The largest d18O anomaly (late 1877) matches the most catastrophic monsoon failure on record

Authors suggest that ENSO dominates d18O variations on interannual timescales, while the Asian monsoon system drives decadal variability in d18O at this site

At  the  Seychelles,  however, one would expect the seasonal temperature variability (of more than 2i¿½C) to dominate the nearly constant d18O of seawater

Furthermore, correspondence with an independent index   of   monsoon   strength demonstrates  that  the  coral  successfully  captures the  large-scale  aspects  of  Asian  monsoon behavior

Charles, C. D.: Interaction Between the ENSO and the Asian Monsoon in a Coral Record of Tropical Climate, Science, 277(5328), 925–928, doi:10.1126/science.277.5328.925, 1997.

Interaction Between the ENSO and the Asian Monsoon in a Coral Record of Tropical Climate

alteration and sample treatment is discussed in Boiseau and Juillet-Leclerc 1997

The chronology is then established by associating each maximum and minimum in d18O with each minimum (August) maximum (March) in the SST record (Figure2), assuming a constant linear extension rate between these 2 months

The relative distributionof rainfall and SST versus time (Figure4) compared with d18O versus core depth over the 1979-1990 period emphasizes a strong similarity between SST and d18O

Boiseau, M., Juillet-Leclerc, A., Yiou, P., Salvat, B., Isdale, P. and Guillaume, M.: Atmospheric and oceanic evidences of El Nino-Southern Oscillation events in the south central Pacific Ocean from coral stable isotopic records over the last 137 years, Paleoceanography, 13(6), 671–685, doi:10.1029/98pa02502, 1998.

Atmospheric and oceanic evidences of El Nino-Southern Oscillation events in the south central Pacific Ocean from coral stable isotopic records over the last 137 years

Boiseau, M., Ghil, M. and Juillet-Leclerc, A.: Climatic trends and interdecadal variability from south-central Pacific coral records, Geophysical Research Letters, 26(18), 2881–2884, doi:10.1029/1999gl900595, 1999.

Chakraborty, S., and R. Ramesh. 1998. Stable isotope variations in a coral (Favia speciosa) from the Gulf of Kutch during 1948-1989 AD: Environmental implications. Proceedings of the Indian Academy of Science (Earth and Planetary Sciences) 107(4):331-341.

Finnigan MAT251 gas source mass   spectrometer with a Carousel48 automated sample preparation device

; climateInterpretation_seasonality changed  was originally monthly; archiveType changed  was originally Coral (CO)

~annual spikes in d13C assumed to take place in April, ages for depths between spikes are linearly interpolated. Chronology is constrained by density banding in xrays and growth rates.

 Kiritimati (Christmas) Island Sr/Ca and isotope records 19381993

Evans, M. N., Fairbanks, R. G. and Rubenstone, J. L.: A proxy index of ENSO teleconnections, Nature, 394(6695), 732–733, doi:10.1038/29424, 1998.

Duplicate with Quinn 2002, Stephans 2004 for the interval 1992-1967 only. DeLong 2012 and 2013 updated the chronology for Quinn 1998, updated d18O and d13C paper is in progress. The new bottom date is 1649 and is based on cross-dating two cores and several 230Th dates. DeLong 2013 details several sections that were suboptimally sampled and replaced with new optimal sampling paths. Use this record with caution since it has changed.

For the upper part of the record (1992-1952) a calendar year was first assigned to each density-band couplet and hence to every 12 samples assuming linear subannual skeletal extension. Second, systematic variations in oxygen isotopic composition were correlated with monthly SST values by using the AnalySeties program [Paillard et al., 1996] to match the peaks and troughs in the two time series. For the lower part of the record (1657-1951), simple band counting was used to extend the chronology back to the beginning of the record, which we estimate to be 1657. Although we have no absolute dates on this coral, Crowley et al. [1997] recently demonstrated that some of the distinctive cool excursions in the mean annual record coincide within 1 year of known volcanic eruptions as determined from the volcano chronology of Sirekin and Siebert [1994] and various ice core records

there are some indications from the salinity record for New Caledonia [Quinn et al., 1996b] of interannual changes of as much as 0.5 per mil. The potential impact of a 0.5 per mil interannual salinity variation on d18O seawater enceo n interannucaol ral$ ?80r angefsr om 0.14 per mil [Fairbanks et al., 1997] to 0.15 per mil [Craig and Gordon, 1965]. This effect could explain part of the difference in the seasonal and mean annual slope of d180/SST is discussed above.

Calibration between the instrument (local SST and gridded GISST2) and proxy records was evaluated using two regression techniques: standard ordinary least sqaures and reduced major axis.

possible duplicate with Quinn 2002, Stephans 2004 for 1992-1967 only DeLong 2012 has updated the chronology for Quinn 1998, updated d18O and d13C paper is in progress.

The original meta data on NOAA states there are five files, NC.Coral.5_98.xls (Microsoft Excel format), NC.1951-1657.Qtr.txt, NC.1992-1952.Mon.txt,  NC.Published.1992-1657.Qtr.txt, NC.RawData.txt (Tab delimited ASCII files of the individual sheets in NC.Coral.5_98.xls), but these appear to be missing from NOAA web site now. I have a copy archived of these files (kdelong@lsu.edu) as well as the new updated chronology and new d18O data that repalced the suboptimal sections discussed in DeLong 2013.

10.1029/98PA00401, 10.1029/96PA01859, 10.1029/97PA01348, 10.1029/1999PA900032, 10.1038/nclimate1583, 10.1016/j.palaeo.2012.08.019

Quinn, T. M., Crowley, T. J., Taylor, F. W., Henin, C., Joannot, P. and Join, Y.: A multicentury stable isotope record from a New Caledonia coral: Interannual and decadal sea surface temperature variability in the southwest Pacific since 1657 A.D, Paleoceanography, 13(4), 412–426, doi:10.1029/98pa00401, 1998.

Quinn, T. M., Taylor, F. W., Crowley, T. J. and Link, S. M.: Evaluation of sampling resolution in coral stable isotope records: A case study using records from New Caledonia and Tarawa, Paleoceanography, 11(5), 529–542, doi:10.1029/96pa01859, 1996.

Siderastrea spp.,  the influence of salinity overwhelms the temperautre influence on the oxygen isotopic composition of corals

Finningan-MAT 251 mass spectrometer attached to an automated carousel

Swart, P. K., White, K. S., Enfield, D., Dodge, R. E. and Milne, P.: Stable oxygen isotopic composition of corals from the Gulf of Guinea as indicators of periods of extreme precipitation conditions in the sub-Sahara, Journal of Geophysical Research: Oceans, 103(C12), 27885–27891, doi:10.1029/98jc02404, 1998.

Oxygen isotope records in banded corals( i¿½!80) are mainly controlled by water composition (i.e., seawater salinity) and sea surface temperature (SST) at the time of accretion

Druffel, E. R. M. and Griffin, S.: Variability of surface ocean radiocarbon and stable isotopes in the southwestern Pacific, Journal of Geophysical Research: Oceans, 104(C10), 23607–23613, doi:10.1029/1999jc900212, 1999.

There is a 0.2 per mil offset in absolute value between the Nauru 1 and 2 records; The offset is ~0.23 per mil prior to 1980 and ~0.14 per mil after 1980

samples were reacted in vacuo in a modified autocarbonate device at 90C and the purified CO2 analyzed on a gas source stable isotope ratio mass spectrometer

we created a preliminary age model using the seasonal (doublet) structure of the respective d13C time series. The age model of Nauru 2 was then optimized through linear mapping of the coral d18O to the local precipitation record with an estimated error of 2-3 months. Over the interval where the two corals have similar sampling resolution (i.e., 1 and 2 mm density) the Nauru 1 d18O record was linearly mapped to the Nauru 2 d18O record

Local  precipitation  and  SST  anomalies  at  Nauru,  indicative  of  the  state  of  the  Southern  Oscillation,  are  faithfully  recorded  in  coral  ?80  over  the  100  year  long  time  series  of  the  two  corals  analyzed

"we created a preliminary age model using the seasonal (doublet) structure of the respective d13C time series. The age model of Nauru 2 was then optimized through linear mapping of the coral d18O to the local precipitation record with an estimated error of 2-3 months. Over the interval where the two corals have similar sampling resolution (i.e., 1 and 2 mm density) the Nauru 1 d18O record was linearly mapped to the Nauru 2 d18O record"

There is a 0.2 per mil offset in absolute value between the Nauru 1 and 2 records; The offset is ~0.23 per mil prior to 1980 and ~0.14 per mil after 1981

The observed d180 decrease that occurs between 1952 and 1995 (-0.5 permil) equates to a -2.5C warming, an -2 permil decrease in salinity [Fairbanks et al., 1997], or some combination thereof. Instrumental and reconstructed SSTs of a slightly larger region [Reynolds and Smith, 1994; Kaplan et al., 1998] do show an -0.5C increase which can only be partly responsible for the observed trend in the coral records. Moreover, the shift does not appear to be a consequence of a change in the isotopic composition of precipitation in the region [Rozanski et al., 1992].

Guilderson, T. P. and Schrag, D. P.: Reliability of coral isotope records from the Western Pacific Warm Pool: A comparison using age-optimized records, Paleoceanography, 14(4), 457–464, doi:10.1029/1999pa900024, 1999.

Reliability of coral isotope records from the Western Pacific Warm Pool: A comparison using age-optimized records

Slabs were carefully checked for diagenetic alterations using X-radiographs, thin sec- tions, and SEM.

A first rough age assignment was based on the density banding pattern evident in x-radiographs over most portions of the coral core. Each couplet of one low- and one high-density band represents the growth of one year. The higher-resolving age model is based on the assumption, that coral d18O primarily depends on temperature. In the d18O data deriving from an annual banding couplet the highest value was assigned to the mid of September, the coldest month on average. The chronology is thus tied to one point within each year; the ages of the other sampling points were linearly interpolated according to their spatial distances along the sampling profile. In skeletal portions with unclear density banding pattern the stratigraphy is solely based on cyclic variations in coral d18O. Each cycle was assumed to represent an annual cycle, as long as it occurred over a skeletal portion extending between 10 and 20 mm. Assignments of sub-annual dates were performed as described

Kuhnert, H., J. PA¤tzold, B. Hatcher, K.H. Wyrwoll, A. Eisenhauer, L. B. Collins, Z. R. Zhu, and G. Wefer

Kuhnert, H., Paetzold, J., Hatcher, B., Wyrwoll, K.-H., Eisenhauer, A., Collins, L. B., Zhu, Z. R. and Wefer, G.: A 200-year coral stable oxygen isotope record from a high-latitude reef off Western Australia, Coral Reefs, 18(1), 1–12, doi:10.1007/s003380050147, 1999.

Some chronology issue can be due to fish grazzing scars  Influence of salinity on coral d18O variability very small and not constant with time (some year more affected than some others)

Using density band because they were very clear, then the chronology was tunnd by aligning d18O variability to SST variability

Linsley, B. K., Messier, R. G. and Dunbar, R. B.: Assessing between-colony oxygen isotope variability in the coral Porites lobata at Clipperton Atoll, Coral Reefs, 18(1), 13–27, doi:10.1007/s003380050148, 1999.

NOTED from downloading Swart1999 data, it is very different from Swart1996 even though the paper says it was the same coral, core, and data, not sure why, will have to contact Peter Swart to ask and look at Healy thesis. This coral species is Solenastrea bournoni, one not used in coral climate reconstructions, and it is located in a complex system of Florida Bay where waters from the Everglades enter the ocean and ther eare high rates of evaporation. The d18O system is not additive but subtractive for SSS and SST. Swart 1999 revisited this coral colony and they collect a new core from the same colony. Hudson 1989 gives a map with the coral location, which is 24degrees 55 minutes, and ~80 degrees and between 40 and 50 minutes, about 44 minutes nu my eye. Swart 1999 NOAA has different corrdinates for this coral 25 0N, 80 36W, Looking at Google earth and Hudsons map, the Swart 1999 corrdinates incorrect, they should be 24 degrees 55 minutes N, and ~80 degrees, 43.5 minutes W

This relationship between the d180 of the water (~w) and salinity is shown in Eqn. 2 and Fig. 2 (r = +0.71, n = 38, p > 0.05). Salinity = 4.98dw + 25.89 (2) Combining Eqns. (1) and (2), an expression (Eqn. 3) is derived expressing salinity in terms of the ~c and T. Salinity = 4.98delta18Ocoral + 1.18T + 19.62 (3) The confirmation of a positive correlation between salinity and the d180 (ffthe water (dw) seems to discount the notion that significant amounts of freshwater from Shark Slough, which is isotopically enriched in lsO (Meyers et al. 1993), is influencing the salinity of Lignumvitae Basin. If this water were influencing the salinity of Lignumvitae Basin then either an inverse correlation or no correlation at all would be expected between ~w and salinity.

Cores cores from the same study and a previous study Swart 1996, Swart 1999 NOAA has different corrdinates for this coral 25 0N, 80 36W, Looking at Google earth and Hudsons map, the Swart 1999 corrdinates incorrect, they should be 24 degrees 55 minutes N, and ~80 degrees, 43.5 minutes W. paper mentions a d18O record for FB-6 that was in a Masters thesis but only Ba/Ca is on NOAA website

10.2307/1353206, 10.1016/0031-0182(95)00078-X, 10.1016/0168-9622(91)90055-2

Swart, P. K., Healy, G., Greer, L., Lutz, M., Saied, A., Anderegg, D., Dodge, R. E. and Rudnick, D.: The Use of Proxy Chemical Records in Coral Skeletons to Ascertain Past Environmental Conditions in Florida Bay, Estuaries, 22(2), 384, doi:10.2307/1353206, 1999.

local precipitation isotope data confirm dDprecip is positively associated with temperature

Condensation temperature influence on isotopic distilation of continental moisture

local precipitation isotope data confirm d18Oprecip is positively associated with temperature

d-excess is influenced by evaporative boundary conditions at the moisture source (North Pacific)

Exclude from iso2k: Derived variable based on measured isotopes and assumptions of long-term changes in sea water

TP: Exclude from iso2k: Derived variable based on measured isotopes and assumptions of long-term changes in sea water

Reconstructed summer temperature anomalies expressed relative to the Holocene mean.

Exclude from iso2k: Derived variable based on measured isotopes and assumptions of long-term changes in sea water, and estimated local temperature-d18O sensitivity.

This is a composite record representing two permafrost cores from the DHP174 peatland (Dempster Highway peatland, near the 174 km marker), and covering the last 13.6 ka. This record is comparable in ways to an ice core, but different in that it accumulates below the surface and traps primarily summer precipitation. Likewise, the temperature reconstruction is linked to the summer season.

Recent summer warming in northwestern Canada exceeds the Holocene thermal maximum

Porter, T. J., Schoenemann, S. W., Davies, L. J., Steig, E. J., Bandara, S. and Froese, D. G.: Recent summer warming in northwestern Canada exceeds the Holocene thermal maximum, Nature Communications, 10(1), doi:10.1038/s41467-019-09622-y, 2019.

age model based on volcanic horizons and counting of annual layers (seasonal variations of stable isotopes)

The reference has been changed : Cole-Dai was not the isotope record, it's Moseley-Thompson. Added secondary reference of Masson 2000

spatial slope (Jouzel et al., 2003,Magnitude of isotope/temperature scaling for interpretation of central Antarctic ice cores  https://doi.org/10.1029/2002JD002677)

Precipitation weighted signal subject to post-depositional processes

Mosley-Thompson, E.: Holocene Climate Changes Recorded in an East Antarctica Ice Core, Climatic Variations and Forcing Mechanisms of the Last 2000 Years, 263–279, doi:10.1007/978-3-642-61113-1_13, 1996.

Masson, V., Vimeux, F., Jouzel, J., Morgan, V., Delmotte, M., Ciais, P., Hammer, C., Johnsen, S., Lipenkov, V. Y., Mosley-Thompson, E., Petit, J.-R., Steig, E. J., Stievenard, M. and Vaikmae, R.: Holocene Climate Variability in Antarctica Based on 11 Ice-Core Isotopic Records, Quaternary Research, 54(3), 348–358, doi:10.1006/qres.2000.2172, 2000.

; archiveType changed - was originally Ice core (IC); archiveType changed - was originally Ice core (IC)

based on counting of annual layers (seasonal variations of stable isotopes) and reference horizons

Dansgaard W. 1964. Stable isotopes in precipitation. Tellus 16: 436a€“468.

Eichler, A., Schwikowski, M., Gaeggeler, H. W., Furrer, V., Synal, H.-A., Beer, J., Saurer, M. and Funk, M.: Glaciochemical dating of an ice core from upper Grenzgletscher (4200 m a.s.l.), Journal of Glaciology, 46(154), 507–515, doi:10.3189/172756500781833098, 2000.

AO: fixed primary reference to Graf 2002, in accordance with Pangea

Graf et al., 2002 https://doi.org/10.3189/172756402781816492 DML spatial slope calibration

Graf, W., Oerter, H., Reinwarth, O., Stichler, W., Wilhelms, F., Miller, H. and Mulvaney, R.: Stable-isotope records from Dronning Maud Land, Antarctica, Annals of Glaciology, 35, 195–201, doi:10.3189/172756402781816492, 2002.

Oerter, H., Wilhelms, F., Jung-Rothenhaeusler, F., Goektas, F., Miller, H., Graf, W. and Sommer, S.: Accumulation rates in Dronning Maud Land, Antarctica, as revealed by dielectric-profiling measurements of shallow firn cores, Annals of Glaciology, 30, 27–34, doi:10.3189/172756400781820705, 2000.

Isaksson, E., van den Broeke, M. R., Winther, J.-G., Karloef, L., Francis Pinglot, J. and Gundestrup, N.: Accumulation and proxy-temperature variability in Dronning Maud Land, Antarctica, determined from shallow firn cores, Annals of Glaciology, 29, 17–22, doi:10.3189/172756499781821445, 1999.

Dansgaard W. 1964. Stable isotopes in precipitation. Tellus 16: 436?468.

WeiSSbach, S., Wegner, A., Opel, T., Oerter, H., Vinther, B. M. and Kipfstuhl, S.: Spatial and temporal oxygen isotope variability in northern Greenland –  implications for a new climate record over the past millennium, Climate of the Past, 12(2), 171–188, doi:10.5194/cp-12-171-2016, 2016.

isotope interpretation 1,2,3 is missing. -BK; TO: This is a duplicate of IC00SC1801A and can be deleted...

; archiveType changed  was originally Ice core (IC); archiveType changed  was originally Ice core (IC)

Stenni, B., Serra, F., Frezzotti, M., Maggi, V., Traversi, R., Becagli, S. and Udisti, R.: Snow accumulation rates in northern Victoria Land, Antarctica, by firn-core analysis, Journal of Glaciology, 46(155), 541–552, doi:10.3189/172756500781832774, 2000.

Steig, E. J., Morse, D. L., Waddington, E. D., Stuiver, M., Grootes, P. M., Mayewski, P. A., Twickler, M. S. and Whitlow, S. I.: Wisconsinan and holocene climate history from an ice core at taylor dome, western ross embayment, antarctica, Geografiska Annaler: Series A, Physical Geography, 82(2-3), 213–235, doi:10.1111/j.0435-3676.2000.00122.x, 2000.

age model based on beta activity and counting of annual layers (seasonal variations of stable isotopes)

correlation to meteorological data, ("...these data provide qualitative support for the hypothesis that temperature, not the amount effect, is the dominant process controlling d18O over the Tibetan Plateau.")

Yao, T., Thompson, L. G., Mosley-Thompson, E., Zhihong, Y., Xingping, Z., and Lin, P.-N.: 1996,Climatological Significance of I´18O in North Tibetan Ice Cores, J. Geophys. Res. 101, 29531a€“29537

isotope interpretation 1 field has an error (move to isotope interpretation 2?) - BK --> TO:corrected

Yao, T., Thompson, L. G., Mosley-Thompson, E., Zhihong, Y., Xingping, Z., and Lin, P.-N.: 1996,Climatological Significance of ?18O in North Tibetan Ice Cores, J. Geophys. Res. 101, 29531?29537

Thompson, L. G.: A High-Resolution Millennial Record of the South Asian Monsoon from Himalayan Ice Cores, Science, 289(5486), 1916–1919, doi:10.1126/science.289.5486.1916, 2000.

Jouzel, J., Masson, V., Cattani, O., Falourd, S., Stievenard, M., Stenni, B., Longinelli, A., Johnsen, S. J., Steffenssen, J. P., Petit, J. R., Schwander, J., Souchez, R. and Barkov, N. I.: A new 27 ky high resolution East Antarctic climate record, Geophysical Research Letters, 28(16), 3199–3202, doi:10.1029/2000gl012243, 2001.

age model based on reference horizons, counting of annual layers

volcanic and other reference horizons used to support the annual layer counting and the timescale

Mulvaney, R., Oerter, H., Peel, D. A., Graf, W., Arrowsmith, C., Pasteur, E. C., Knight, B., Littot, G. C. and Miners, W. D.: 1000 year ice-core records from Berkner Island, Antarctica, Annals of Glaciology, 35, 45–51, doi:10.3189/172756402781817176, 2002.

added interpretation, which is not the mean annual temperature, but not sure if I should delete all interpretation fields.

Schlosser 2002: "the observed variations in d18O cannot be explained using the emperature data. Factors other than temperature, such as changes in atmospheric circulation, must be involved."

Schlosser, E. and Oerter, H.: Shallow firn cores from Neumayer, Ekstroemisen, Antarctica: a comparison of accumulation rates and stable-isotope ratios, Annals of Glaciology, 35, 91–96, doi:10.3189/172756402781816915, 2002.

Stenni et al., 2002 : spatial correlation, A d18O temperature gradient of about 0.6permil/A°C was calculated between the two sites. This value is very close to the data reported by Lorius and Merlivat [1977] for present-day East Antarctic precipitation and by Stenni et al. [2000] for the Northern Victoria Land.

Stenni, B., Proposito, M., Gragnani, R., Flora, O., Jouzel, J., Falourd, S. and Frezzotti, M.: Eight centuries of volcanic signal and climate change at Talos Dome (East Antarctica), Journal of Geophysical Research: Atmospheres, 107(D9), ACL 3–1–ACL 3–13, doi:10.1029/2000jd000317, 2002.

chronology based on 36Cl reference horizon, wiggle matching, 14C dating and ice-flow modelling

Thompson, L. G.: Kilimanjaro Ice Core Records: Evidence of Holocene Climate Change in Tropical Africa, Science, 298(5593), 589–593, doi:10.1126/science.1073198, 2002.

chronology based on annual layer counting, volcanic and bomb reference horizons

Comparison with general circulation model results and meteorological data suggest that the Andean high altitude records are primarily controlled by precipitation variability over the Amazon basin.

Less (more) depletion of the water isotopes correlates well with anomalously dry (wet) conditions over the Amazon in agreement with the isotopic amount effect [Dansgaard, 1964]., Comparison with general circulation model results and meteorological data suggest that the Andean high altitude records are primarily controlled by precipitation variability over the Amazon basin."

Hoffmann, G., Ramirez, E., Taupin, J. D., Francou, B., Ribstein, P., Delmas, R., Duerr, H., Gallaire, R., Simoes, J., Schotterer, U., Stievenard, M. and Werner, M.: Coherent isotope history of Andean ice cores over the last century, Geophysical Research Letters, 30(4), doi:10.1029/2002gl014870, 2003.

based on volcanic horizons, beta activity and counting of annual layers (seasonal variations of stable isotopes)

Shugui, H., Dahe, Q., Dongqi, Z., Shichang, K., Mayewski, P. A. and Wake, C. P.: A 154a high-resolution ammonium record from the Rongbuk Glacier, north slope of Mt. Qomolangma (Everest), Tibet–Himal region, Atmospheric Environment, 37(5), 721–729, doi:10.1016/s1352-2310(02)00582-4, 2003.

data in supplements of 10.1038/nature10581 and 10.5194/cp-10-1605-2014

Fisher, D. A., Wake, C., Kreutz, K., Yalcin, K., Steig, E., Mayewski, P., Anderson, L., Zheng, J., Rupper, S., Zdanowicz, C., Demuth, M., Waszkiewicz, M., Dahl-Jensen, D., Goto-Azuma, K., Bourgeois, J. B., Koerner, R. M., Sekerka, J., Osterberg, E., Abbott, M. B., Finney, B. P. and Burns, S. J.: Stable Isotope Records from Mount Logan, Eclipse Ice Cores and Nearby Jellybean Lake. Water Cycle of the North Pacific Over 2000 Years and Over Five Vertical Kilometres: Sudden Shifts and Tropical Connections, Geographie physique et Quaternaire, 58(2-3), 337–352, doi:10.7202/013147ar, 2006.

Isaksson, E., Divine, D., Kohler, J., Martma, T., Pohjola, V., Motoyama, H. and Watanabe, O.: Climate oscillations as recorded in svalbard ice core ω18o records between ad 1200 and 1997, Geografiska Annaler: Series A, Physical Geography, 87(1), 203–214, doi:10.1111/j.0435-3676.2005.00253.x, 2005.

Isaksson, E., Kohler, J., Pohjola, V., Moore, J., Igarashi, M., Karloef, L., Martma, T., Meijer, H., Motoyama, H., Vaikmaee, R. and van de Wal, R. S. W.: Two ice-core δ18O records from Svalbard illustrating climate and sea-ice variability over the last 400 years, The Holocene, 15(4), 501–509, doi:10.1191/0959683605hl820rp, 2005.

Kaczmarska, M., Isaksson, E., Karloef, L., Winther, J.-G., Kohler, J., Godtliebsen, F., Olsen, L. R., Hofstede, C. M., Van Den Broeke, M. R., Van De Wal, R. S. W. and Gundestrup, N.: Accumulation variability derived from an ice core from coastal Dronning Maud Land, Antarctica, Annals of Glaciology, 39, 339–345, doi:10.3189/172756404781814186, 2004.

isotope interpretation 1 field has an error (move to isotope interpretation 2?) - BK --> TO: corrected

Thompson, L. G., Mosley-Thompson, E., Brecher, H., Davis, M., Leon, B., Les, D., Lin, P.-N., Mashiotta, T. and Mountain, K.: Abrupt tropical climate change: Past and present, Proceedings of the National Academy of Sciences, 103(28), 10536–10543, doi:10.1073/pnas.0603900103, 2006.

isotope interpretation 1 field has an error (move to isotope interpretation 2?) - BK

An abrupt warming (inferred from higher d18O values) occurred between 1910 and 1920 (Fig 6a and b)...

year start should not be a variable --> TO: This entry should be deleted

age model based on counting of annual layers (seasonal variations of dust and stable isotopes), beta activity and ice-flow modelling

Thompson, L. G., Tandong, Y., Davis, M. E., Mosley-Thompson, E., Mashiotta, T. A., Lin, P.-N., Mikhalenko, V. N. and Zagorodnov, V. S.: Holocene climate variability archived in the Puruogangri ice cap on the central Tibetan Plateau, Annals of Glaciology, 43, 61–69, doi:10.3189/172756406781812357, 2006.

Vinther, B. M., Clausen, H. B., Johnsen, S. J., Rasmussen, S. O., Andersen, K. K., Buchardt, S. L., Dahl-Jensen, D., Seierstad, I. K., Siggaard-Andersen, M.-L., Steffensen, J. P., Svensson, A., Olsen, J. and Heinemeier, J.: A synchronized dating of three Greenland ice cores throughout the Holocene, Journal of Geophysical Research, 111(D13), doi:10.1029/2005jd006921, 2006.

Our previous studies[10,19] have revealed that annual mean I´ 18O in the Malan ice core mainly reflects the summer temperature (high annual mean  I´ 18O value implies warm summer while low annual mean I´ 18O value means  cold summer), and its variation can ex-press the variations of summer temperatures in the large part of the northern Tibetan Plateau.

Tian, L., V. Masson-Delmotte, M. Stievenard, T. Yao and J. Jouzel.2001. Tibetan Plateau summer monsoon northward extent revealed by measurements of water stable isotopes.J. Geophys. Res., 106(D22), 28,081?28,088.

Wang, N., Yao, T., Pu, J., Zhang, Y. and Sun, W.: Climatic and environmental changes over the last millennium recorded in the Malan ice core from the northern Tibetan Plateau, Science in China Series D: Earth Sciences, 49(10), 1079–1089, doi:10.1007/s11430-006-1079-9, 2006.

10.1038/nature01525, 10.1038/nature06015, 10.1016/j.polar.2011.08.001, 10.5194/tcd-8-769-2014

Watanabe, O., Jouzel, J., Johnsen, S., Parrenin, F., Shoji, H. and Yoshida, N.: Homogeneous climate variability across East Antarctica over the past three glacial cycles, Nature, 422(6931), 509–512, doi:10.1038/nature01525, 2003.

Igarashi, M., Nakai, Y., Motizuki, Y., Takahashi, K., Motoyama, H. and Makishima, K.: Dating of the Dome Fuji shallow ice core based on a record of volcanic eruptions from AD 1260 to AD 2001, Polar Science, 5(4), 411–420, doi:10.1016/j.polar.2011.08.001, 2011.

This verifies that the amount effect acts as an important control on seasonal-decadal scale variations in the isotopic composition of Everest precipitation. More specifically, precipitation increases during periods of more intense convective activity, resulting in more negative dD. Variations in convective activity (i.e., amount effect) and moisture source region related to changes in atmospheric circulation are the dominant controls on the isotopic composition of precipitation in this region (see auxiliary material).

Kaspari, S., Mayewski, P., Kang, S., Sneed, S., Hou, S., Hooke, R., Kreutz, K., Introne, D., Handley, M., Maasch, K., Qin, D. and Ren, J.: Reduction in northward incursions of the South Asian monsoon since ∼1400 AD inferred from a Mt. Everest ice core, Geophysical Research Letters, 34(16), doi:10.1029/2007gl030440, 2007.

Sea surface temperature and humidity at the oceanic source region of the precipitation

Divine, D. V., Isaksson, E., Pohjola, V., Meijer, H., van de Wal, R. S. W., Martma, T., Moore, J., Sjoegren, B. and Godtliebsen, F.: Deuterium excess record from a small Arctic ice cap, Journal of Geophysical Research, 113(D19), doi:10.1029/2008jd010076, 2008.

AO: fixed year (2009) of original citation, and basis for isotope interpretation

We are using a temporal gradient of 0.5 A± 0.1 a€° per A°C to convert I´18O to temperature, based on the calibration between the I´18O with site temperatures from the European Centre for Medium Range Weather Forecasts (ECMWF) (1980a€“2005)

Thomas, E. R., Dennis, P. F., Bracegirdle, T. J. and Franzke, C.: Ice core evidence for significant 100-year regional warming on the Antarctic Peninsula, Geophysical Research Letters, 36(20), doi:10.1029/2009gl040104, 2009.

Thomas, E. R., Marshall, G. J. and McConnell, J. R.: A doubling in snow accumulation in the western Antarctic Peninsula since 1850, Geophysical Research Letters, 35(1), doi:10.1029/2007gl032529, 2008.

Vinther, B. M., Clausen, H. B., Fisher, D. A., Koerner, R. M., Johnsen, S. J., Andersen, K. K., Dahl-Jensen, D., Rasmussen, S. O., Steffensen, J. P. and Svensson, A. M.: Synchronizing ice cores from the Renland and Agassiz ice caps to the Greenland Ice Core Chronology, Journal of Geophysical Research, 113(D8), doi:10.1029/2007jd009143, 2008.

chronology based on annual layer counting, bomb reference horizon

Vimeux, F., de Angelis, M., Ginot, P., Magand, O., Casassa, G., Pouyaud, B., Falourd, S. and Johnsen, S.: A promising location in Patagonia for paleoclimate and paleoenvironmental reconstructions revealed by a shallow firn core from Monte San Valentin (Northern Patagonia Icefield, Chile), Journal of Geophysical Research, 113(D16), doi:10.1029/2007jd009502, 2008.

age model based on volcanic horizons, beta activity and counting of annual layers (seasonal variations of stable isotopes)

correlation to meteorological data: "A good correlation between 10-year averaged d18O data and Marcha€“November Barnaul temperatures was found (Figure S3, r = 0.83, p < 0.001 for the period 1850a€“1980), suggesting that d18O in precipitation at Belukha glacier is suitable as a proxy of atmospheric temperature, which is in good agreement with previous studies."

AraguaA´s-AraguaA´s, L., and K. FrA¶hlich (1998), Stable isotope composition of precipitation over southeast Asia, J. Geophys. Res., 103, 28,721a€“28,742.

Eichler, A., Olivier, S., Henderson, K., Laube, A., Beer, J., Papina, T., Gaeggeler, H. W. and Schwikowski, M.: Temperature response in the Altai region lags solar forcing, Geophysical Research Letters, 36(1), doi:10.1029/2008gl035930, 2009.

Fisher, D. A., Koerner, R. M. and Reeh, N.: Holocene climatic records from Agassiz Ice Cap, Ellesmere Island, NWT, Canada, The Holocene, 5(1), 19–24, doi:10.1177/095968369500500103, 1995.

Kaufman, D. S., Schneider, D. P., McKay, N. P., Ammann, C. M., Bradley, R. S., Briffa, K. R., Miller, G. H., Otto-Bliesner, B. L., Overpeck, J. T., Vinther, B. M., Abbott, M., Axford, Y., Bird, B., Birks, H. J. B., Bjune, A. E., Briner, J., Cook, T., Chipman, M., Francus, P., Gajewski, K., Geirsdottir, A., Hu, F. S., Kutchko, B., Lamoureux, S., Loso, M., MacDonald, G., Peros, M., Porinchu, D., Schiff, C., Seppa, H. and Thomas, E.: Recent Warming Reverses Long-Term Arctic Cooling, Science, 325(5945), 1236–1239, doi:10.1126/science.1173983, 2009.

age model based on volcanic horizons and counting of annual layers (seasonal variations of stable isotopes) GIC05 chronology from Vinther 2008

omitted since there's another Dye3 record that is longer, and not normalized

not a d18O record, furthermore there is a longer record available (IC13OPAN01A)

isotope interpretation1,2,3 is missing. -BK --> TO: corrected, but this record should be omitted

fraction of secondary regional moisture source related to regional sea-ice cover

Opel, T., Fritzsche, D., Meyer, H., Schuett, R., Weiler, K., Ruth, U., Wilhelms, F. and Fischer, H.: 115 year ice-core data from Akademii Nauk ice cap, Severnaya Zemlya: high-resolution record of Eurasian Arctic climate change, Journal of Glaciology, 55(189), 21–31, doi:10.3189/002214309788609029, 2009.

Vinther, B. M., Buchardt, S. L., Clausen, H. B., Dahl-Jensen, D., Johnsen, S. J., Fisher, D. A., Koerner, R. M., Raynaud, D., Lipenkov, V., Andersen, K. K., Blunier, T., Rasmussen, S. O., Steffensen, J. P. and Svensson, A. M.: Holocene thinning of the Greenland ice sheet, Nature, 461(7262), 385–388, doi:10.1038/nature08355, 2009.

Naik, S. S., Thamban, M., Laluraj, C. M., Redkar, B. L. and Chaturvedi, A.: A century of climate variability in central Dronning Maud Land, East Antarctica, and its relation to Southern Annular Mode and El Nino-Southern Oscillation, Journal of Geophysical Research, 115(D16), doi:10.1029/2009jd013268, 2010.

Vinther, B. M., Jones, P. D., Briffa, K. R., Clausen, H. B., Andersen, K. K., Dahl-Jensen, D. and Johnsen, S. J.: Climatic signals in multiple highly resolved stable isotope records from Greenland, Quaternary Science Reviews, 29(3-4), 522–538, doi:10.1016/j.quascirev.2009.11.002, 2010.

Climatic signals in multiple highly resolved stable isotope records from Greenland

spatial slope from Masson-Delmotte et al., 2008 adapted to the VLG site. "we chose the most local conversion slope from Taylor Dome I´D (4.0a€° per A°C) to provide an estimate for I”T." (Bertler et al., 2011)

Bertler, N. A. N., Mayewski, P. A. and Carter, L.: Cold conditions in Antarctica during the Little Ice Age — Implications for abrupt climate change mechanisms, Earth and Planetary Science Letters, 308(1-2), 41–51, doi:10.1016/j.epsl.2011.05.021, 2011.

Divine, D., Isaksson, E., Martma, T., Meijer, H. A. J., Moore, J., Pohjola, V., van de Wal, R. S. W. and Godtliebsen, F.: Thousand years of winter surface air temperature variations in Svalbard and northern Norway reconstructed from ice-core data, Polar Research, 30(1), 7379, doi:10.3402/polar.v30i0.7379, 2011.

Kinnard, C., Zdanowicz, C. M., Fisher, D. A., Isaksson, E., de Vernal, A. and Thompson, L. G.: Reconstructed changes in Arctic sea ice over the past 1,450 years, Nature, 479(7374), 509–512, doi:10.1038/nature10581, 2011.

AO: fixed publi DOI; no isotope interpretation in the publication, and no altitude given either. TP added elevation

Laluraj, C. M., Thamban, M., Naik, S. S., Redkar, B. L., Chaturvedi, A. and Ravindra, R.: Nitrate records of a shallow ice core from East Antarctica: Atmospheric processes, preservation and climatic implications, The Holocene, 21(2), 351–356, doi:10.1177/0959683610374886, 2010.

counting of annual layers (seasonal variations of stable isotopes and major ions) and beta activity

In central Asia, the firsta€order control on seasonal d18O variability is temperature [AraguA¡sa€AraguA¡s et al., 1998]. A high correlation between temperature and precipitation d18O was found for eastern Tien Shan [Hou et al., 1999]. Accordingly, sections of lower d18O values along the core are interpreted as precipitation falling during cold winter seasons and those with higher d18O values, as precipitation falling during warm summer seasons."

Liu, Y., Hou, S., Hong, S., Hur, S. D., Lee, K. and Wang, Y.: High-resolution trace element records of an ice core from the eastern Tien Shan, central Asia, since 1953 AD, Journal of Geophysical Research, 116(D12), doi:10.1029/2010jd015191, 2011.

A d18O temperature gradient of about 0.6permil/A°C was calculated between the two sites. (Stenni et al., 2002)

Stenni, B., Buiron, D., Frezzotti, M., Albani, S., Barbante, C., Bard, E., Barnola, J. M., Baroni, M., Baumgartner, M., Bonazza, M., Capron, E., Castellano, E., Chappellaz, J., Delmonte, B., Falourd, S., Genoni, L., Iacumin, P., Jouzel, J., Kipfstuhl, S., Landais, A., Lemieux-Dudon, B., Maggi, V., Masson-Delmotte, V., Mazzola, C., Minster, B., Montagnat, M., Mulvaney, R., Narcisi, B., Oerter, H., Parrenin, F., Petit, J. R., Ritz, C., Scarchilli, C., Schilt, A., Schuepbach, S., Schwander, J., Selmo, E., Severi, M., Stocker, T. F. and Udisti, R.: Expression of the bipolar see-saw in Antarctic climate records during the last deglaciation, Nature Geoscience, 4(1), 46–49, doi:10.1038/ngeo1026, 2010.

Severi, M., Udisti, R., Becagli, S., Stenni, B. and Traversi, R.: Volcanic synchronisation of the EPICA-DC and TALDICE ice cores for the last 42 kyr BP, Climate of the Past, 8(2), 509–517, doi:10.5194/cp-8-509-2012, 2012.

correlation to meteorological data, ERA-Interim reanalyses, and spatial slope from Masson-Delmotte et al., 2008.

Temperature anomalies were calculated using a I´Da€“temperature dependence of 6.4a€‰A±a€‰1.3a€°a€‰A°Caˆ’1 (Abram et al. 2011), under the assumption that the modern-day calibration holds over the entire record26, and are given with reference to ada€‰1961a€“1990.

Mulvaney, R., Abram, N. J., Hindmarsh, R. C. A., Arrowsmith, C., Fleet, L., Triest, J., Sime, L. C., Alemany, O. and Foord, S.: Recent Antarctic Peninsula warming relative to Holocene climate and ice-shelf history, Nature, 489(7414), 141–144, doi:10.1038/nature11391, 2012.

Abram, N. J., Mulvaney, R., Wolff, E. W., Triest, J., Kipfstuhl, S., Trusel, L. D., Vimeux, F., Fleet, L. and Arrowsmith, C.: Acceleration of snow melt in an Antarctic Peninsula ice core during the twentieth century, Nature Geoscience, 6(5), 404–411, doi:10.1038/ngeo1787, 2013.

age model based on volcanic horizons and counting of annual layers (seasonal variations of stable isotopes and impurities)

We employ the Taylor Dome I´-borehole temperature calibration of 4A±1.5 a€°I´D perA°C(Steig et al., 1998).

Rhodes, R. H., Bertler, N. A. N., Baker, J. A., Steen-Larsen, H. C., Sneed, S. B., Morgenstern, U. and Johnsen, S. J.: Little Ice Age climate and oceanic conditions of the Ross Sea, Antarctica from a coastal ice core record, Climate of the Past, 8(4), 1223–1238, doi:10.5194/cp-8-1223-2012, 2012.

AO: added isotope interpretation, fixed DOI which was pointing to the wrong paper

Using ECMWF Interim Re-Analysis (ERA-Interim) data, this study develops a precipitation-weighted I´18O-temperature transfer function of 0.62a€° A°Caˆ’1, which is comparable to other proximal ice cores, such as Taylor, Talos, and Law Domes.

Sinclair, K. E., Bertler, N. A. N. and van Ommen, T. D.: Twentieth-Century Surface Temperature Trends in the Western Ross Sea, Antarctica: Evidence from a High-Resolution Ice Core, Journal of Climate, 25(10), 3629–3636, doi:10.1175/jcli-d-11-00496.1, 2012.

Wagenbach, D., Bohleber, P. and Preunkert, S.: Cold, alpine ice bodies revisited: what may we learn from their impurity and isotope content?, Geografiska Annaler: Series A, Physical Geography, 94(2), 245–263, doi:10.1111/j.1468-0459.2012.00461.x, 2012.

based on counting of annual layers (major ions) and reference horizons (Tritium, Saharan dust and volcanic)

Bohleber, P., Wagenbach, D., Schoener, W. and Boehm, R.: To what extent do water isotope records from low accumulation Alpine ice cores reproduce instrumental temperature series?, Tellus B: Chemical and Physical Meteorology, 65(1), 20148, doi:10.3402/tellusb.v65i0.20148, 2013.

Opel, T., Fritzsche, D. and Meyer, H.: Eurasian Arctic climate over the past millennium as recorded in the Akademii Nauk ice core (Severnaya Zemlya), Climate of the Past, 9(5), 2379–2389, doi:10.5194/cp-9-2379-2013, 2013.

Morgan, V. I., Wookey, C. W., Li, J., van Ommen, T. D., Skinner, W. and Fitzpatrick,  Μ. F.: Site information and initial results from deep ice drilling on Law Dome, Antarctica, Journal of Glaciology, 43(143), 3–10, doi:10.3189/s0022143000002768, 1997.

Morgan, V. and van Ommen, T. D.: Seasonality in late-Holocene climate from ice-core records, The Holocene, 7(3), 351–354, doi:10.1177/095968369700700312, 1997.

Steig et al. 2013 suppl: Scaling between I´18O and temperature in West Antarctica can be estimated in a number of ways, all yielding similar results.  The local interannual scaling between WAIS Divide I´18O and Byrd temperature is 0.5a€°/A°C; the ratio of 50-year trends also yields 0.5a€°/A°C (1957-2006, Byrd temperature trend7 = 0.48A°C/decade; WAIS Divide I´18O trend = 0.24a€°/decade).  Regional interannual scaling between the composite I´18O series in Figure 1 and the West-Antarctic average temperature from Steig et al.4 is also 0.5a€°/A°C; the ratio of 50-year trends is 0.6a€°/A°C (1957-2006, West Antarctic temperature trend = 0.19A°C/decade4; composite I´18O trend = 0.12a€°/decade).  Comparison betweenI´18O and the borehole temperature reconstruction from WAIS Divide6 over the last 2000 years also results in similar scaling. See also Kuttel et al, 2012 for more interpretation

Steig, E. J., Ding, Q., White, J. W. C., Kuettel, M., Rupper, S. B., Neumann, T. A., Neff, P. D., Gallant, A. J. E., Mayewski, P. A., Taylor, K. C., Hoffmann, G., Dixon, D. A., Schoenemann, S. W., Markle, B. R., Fudge, T. J., Schneider, D. P., Schauer, A. J., Teel, R. P., Vaughn, B. H., Burgener, L., Williams, J. and Korotkikh, E.: Recent climate and ice-sheet changes in West Antarctica compared with the past 2,000 years, Nature Geoscience, 6(5), 372–375, doi:10.1038/ngeo1778, 2013.

Kuettel, M., Steig, E. J., Ding, Q., Monaghan, A. J. and Battisti, D. S.: Seasonal climate information preserved in West Antarctic ice core water isotopes: relationships to temperature, large-scale circulation, and sea ice, Climate Dynamics, 39(7-8), 1841–1857, doi:10.1007/s00382-012-1460-7, 2012.

AO: added isotope interpretation. Isotope interpretation is tied to atmospheric circulation, should we change the primary interpretation field?

The F10 record is significantly correlated (r = 0.44, P = 0.01) with ERA-Interim temperature (t850, 1979a€“2009), and we observe that the pattern of corre- lation with atmospheric pressure and sea surface tempera- tures (SSTs) is similar for both observational I´D and local temperature from reanalysis; however, we do not assume that I´D is a quantitative temperature proxy.

Thomas, E. R., Bracegirdle, T. J., Turner, J. and Wolff, E. W.: A 308 year record of climate variability in West Antarctica, Geophysical Research Letters, 40(20), 5492–5496, doi:10.1002/2013gl057782, 2013.

; paleoData_variableName changed - was originally d18OiceSMOW; paleoData_units changed - was originally per mil SMOW; climateInterpretation_seasonality changed - was originally austral winter; archiveType changed - was originally ice core

Three-year running mean significantly correlated to SST Nino 4 region

There is no significant relationship between stable isotopes and precipitation (net accumulation) on the Quelccaya ice cap. In other words, the precipitation “amount effect” does not appear to govern the stable isotopic chemistry on this tropical glacier. Because 70 to 80% of the precipitation falling on Quelccaya arrives during the wet season, the δ18O history reflects primarily conditions during austral summer. Decadal averages of precipitation amount and δ18O are not strongly related

; paleoData_variableName changed - was originally iceacc_m; paleoData_units changed - was originally meters water equivalent

Thompson, L. G.;Mosley-Thompson, E.;Davis, M. E.;Zagorodnov, V. S.;Howat, I. M.;Mikhalenko, V. N.;Lin, P.- N.

Annually resolved ice core records of tropical climate variability over the past 1800 years

Thompson, L. G., Mosley-Thompson, E., Davis, M. E., Zagorodnov, V. S., Howat, I. M., Mikhalenko, V. N. and Lin, P.-N.: Annually Resolved Ice Core Records of Tropical Climate Variability over the Past  1800 Years, Science, 340(6135), 945–950, doi:10.1126/science.1234210, 2013.

Ekaykin et al., 2014. VRS13 is correlated with the local instrumentally measured near-surface air temperature data for the period1958a€“2010. Surprisingly, VRS13 is much more consistent with the temperature of the warm period of the year (Novembera€“January), with a correlation coefficient of 0.57.

Ekaykin, A. A., Kozachek, A. V., Lipenkov, V. Y. and Shibaev, Y. A.: Multiple climate shifts in the Southern Hemisphere over the past three centuries based on central Antarctic snow pits and core studies, Annals of Glaciology, 55(66), 259–266, doi:10.3189/2014aog66a189, 2014.

Ekaykin, A. A., Vladimirova, D. O., Lipenkov, V. Y. and Masson-Delmotte, V.: Climatic variability in Princess Elizabeth Land (East Antarctica) overthe last 350 years, , doi:10.5194/cp-2016-76, 2016.

Vostok composite VRS13 ( a stack of 15 individual isotopic records from snow pits and shallow cores recovered in the vicinity of Vostok Station)

Mariani, I., Eichler, A., Jenk, T. M., Broennimann, S., Auchmann, R., Leuenberger, M. C. and Schwikowski, M.: Temperature and precipitation signal in two Alpine ice cores over the period 1961&ndash;2001, Climate of the Past, 10(3), 1093–1108, doi:10.5194/cp-10-1093-2014, 2014.

Ekaykin et al., 2017. The apparent isotopea€“temperature gradient, obtained as a standard deviation of isotopic values divided by standard deviations of temperature values, is 13.8A±2.5 permil/A°C.

isotope interpretation1,2,3 is missing. -BK --> TO: Record should be omitted anyway.

Gao, J., Risi, C., Masson-Delmotte, V., He, Y. and Xu, B.: Southern Tibetan Plateau ice core δ18O reflects abrupt shifts in atmospheric circulation in the late 1970s, Climate Dynamics, 46(1-2), 291–302, doi:10.1007/s00382-015-2584-3, 2015.

Masson-Delmotte, V., Steen-Larsen, H. C., Ortega, P., Swingedouw, D., Popp, T., Vinther, B. M., Oerter, H., Sveinbjornsdottir, A. E., Gudlaugsdottir, H., Box, J. E., Falourd, S., Fettweis, X., Gallee, H., Garnier, E., Gkinis, V., Jouzel, J., Landais, A., Minster, B., Paradis, N., Orsi, A., Risi, C., Werner, M. and White, J. W. C.: Recent changes in north-west Greenland climate documented by NEEM shallow ice core data and simulations, and implications for past-temperature reconstructions, The Cryosphere, 9(4), 1481–1504, doi:10.5194/tc-9-1481-2015, 2015.

age model based on volcanic horizons and counting of annual layers (seasonal variations of MSA)

Goodwin, B. P., Mosley-Thompson, E., Wilson, A. B., Porter, S. E. and Sierra-Hernandez, M. R.: Accumulation Variability in the Antarctic Peninsula: The Role of Large-Scale Atmospheric Oscillations and Their Interactions, Journal of Climate, 29(7), 2579–2596, doi:10.1175/jcli-d-15-0354.1, 2016.

DVD: a stack of North Greenland Traverse d18O records (BXX cores)

From the comparison between RICE I´Do and ERAi SAT records, we obtain a temporal slope of 3.37 permil/A°C

Bertler, N. A. N., Conway, H., Dahl-Jensen, D., Emanuelsson, D. B., Winstrup, M., Vallelonga, P. T., Lee, J. E., Brook, E. J., Severinghaus, J. P., Fudge, T. J., Keller, E. D., Baisden, W. T., Hindmarsh, R. C. A., Neff, P. D., Blunier, T., Edwards, R., Mayewski, P. A., Kipfstuhl, S., Buizert, C., Canessa, S., Dadic, R., Kjaer, H. A., Kurbatov, A., Zhang, D., Waddington, E. D., Baccolo, G., Beers, T., Brightley, H. J., Carter, L., Clemens-Sewall, D., Ciobanu, V. G., Delmonte, B., Eling, L., Ellis, A., Ganesh, S., Golledge, N. R., Haines, S., Handley, M., Hawley, R. L., Hogan, C. M., Johnson, K. M., Korotkikh, E., Lowry, D. P., Mandeno, D., McKay, R. M., Menking, J. A., Naish, T. R., Noerling, C., Ollive, A., Orsi, A., Proemse, B. C., Pyne, A. R., Pyne, R. L., Renwick, J., Scherer, R. P., Semper, S., Simonsen, M., Sneed, S. B., Steig, E. J., Tuohy, A., Venugopal, A. U., Valero-Delgado, F., Venkatesh, J., Wang, F., Wang, S., Winski, D. A., Winton, V. H. L., Whiteford, A., Xiao, C., Yang, J. and Zhang, X.: The Ross Sea Dipole – temperature, snow accumulation and sea ice variability in the Ross Sea region, Antarctica,  over the past 2700 years, Climate of the Past, 14(2), 193–214, doi:10.5194/cp-14-193-2018, 2018.

based on counting of annual layers (stable isotopes, major ions)

In the warm season (Maya€“October) the isotopic composition depends on local temperatures, but the correlation is not persistent over time, while in the cold season (Novembera€“April), atmospheric circulation is the predominant driver of the ice corea€™s isotopic composition.

In the summer season the isotopic composition depends on the local temperature, while in winter, the atmospheric circulation is the predominant driver of the ice core isotopic composition.

So far, no regional or large-scale climate signal could be identified in Elbrus deuterium excess.

Kozachek, A., Mikhalenko, V., Masson-Delmotte, V., Ekaykin, A., Ginot, P., Kutuzov, S., Legrand, M., Lipenkov, V. and Preunkert, S.: Large-scale drivers of Caucasus climate variability in meteorological records and Mt El’brus ice cores, Climate of the Past, 13(5), 473–489, doi:10.5194/cp-13-473-2017, 2017.

DVD: 2K record; 2 years shift in chrono relative to https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/polar/devon/d7273del_5yr.txt

DVD: annual series from https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/polar/devon/d73del_1yr.txt

Fisher, D. A., Koerner, R. M., Paterson, W. S. B., Dansgaard, W., Gundestrup, N. and Reeh, N.: Effect of wind scouring on climatic records from ice-core oxygen-isotope profiles, Nature, 301(5897), 205–209, doi:10.1038/301205a0, 1983.

based on counting of annual layers (seasonal variations of stable isotopes)

This annual variation of the isotope content of precipitation usually remains detectable in snow covers (Moser and Stichler, 1975).

These results indicate that besides the general enrichment of the stable isotopes 2H and 180 during ablation (melting and evaporation), the deuterium excess d decreases. These effects can be used to identify those snow layers exposed at the glacier surface during summer time.

DVD: data from https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/greenland/gisp/dye2/dye2ad77.txt

Langway, C. C., Oeschger, H. and Dansgaard, W., Eds.: Greenland Ice Core: Geophysics, Geochemistry, and the Environment, Geophysical Monograph Series, doi:10.1029/gm033, 1985.

age model based on  volcanic horizons and beta activity peaks as reference horizons, annual layers and flow modelling

DVD: data from https://doi.pangaea.de/10.1594/PANGAEA.56088?format=html#download

TO: This should be high-res (sub-annual) values of IC93BAGI01A but apparently something went wrong in the datatable

Barlow, L. K., White, J. W. C., Barry, R. G., Rogers, J. C. and Grootes, P. M.: The North Atlantic Oscillation signature in deuterium and deuterium excess signals in the Greenland Ice Sheet Project 2 Ice Core, 1840-1970, Geophysical Research Letters, 20(24), 2901–2904, doi:10.1029/93gl03305, 1993.

age model based on volcanic horizons and counting of annual layers (seasonal variations of stable isotopes and SO4)

AO: added isotope interpretation, doi and chronology information. TP added elevation

Thompson, L. G., Peel, D. A., Mosley-thompson, E., Mulvaney, R., Dal, J., Lin, P. N., Davis, M. E. and Raymond, C. F.: Climate since AD 1510 on Dyer Plateau, Antarctic Peninsula: evidence for recent climate change, Annals of Glaciology, 20, 420–426, doi:10.3189/1994aog20-1-420-426, 1994.

DVD: data from https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/polar/agassiz/a87del18_1yr.txt  ; corrected coordinates

Correlation with nearby Halley Station meteorological data 5thompson et al, 1994, fig 4)

chronology based on annual layer counting, 36Cl reference horizon, and ice-flow modelling

thermal year (Aug-Jul) (but 80% of precipitation from Nov to May)

Simple d18O-temperature relations used in polar regions (30), when applied to the d18O decrease of 8 per mil in LGS ice on Huascaran, suggest that air temperatures may have been lower by as much as 8A° to 12A°C at high elevation in the tropics.

annual  (thermal year (Aug-Jul), but 80% of precipitation from Nov to May)

Thompson, L. G., Mosley-Thompson, E., Davis, M. E., Lin, P.-N., Henderson, K. A., Cole-Dai, J., Bolzan, J. F. and Liu, K. -b.: Late Glacial Stage and Holocene Tropical Ice Core Records from Huascaran, Peru, Science, 269(5220), 46–50, doi:10.1126/science.269.5220.46, 1995.

age model based on counting of annual layers (seasonal variations of stable isotopes and ECM)

AO: added isotope interpretation, doi and chronology information

Spatial correlation between mean d18O and borehole 10-m temperatures (Lorius and Merlivat 1977)

We have determined a  gradient of 1.16 permil/A°C for this area based on a linear regression with the mean d18O and borehole 10-m temperature. (Isaksson and Karlen, Clim.Changes, 1994)

Isaksson, E., Karlen, W., Gundestrup, N., Mayewski, P., Whitlow, S. and Twickler, M.: A century of accumulation and temperature changes in Dronning Maud Land, Antarctica, Journal of Geophysical Research: Atmospheres, 101(D3), 7085–7094, doi:10.1029/95jd03232, 1996.

AO: changed primary reference from 1996 to 1990. added DOI, added isotope interpretation

Comparison with meteorological stations. No quantification attempted. "For the purpose of this paper the d18O is assumed to provide a proxy history for the condensation temperature of Siple precipitation."

Mosley-Thompson, E., Thompson, L. G., Grootes, P. M. and Gundestrup, N.: Little Ice Age (Neoglacial) Paleoenvironmental Conditions At Siple Station, Antarctica, Annals of Glaciology, 14, 199–204, doi:10.3189/s0260305500008570, 1990.

DVD: data from https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/greenland/summit/gisp2/isotopes/d18o1yr.txt

Grootes, P. M. and Stuiver, M.: Oxygen 18/16 variability in Greenland snow and ice with 10−3- to 105-year time resolution, Journal of Geophysical Research: Oceans, 102(C12), 26455–26470, doi:10.1029/97jc00880, 1997.

Thompson, L. G.: Tropical Climate Instability: The Last Glacial Cycle from a Qinghai-Tibetan Ice Core, Science, 276(5320), 1821–1825, doi:10.1126/science.276.5320.1821, 1997.

DVD: data from https://www1.ncdc.noaa.gov/pub/data/paleo/icecore/polar/penny/penny95/d18o/del25ysg_954.txt

Fisher, D. A., Koerner, R. M., Bourgeois, J. C., Zielinski, G., Wake, C., Hammer, C. U., Clausen, H. B., Gundestrup, N., Johnsen, S., Goto-Azuma, K., Hondoh, T., Blake, E. and Gerasimoff, M.: Penny Ice Cap Cores, Baffin Island, Canada, and the Wisconsinan Foxe Dome Connection: Two States of Hudson Bay Ice Cover, Science, 279(5351), 692–695, doi:10.1126/science.279.5351.692, 1998.

chronology based on annual layer counting, volcanic reference horizon, 14C dating and matching to GISP2 ice core

Thompson, L. G.: A 25,000-Year Tropical Climate History from Bolivian Ice Cores, Science, 282(5395), 1858–1864, doi:10.1126/science.282.5395.1858, 1998.

The gradient for this area is 0.73 permil/A°C (R2=0.98), which is very close to the gradient of 0.75 permil/A°C proposed for East Antarctica by Lorius and Merlivat (1977).

Oerter, H., Graf, W., Wilhelms, F., Minikin, A. and Miller, H.: Accumulation studies on Amundsenisen, Dronning Maud Land, Antarctica, by means of tritium, dielectric profiling and stable-isotope measurements: first results from the 1995–96 and 1996–97 field seasons, Annals of Glaciology, 29, 1–9, doi:10.3189/172756499781820914, 1999.

On the basis of a d18O/temperature relation for event-based samples from Jungfraujoch and equally sliced ice core segments from Fiescherhorn for the years 1983/1984 [Schotterer et al., 1997], winter snow (months December, January, February, and March) was defined as snow with d18O< -19permill and summer snow was defined as that with d18O > -15A¸permill (months June, July, August, and September).

In winter the d18O also shows the most negative values because the temperatures during snow formation are lowest

Schwikowski, M., Bruetsch, S., Gaeggeler, H. W. and Schotterer, U.: A high-resolution air chemistry record from an Alpine ice core: Fiescherhorn glacier, Swiss Alps, Journal of Geophysical Research: Atmospheres, 104(D11), 13709–13719, doi:10.1029/1998jd100112, 1999.

; archiveType changed - was originally Ice Wedge (IW); archiveType changed - was originally Ice Wedge (IW)

However, both observations and isotope modelling results indicate that temperature is the primary control on 18O in the study region (Supplementary Information).

Meyer, H., Opel, T., Laepple, T., Dereviagin, A. Y., Hoffmann, K. and Werner, M.: Long-term winter warming trend in the Siberian Arctic during the mid- to late Holocene, Nature Geoscience, 8(2), 122–125, doi:10.1038/ngeo2349, 2015.

Suggest changing isotope interpretation 1 to "P_isotope" and making isotope interpretation 2 = "postdepositional processes", TO: I changed isotope interpretation 1, but omitted postdeposional processes as isotope interpretation 2 as this is true for all records and archives

Opel, T., Laepple, T., Meyer, H., Dereviagin, A. Y. and Wetterich, S.: Northeast Siberian ice wedges confirm Arctic winter warming over the past two millennia, The Holocene, 27(11), 1789–1796, doi:10.1177/0959683617702229, 2017.

model used to convert 210Pb activity to age (e.g., constant rate of supply)

years before 1950 (calibrated age, or ages that dont need calibration)

Seltzer, G., Rodbell, D. and Burns, S.: Isotopic evidence for late Quaternary climatic change in tropical South America, Geology, 28(1), 35, doi:10.1130/0091-7613(2000)28<35:ieflqc>2.0.co;2, 2000.

solvent extraction, bleaching, and alkaline hydrolysis, removed noncellulose organic components

18O of lake water largey controled by 18O of precip, which is attributed primarly to air temperature. The d18OP profiles have been reconstructed from a combination of: (1) estimated changes in MAT during the early to mid-Holocene assuming the modern relation 0.59? d18OP/i¿½C; (2) mid-Holocene paleo-d18OP inferred from peat porewater (described above); (3) minimum d18Olw values during the mid- to late Holocene at Middendorf and Dolgoe Lakes, which likely reflect values that have not been strongly influenced by evaporation; and (4) modern estimated d18OP for each site.

Effects of evaporative related to circulation are secondary influence on hydrological balance

regions plot close to the global meteoric water line of Craig 1961;d2H= 8 d18O + 10)

Wolfe, B., Edwards, T., Aravena, R., Forman, S., Warner, B., Velichko, A., & MacDonald, G.

<jats:title>Abstract</jats:title>
            <jats:p>Lake-water oxygen-isotope histories for three lakes in northern Russia, derived from the cellulose oxygen-isotope stratigraphies of sediment cores, provide the basis for preliminary reconstruction of Holocene paleohydrology in two regions along the boreal treeline. Deconvolution of shifting precipitation δ<jats:sup>18</jats:sup>O from secondary evaporative isotopic enrichment is aided by knowledge of the distribution of isotopes in modern precipitation, the isotopic composition of paleo-waters preserved in frozen peat deposits, as well as other supporting paleoclimatic information. These data indicate that during the early Holocene, when the boreal treeline advanced to the current arctic coastline, conditions in the lower Yenisey River region were moist compared to the present, whereas greater aridity prevailed to the east near the lower Lena River. This longitudinal moisture gradient is consistent with the suggestion that oceanic forcing (increased sea-surface temperatures in the Nordic Seas and reduced sea-ice cover) was a major contributor to the development of a more maritime climate in western Eurasia, in addition to increased summer insolation. East of the Taimyr Peninsula, large tracts of the continental shelf exposed by glacial sea-level drawdown may have suppressed maritime climatic influence in what are now coastal areas. In contrast, during the late Holocene the two regions have apparently experienced coherent shifts in effective moisture. The similarity of the records may primarily reflect reduced North Atlantic influence in the Nordic Seas and southward retreat of coastline in eastern Siberia, coupled with declining summer insolation.</jats:p>

Holocene Paleohydrology and Paleoclimate at Treeline, North-Central Russia, Inferred from Oxygen Isotope Records in Lake Sediment Cellulose

Wolfe, B. B., Edwards, T. W. D., Aravena, R., Forman, S. L., Warner, B. G., Velichko, A. A. and MacDonald, G. M.: Holocene Paleohydrology and Paleoclimate at Treeline, North-Central Russia, Inferred from Oxygen Isotope Records in Lake Sediment Cellulose, Quaternary Research, 53(3), 319–329, doi:10.1006/qres.2000.2124, 2000.

Kiel III carbonate preparation device interfaced with a Finnigan MAT 252 mass spectrometer

About 10 to 15 specimens were selected from each 1cm sample. Each shell was cracked open and sonicated in methanol to remove degreesnegrained particles that degreesll the chambers. Cleaned shell fragments were treated with 15% H2O2 for 1 hour to remove organic matter, dried, and ground to a homogenous powder.

The d18O record from Chichancanab generally supports our E/P inferences based on the S record

Hodell, D. A.: Solar Forcing of Drought Frequency in the Maya Lowlands, Science, 292(5520), 1367–1370, doi:10.1126/science.1057759, 2001.

Hypothesised that deep lake temperatures dont change, as recorded by benthic ostracods Thus difference between ostracods and authigenic carbonate relates to temperature

Although evaporation could potentially cause more 18O enrichment in surface water than in bottom water of a lake, this factor is likely negligible at Farewell Lake, because the lake has a large volume (maximum depth of the south basin: 55 m; surface area: 4 km2) and because no major moisture deficit exists in the region. This argument is supported by the fact that the 18O values (12.2?12.5?) of water samples taken weekly from the lake surface during July 19?September 25, 2000, show no time-dependent trend. 18Oac reflects changes in atmospheric temperature, as abiotic carbonate precipitation occurs in surface water, where the temperature fluctuates in response to atmospheric temperature changes (19). In contrast, because Farewell Lake is deep and has a large water volume, the bottom-water temperature likely remains constant at 4i¿½C, as it was in June 1990 and July 2000, based on field measurements. Therefore, the deviation of 18Oac from contemporaneous 18Obo results from oxygen-isotope frac- tionation induced by the temperature difference between sur- face and bottom waters after accounting for any vital effects.

deltaT = [(d18Oac - d18Obo)past - (d18Oac - d18Obo)modern]/-0.25

Hu, F. S. , Ito, E. , Brown, T. A. , Curry, B. B. , Engstrom, D. R.

Pronounced climatic variations in Alaska during the last two millennia

Hu, F. S., Ito, E., Brown, T. A., Curry, B. B. and Engstrom, D. R.: Pronounced climatic variations in Alaska during the last two millennia, Proceedings of the National Academy of Sciences, 98(19), 10552–10556, doi:10.1073/pnas.181333798, 2001.

Prior to TIC and d18O analyses, each sample was combined withdeionize d water, shaken and centrifuged for 15 min at 20,000 rpm using a Sorval Superspeed RC2B.1 After centrifugation, the conductivity of the supernatant was measured and the supernatant discarded. This procedure was repeated until the conductivity of the supernatant was o3 times the conductivity of Boulder, Colorado, tap water. The sample was then freeze dried and homogenized with a mortar and pestle.

Continuous, high-resolution d18O records from cored sediments of Pyramid Lake, Nevada, indicate that oscillations in the hydrologic balance occurred. When drought occurs in the Sierra Nevada, the flow of the Truckee River is reduced and Pyramid Lake falls or the amount of overflow to Winnemucca Lake basin decreases. This results in increasing d18O values of lake water. For the purposes of this paper, we define ??hydrologic droughts?? as periods during which Dd18O=Dt tends to be positive; that is, times when lake volume (or spill rate) decreases.

There are two principal sources of d18Oin to Pyramid Lake: Sierran snowmelt and Lake Tahoe overflow.Evaporation from Lake Tahoe has resulted in a d18O value (5.6m) much larger than that of snowmelt (14.6m). Thus, during droughts when Lake Fig. 19. Plot of TOC, d13C and d18O data from PLB98-2 (solid lines) and the top of PLC97-1 (dashed lines) indicating overlap of cores. 670 L. Benson et al. / Quaternary Science Reviews 21 (2002) 659?682 Tahoe ceases spilling, the d18O value of Truckee River discharge decreases from B11m to B14.6m. Th e input of 14.6m water to Pyramid lake causes its d18O value to first increase as its volume decreases; however, its steady-state value (1.6m) is much smaller than when the lake receives spill from Lake Tahoe.

Benson, Larry , Kashgarian, Michaele , Rye, Robert , Lund, Steve , Paillet, Fred , Smoot, Joseph , Kester, Cynthia , Mensing, Scott , Meko, Dave , Lindstri¿½m, Susan

Holocene multidecadal and multicentennial droughts affecting Northern California and Nevada

Benson, L., Kashgarian, M., Rye, R., Lund, S., Paillet, F., Smoot, J., Kester, C., Mensing, S., Meko, D. and Lindstroem, S.: Holocene multidecadal and multicentennial droughts affecting Northern California and Nevada, Quaternary Science Reviews, 21(4-6), 659–682, doi:10.1016/s0277-3791(01)00048-8, 2002.

stronger zonal atmospheric circulation during the early Holocene remains the most plausable mechanism to explain the strong shifts in the d18O-MAT relation. Temperature equation applied to surface sediment yields essentially modern July temperatures|lake water d18O corresponds with pollen-inferred temperatures.

the water body is affected by a well-developed evaporative isotopic enrichment in spite ofthe rather short residence time (ca 20 days or less) as estimated from catchment size and meteorological data. Surface run-off from the catchment and direct precipitation seems to have no major impact on the isotopic composition oflake water during the ice-free season; groundwater level and related adjustments of lake level and surface/volume ratio of the basin during the ice-free season

Temperature equation applied to surface sediment yields essentially modern July temperatures

File updated from "Tibetanus.Hammarlund.2002"
14C data are at: https://doi.org/10.1080/11035899801201059

Holocene changes in atmospheric circulation recorded in the oxygen-isotope stratigraphy of lacustrine carbonates from northern Sweden

Hammarlund, D., Barnekow, L., Birks, H. J. B., Buchardt, B. and Edwards, T. W. D.: Holocene changes in atmospheric circulation recorded in the oxygen-isotope                 stratigraphy of lacustrine carbonates from northern Sweden, The Holocene, 12(3), 339–351, doi:10.1191/0959683602hl548rp, 2002.

; archiveType changed - was originally Lake sediment (LS); archiveType changed - was originally Lake sediment (LS)

Trace element (Mg and Sr) concentrations in ostracod shells from Lakes Salpete ?n and Pete ?n Itza ? parallel the ?18O records, suggesting that ?18O records ref ect basin hydrology rather than changes in the isotopic composition of rainfall (Rosenmeier et al., in press). Furthermore, covariance in both ?18O and Mg eliminate temperature as a control on the oxygen isotope record.

Rosenmeier, Michael F , Hodell, David A , Brenner, Mark , Curtis, Jason H , Guilderson, Thomas P

Rosenmeier, M. F., Hodell, D. A., Brenner, M., Curtis, J. H. and Guilderson, T. P.: A 4000-Year Lacustrine Record of Environmental Change in the Southern Maya Lowlands, Peten, Guatemala, Quaternary Research, 57(2), 183–190, doi:10.1006/qres.2001.2305, 2002.

bulk carbonate, chara sp. and calcitic encrustations precipitated on Chara sp., and calcitic opercula of Bithynia tentaculata

Xray diffraction analysis, carbonates in the bulk sediment samples used for isotopic analyses were identified as exclusively lowMg calcite. No other carbonate minerals were detected.

and most ofthe carbonate macro fossil samples were processed on a preparation  line described by Buchardt (1977); less than 200um

The isotopic records from Lake Igelsj .on provide evidence ofsevera l rapid changes in net precipitation during the Holocene, the most extensive ofwhich occurred between 8300 and 8000 cal BP and around 4000 cal BP, respectively. These climatic shifts, which affected large parts of northern and central Europe, were probably related to large-scale rearrangements of atmospheric circulation patterns"For example, the widely recorded cooling shortly before 8000 cal BP, with inferred records of lowered growth-season temperatures distributed from northern Sweden to Switzerland (Snowball et al., 2002; Tinner and Lotter, 2001), seems to be associated with an increase in effective moisture of equally regional significance. This pattern suggests a  southward displacement ofthe Polar Front across most  of the North Atlantic region, giving rise to cooler summers and drastically altered cyclonic pathways, preferentially during winter seasons.

and our interpretations are based on a simplistic climate-hydrology model in which variations in groundwater generation within the lake catchment produce changes in On a hydrogen-/oxygen-isotope cross-plot (Fig. 6) all groundwater samples as well as lake-water samples from January,March, and April plot close to the global meteoric water line (Craig, 1961), whereas lake-water samples from May to July fall along a local evaporation line with a slope near 5 as expected for water bodies affected by evaporation (Craig and Gordon, 1965). These results suggest that the water body is affected by a well-developed evaporative isotopic enrichment in spite ofthe rather short residence time (ca 20 days or less) as estimated from catchment size and meteorological data. Surface run-off from the catchment and direct precipitation seems to have no major impact on the isotopic composition oflake water during the ice-free season; groundwater level and related adjustments of lake level and surface/volume ratio of the basin during the ice-free season

Rapid hydrological changes during the Holocene revealed by stable isotope records of lacustrine carbonates from Lake Igelsjdegreesn, southern Sweden

Hammarlund, D.: Rapid hydrological changes during the Holocene revealed by stable isotope records of lacustrine carbonates from Lake Igelsjoen, southern Sweden, Quaternary Science Reviews, 22(2-4), 353–370, doi:10.1016/s0277-3791(02)00091-4, 2003.

Finnegan MAT 252 isotope-ratio mass spectrometer connected to a Kiel device

We interpret the sedimentary calcite in these cores to be endogenic because (1) there are no significant sources for detrital calcite in the Lake Edward catchment (Bishop, 1969) and (2) the Mg concentration of modern calcite is in rough agreement with equilibrium calculations based on modern lake water (Lehman, 2002).

The d18O, d13C, and Mg percentage in calcite are highly covariant (Fig. 2), a relationship that indicates that Mg and d18O are strongly controlled by the P/E ratio as opposed to other environmental variables (Talbot, 1990).

chronology in Russell et al 2003b; d18O data only between 1700 BP and 400 BP

A 725 yr cycle in the climate of central Africa during the late Holocene

Russell, J. M., Johnson, T. C. and Talbot, M. R.: A 725 yr cycle in the climate of central Africa during the late Holocene, Geology, 31(8), 677, doi:10.1130/g19449.1, 2003.

the Holocene was sampled more intensively (every 0.5 cm), 4 cm intervals from 3000 cal. BP to the present, and at 1 cm intervals prior to 8200 cal. BP; Optically pure diatomite was obtained by oxidation (H2O2) to remove organics, an acid wash (10% HCl) to remove carbonates and gravity settling to remove small amounts of clay. The hydrous layer of the diatoms was stripped by outgassing during a prefluorination.

summer precipitation would impose a shift in the  isotopic composition of the lake water and ultimately  in the d18Odiatom record. More positive d18Odiatom values would suggest a greater contribution of summer rainfall from the Atlantic, bringing warmer temperatures. While more negative d18Odiatom suggests a greater contribution from the colder Arctic air mass.

The diatom blooms that provide the biogenic silica to the sediment occur in the summer months, June?  September, when the lake is ice-free, when temperatures  are highest and when rainfall is heaviest enabling  nutrients to be washed in from the catchment. The  d18Odiatom signal therefore reflects the climatic regime  during the summer months although there will be a  component of winter precipitation released from ice and snow in the catchment during the early summer thaw.; evaporative effects on the isotopic composition of the lake water are minimal.;comparison with  the pollen based temperature reconstruction indicates that the magnitude and direction of the isotope inferred temperature change is unrealistic.;

d18O values were normalised through laboratory  standards and NBS28, and corrected according to Craig  (1957) and Deines (1970).

ages derived from SOLOVIEVA and JONES, 2002 are 1996 AD and 8998 cal yr BP (-7048 AD)

Jones, Vivienne J. , Leng, Melanie J. , Solovieva, Nadia , Sloane, Hilary J. , Tarasov, Pavel

Holocene climate of the Kola Peninsula; evidence from the oxygen isotope record of diatom silica

Jones, V. J., Leng, M. J., Solovieva, N., Sloane, H. J. and Tarasov, P.: Holocene climate of the Kola Peninsula; evidence from the oxygen isotope record of diatom silica, Quaternary Science Reviews, 23(7-8), 833–839, doi:10.1016/j.quascirev.2003.06.014, 2004.

Micromass Optima gas-source mass spectrometer with a MultiPrep automated sample preparation device

Piston cores were split, described, and one half of the core was slab sampled at 1-cm intervals. The boxcore was extruded vertically and sampled every 0.5 cm. Samples were washed in deionized water, oven dried, and homogenized prior to coulometric and isotopic analyses [Yuan, 2003]

The unusual dry climate in the MWE was previously attributed to a contraction of the circumpolar vortex that resulted in the atmospheric jet stream remaining to the north of California throughout much of the MWE [Stine, 1994]. Our results support this hypothesis.

The TIC d18O derived from downcore sediments effectively parallels the anthropogenic lake-level lowering (Figure 2). The anthropogenically induced drought is recorded in downcore sediments as a 6% increase in TIC d18O. During the El Nin?o years of 1982?83 and 1997?98, Walker Lake (like Pyramid Lake) received well above average moisture. The lake volume increased by 28% from its September 1981 value and the d18OL decreased 3.6% during the 1982?83 event [Benson et al., 1991]. This climate-induced wet event was well recorded in downcore sediments as a 3% decrease in TIC d18O (Figures 2b and 2c)

A 1200 year record of hydrologic variability in the Sierra Nevada from sediments in Walker Lake, Nevada

Yuan, F., Linsley, B. K., Lund, S. P. and McGeehin, J. P.: A 1200 year record of hydrologic variability in the Sierra Nevada from sediments in Walker Lake, Nevada, Geochemistry, Geophysics, Geosystems, 5(3), doi:10.1029/2003gc000652, 2004.

Kiel automated device for isotope ratio mass spectrometry on a Finnigan Delta XLfor isotope ratio mass spectrometry on a Finnigan Delta XL

Jellybean is an evaporation-insensitive lake; The d18O of Jellybean Lake water (average 20.4 ) was identical to mean annual precipitation ( 20.4 ). We conclude that multi-annual y18 Op variation in this region is not driven by temperature changes alone. We suggest that temporal changes in atmospheric circulation across the St. Elias Mountains are the major control on the oxygen isotope composition of precipitation in the interior of the southern Yukon and hence hydrologically open lakes such as Jellybean.

We infer that  the primary control on y18Op in the southwest Yukon is temporally changing moisture trajectories into and over the coastal mountains driven by the strength and the position of the AL. Assuming this is correct, the y18OCa from Jellybean Lake provides a record of Holocene changes in intensity and/ or position of the AL

dsample= [(Rsample/ Rstandard) _ 1] _ 1000_, where R is the18O/16O

Anderson, Lesleigh , Abbott, Mark B. , Finney, Bruce P. , Burns, Stephen J.

Regional atmospheric circulation change in the North Pacific during the Holocene inferred from lacustrine carbonate oxygen isotopes, Yukon Territory, Canada

Anderson, L., Abbott, M. B., Finney, B. P. and Burns, S. J.: Regional atmospheric circulation change in the North Pacific during the Holocene inferred from lacustrine carbonate oxygen isotopes, Yukon Territory, Canada, Quaternary Research, 64(1), 21–35, doi:10.1016/j.yqres.2005.03.005, 2005.

ThermoFinnigan Kiel III carbonate preparation device coupled to a Thermo- Finnigan MAT 252 mass spectrometer

Core-top d18O values for ostracods and gastropods are close to calculated equilibrium values for calcite and aragonite, respectively

AZ: check if chronology and/or sensor integration time. integrationTime "uncertainty type" given but no time units.

DK: The LiPD file looks corupt. I assume that there should be data for 3 types of CaCO3 (snails, 'codes, and algae). Plus, time series should extend to 4.5 ka  MJ: LiPD file works ok in Playground, there are three core drives displayed seperately. AZ: check if chronology and/or sensor integration time. integrationTime "uncertainty type" given but no time units.

five shells of the spinose morphotype of P. coronatus were selected and crushed to open internal chambers, cleaned, and fragments re-picked prior to pretreatment...Gastropod shells were broken open and sonically cleaned to remove fine-grained particles from internal chambers...All carbonate samples were soaked in ~15% H2O2 for 30 min to remove organic matter and then rinsed with methanol. The methanol was removed with a syringe, and samples were dried in an oven at 508C for 24 h. Gastropods and Chara samples were ground to a homogeneous powder and ostracods were analyzed whole. Approximately 50?100 Ag of carbonate was loaded into individual reaction vessels for isotopic analysis

The salinity and 18O content of the lake water increased as a result of reduced precipitation and/or increased evaporation in the mid- to late 1500s

Variations in carbonate d18O in Aguada X?caamal were principally controlled by changes in the d18O of lake water that, in turn, reflect changes in the lake?s hydrologic budget (evaporation, precipitation, and outflow) and the d18O of incoming precipitation and groundwater

Gastropods data used here, also ostracod and charphyte carbonate records which show the same trends.

Hodell, David A. , Brenner, Mark , Curtis, Jason H. , Medina-Gonzi¿½lez, Roger , Ildefonso-Chan Can, Enrique , Albornaz-Pat, Alma , Guilderson, Thomas P.

Climate change on the Yucatan Peninsula during the Little Ice Age

Hodell, D. A., Brenner, M., Curtis, J. H., Medina-Gonzalez, R., Ildefonso-Chan Can, E., Albornaz-Pat, A. and Guilderson, T. P.: Climate change on the Yucatan Peninsula during the Little Ice Age, Quaternary Research, 63(2), 109–121, doi:10.1016/j.yqres.2004.11.004, 2005.

Crausbay, Shelley D. , Russell, James M. , Schnurrenberger, Douglas W.

A ca. 800Year Lithologic Record of Drought from Subannually Laminated Lake Sediment, East Java

Crausbay, S. D., Russell, J. M. and Schnurrenberger, D. W.: A ca. 800-Year Lithologic Record of Drought from Sub-annually Laminated Lake Sediment, East Java, Journal of Paleolimnology, 35(3), 641–659, doi:10.1007/s10933-005-4440-7, 2006.

estimate of lake residence time from mass balance modelling (Jones et al., 2005)

Modern lake isotope hydrology,  down core changes in other proxies.

Dean, Jonathan R. , Jones, Matthew D. , Leng, Melanie J. , Sloane, Hilary J. , Roberts, C. Neil , Woodbridge, Jessie , Swann, George E.A. , Metcalfe, Sarah E. , Eastwood, Warren J. , Yi?itba??o?lu, Hakan

Dean, J. R., Jones, M. D., Leng, M. J., Sloane, H. J., Roberts, C. N., Woodbridge, J., Swann, G. E. A., Metcalfe, S. E., Eastwood, W. J. and Yigitbasıoglu, H.: Palaeo-seasonality of the last two millennia reconstructed from the oxygen isotope composition of carbonates and diatom silica from Nar Goelue, central Turkey, Quaternary Science Reviews, 66, 35–44, doi:10.1016/j.quascirev.2012.07.014, 2013.

Modern lake isotope hydrology, climate calibration, down core changes in other proxies.

see aslo Dean et al in press 10.1016/j.jhydrol.2014.11.004; Jones et al., 2005 10.1007/s10933-005-6743-0

Jones, Matthew D. , Roberts, C. Neil , Leng, Melanie J. , Ti¿½rke?, Murat

A high-resolution late Holocene lake isotope record from Turkey and links to North Atlantic and monsoon climate

Jones, M. D., Roberts, C. N., Leng, M. J. and Tuerkes, M.: A high-resolution late Holocene lake isotope record from Turkey and links to North Atlantic and monsoon climate, Geology, 34(5), 361, doi:10.1130/g22407.1, 2006.

observed d18O variations over a range of 10%are much larger than water temperature variations, and species- specific differences in ostracod shell calcite formation could have caused. Water temperature alone would have had to change by 421C to engender ad18O shift of about 10%(Stuiver, 1970). Thus,d18O of the lake?s water must have changed considerably in the past reflecting salinity varia- tions at the core site and overalld18O changes of regional precipitation

range of variability exceeds possible temperature influence; corresponding ostracod species and Mg/Ca ratios

The Holocene salinity history of Bosten Lake (Xinjiang, China) inferred from ostracod species assemblages and shell chemistry: Possible palaeoclimatic implications

Mischke, S. and Wuennemann, B.: The Holocene salinity history of Bosten Lake (Xinjiang, China) inferred from ostracod species assemblages and shell chemistry: Possible palaeoclimatic implications, Quaternary International, 154-155, 100–112, doi:10.1016/j.quaint.2006.02.014, 2006.

chronological; resolution; amount of lake water temperature variation

Holocene hydrologic balance of tropical South America from oxygen isotopes of lake sediment opal, Venezuelan Andes

POLISSAR, P., ABBOTT, M., SHEMESH, A., WOLFE, A. and BRADLEY, R.: Holocene hydrologic balance of tropical South America from oxygen isotopes of lake sediment opal, Venezuelan Andes, Earth and Planetary Science Letters, 242(3-4), 375–389, doi:10.1016/j.epsl.2005.12.024, 2006.

Check that inferred material is correct (soil water vs lake water). ; change mathematical relation = "it depends..." to nonlinear?

Given the lack of correlation between dDlw and pollen- inferred mean July temperatures (Fig. 6), the downcore dDlw changes likely represent either a change in the ratio of soil water and precipitation utilized by the vegetation and/ or a change in source and pathway of regional precipita- tion. The dDlw data may indicate a heavy reliance of terrestrial plants on cool-season derived soil moisture from 11,000?8000 cal yr BP when conditions were dry. Growing- season precipitation may have been too low to provide sufficient water to the plants. An alternative and not mutually exclusive interpretation is that growing-season precipitation was not enriched in deuterium from 11,000?8000 cal yr BP because the presence of high pressure over the Laurentide ice sheet prevented the northward advection of humid, sub-tropical airmasses that are important for summer precipitation today. Both interpre- tations are consistent with Shuman and Donnelly?s (2006) interpretation that low lake levels prior to ca 8200 cal yr BP resulted from low summer precipitation rates and a high ratio of winter to summer precipitation.

circulation changes caused by ice sheet topography. Precipitation seasonality.

changes depending on which season provides source moisture for plants

match with pollen based January temperature, C16 n-acids are produced by aquatic plants, and ponds in this region are recharged mainly by winter precipitation (Shuman and Donnelly, 2006, Quat Res, 65:44-56)

match with pollen based January temperature, C16 n-acids are produced by aquatic plants, and ponds in this region are recharged mainly by winter precipitation

lake equilibrium with the mean annual balance of precipitation and evaporation across the watershed

Compound-specific isotopic analyses track changes in seasonal precipitation regimes in the Northeastern United States at ca 8200calyrBP

Shuman, B., Huang, Y., Newby, P. and Wang, Y.: Compound-specific isotopic analyses track changes in seasonal precipitation regimes in the Northeastern United States at ca 8200calyrBP, Quaternary Science Reviews, 25(21-22), 2992–3002, doi:10.1016/j.quascirev.2006.02.021, 2006.

amount of calcite estimated from peak intensities of the diffractograms is 15%

sediment had been bleached to  remove organic matter and sieved at 63 um to remove ostracodes.

Stevens, Lora R. , Stone, Jeffery R. , Campbell, Josh , Fritz, Sherilyn C.

A 2200-yr record of hydrologic variability from Foy Lake, Montana, USA, inferred from diatom and geochemical data

Stevens, L. R., Stone, J. R., Campbell, J. and Fritz, S. C.: A 2200-yr record of hydrologic variability from Foy Lake, Montana, USA, inferred from diatom and geochemical data, Quaternary Research, 65(02), 264–274, doi:10.1016/j.yqres.2005.08.024, 2006.

Finnigan MAT 252 isotope-ratio mass spectrometer (IRMS) interfaced with an automated Kiel device

We sampled the sediments contiguously at 3-year intervals for the past 250 years and at 5-year intervals for the remainder of the past 3100 years.

The d18O record of the past 3100 years reveals that droughts of greater severity and duration than during the 20th century occurred repeatedly, especially prior to 300 AD. Drought variability was anomalously low during the 20th century; 90% of the variability values during the last 3100 years were greater than the 20th-century average. d18O is strongly correlated with the index of the Pacific Decadal Oscillation (PDO) during the past 100 years, and periodicities of the late- Holocene d18O record are similar to those of the PDO. Furthermore, time series of d18O and atmospheric D14C are generally coherent after 700 AD. Both the Pacific climate and solar irradiance probably played a role in drought occurrence, but their effects were non-stationary through the late Holocene.;a highly significant, positive correlation (r = 0.63, n = 32, p < 0.0001) exists between d18O and the PDO. This pattern can be explained by the negative correlation of the PDO with measured winter (r = 0.44, n = 103, p < 0.001) and summer (r = 0.35, n = 103, p < 0.001) precipitation near Steel Lake. Dry winters likely decrease the proportion of 18O-depleted winter precipitation entering the lake, and dry summers enhance evaporative 18O-enrichment of lake watea highly significant, positive correlation (r = 0.63, n = 32, p < 0.0001) exists between d18O and the PDO. This pattern can be explained by the negative correlation of the PDO with measured winter (r = 0.44, n = 103, p < 0.001) and summer (r = 0.35, n = 103, p < 0.001) precipitation near Steel Lake. Dry winters likely decrease the proportion of 18O-depleted winter precipitation entering the lake, and dry summers enhance evaporative 18O-enrichment of lake wate

However, two lines of evidence indicate that at Steel Lake, evaporative 18O enrichment related to aridity was the dominant control. First, the d18O values of water samples from the epilimnion and hypolimnion of Steel Lake were 8.7 and 10.7%, respectively, in July 2001 (Figure 1d). The elevated d18O value of the epilimnetic water resulted from evaporative 18O enrichment, suggesting that Steel  Lake is sensitive to evaporation;In particular, the most severe historic drought events in north-central Minnesota, the 1988 drought [Trenberth et al., 1988] and 1930s Dust Bowl [Worster, 1979], are recorded by the heaviest d18O values at Steel Lake

Possible linkages of late-Holocene drought in the North American midcontinent to Pacific Decadal Oscillation and solar activity

Tian, J., Nelson, D. M. and Hu, F. S.: Possible linkages of late-Holocene drought in the North American midcontinent to Pacific Decadal Oscillation and solar activity, Geophysical Research Letters, 33(23), doi:10.1029/2006gl028169, 2006.

Kiel automated device for isotope ratio mass spectrometry on a Finnigan Delta XL mass ratio spectrometer.

Chara encrustations, ostracodes, gastropod and mollusk shell fragments and the <125-mm fraction of marl sediment from selected intervals of the core

Bulk sediment samples were taken from core C/E for isotope analyses at 0.5-cm increments for the uppermost 16.5 cm (32 field-extruded samples; Glew, 1988; Glew et al., 2001), at 1-cm increments from 16.5-cm depth to the White River Ash at 64-cm depth, and at 2-cm increments from 64- to 144-cm depth for a total of 121 samples. The bulk sediment samples were wet sieved through nested screens (63, 125, 250-mm), collected separately and freeze dried. At least five individual Chara stem encrustations (1?3 mm each in length) were picked from the dried fractions, examined for purity, homogenized and sub- sampled for CO2 extraction

18O-enrichment in Marcella Lake water caused by summer effective moisture conditions; These prominent late Holocene changes in effective moisture occurred simultaneously with changes in Aleutian Low circulation patterns over the Gulf of Alaska indicated by Jellybean Lake. The reconstructed climate patterns are consistent with the topographically controlled climatic heterogeneity observed in the coastal mountains and interior valleys of the region today

effective moisture occurred simultaneously with changes in Aleutian Low circulation

Temperature fractionations between calcite and lake water were considered and are thought to be minor (0.25%/1C).

dsample 1?4 ([Rsample/Rstandard]-) x 1000 where R = 2H/1H, 18O/16O in sample and standard, respectively; First, the oxygen isotope stratigraphy from each lake was converted into three smoothed time-series at 50, 100 and 200-year intervals to examine multi-decadal and longer-term variations (Figs. 5a and b). Second, the Jellybean-d18OCa time-series were subtracted from the Marcella-d18O Chara time-series to produce a third, Dd (Fig. 5c). Variability of evaporation-insensitive Jellybean-d18OCa is relatively small (1.5?2%) compared to Marcella Lake (4.0?5.0%), but there are intervals where the d18Op correction results in  distinguishable effects on long-term trends of Marcella-d18OChara (note arrows in Fig. 5a and c). The smoothing procedure was done to eliminate problems due to temporal mismatches between individual samples from the two cores but given the nature of the trends does not significantly effect the uncertainty regarding timing of prominent shifts or long-term trends.

Late Holocene moisture balance variability in the southwest Yukon Territory, Canada

Anderson, L., Abbott, M. B., Finney, B. P. and Burns, S. J.: Late Holocene moisture balance variability in the southwest Yukon Territory, Canada, Quaternary Science Reviews, 26(1-2), 130–141, doi:10.1016/j.quascirev.2006.04.011, 2007.

comparison of theoretical carbaontes precipitated from modern waters

Just accepted as age model based on age nearish to 1AD i.e. 2600 BP

Eastwood, Warren J. , Leng, Melanie J. , Roberts, Neil , Davis, Basil

Eastwood, W. J., Leng, M. J., Roberts, N. and Davis, B.: Holocene climate change in the eastern Mediterranean region: a comparison of stable isotope and pollen data from Lake Goelhisar, southwest Turkey, Journal of Quaternary Science, 22(4), 327–341, doi:10.1002/jqs.1062, 2007.

no mineralogical data are available, the range of oxygen isotope values is consistent with other calcite producing lakes in Ethiopia

Using Leng and Marshall's (2004) expression of Kim and O'Neil's (1997) equation, the surface sediment 18O value of 6.2? (core top taken in 1999) and 18O water of 8.1? (average between 1997 and 2001, Table 2) suggests precipitation temperatures of around 23C, higher than the measured mean annual air temperature of 18C.

Rainfall at Addis Ababa has a weighted mean 18O composition of 1.2?, while groundwater values recorded in Ethiopia range from a6.2? to a1.3? (table 2 in Lamb et al., 2000). It seems likely that the oxygen isotope values for the lake surface water (up to 9? VSMOW) result from evaporative enrichment (confirmed by the hydrological balance, Table 1), which is also represented in the high values for the carbonates in the surface sediments (18O 6.2? VPDB).

Using Leng and Marshall?s (2004) expression of Kim and O?Neil?s (1997) equation, the surface sediment 18O value of 6.2? (core top taken in 1999) and 18O water of 8.1? (average between 1997 and 2001, Table 2) suggests precipitation temperatures of around 23C, higher than the measured mean annual air temperature of 18C.

Lamb, H. F. , Leng, M. J. , Telford, R. J. , Ayenew, T. , Umer, M.

Oxygen and carbon isotope composition of authigenic carbonate from an Ethiopian lake: a climate record of the last 2000 years

Lamb, H. F., Leng, M. J., Telford, R. J., Ayenew, T. and Umer, M.: Oxygen and carbon isotope composition of authigenic carbonate from an Ethiopian lake: a climate record of the last 2000 years, The Holocene, 17(4), 517–526, doi:10.1177/0959683607076452, 2007.

our calculated [equilibium] d18OC values of ?12.7? are similar to core values from the last few hundred years, which lends support to the idea that the modern carbonates are precipitating in equilibrium.

We argue that a substantial and persistent change in !p is required to change the annual mean values of d18Ow in northern Scandinavia.

All the modern lake and groundwater isotope data lie on the Local Meteoric Water Line (LMWL) (IAEA/WMO, 2006) indicating that evaporation is not important. The similarity of the isotope composition of the lake and its different groundwater reservoirs indicate that the lake is likely to be constantly replenished by groundwater input and subterraneous outflow resulting in a short water residence time.

North Atlantic region atmospheric circulation dynamics inferred from a late-Holocene lacustrine carbonate isotope record, northern Swedish Lapland

Rosqvist, G. C., Leng, M. J. and Jonsson, C.: North Atlantic region atmospheric circulation dynamics inferred from a late-Holocene lacustrine carbonate isotope record, northern Swedish Lapland, The Holocene, 17(7), 867–873, doi:10.1177/0959683607080508, 2007.

GV IsoPrime IRMS coupled with an online carbonate preparation system (MultiPrep)

I just moved this from the Rejected list - not sure why it was there and not here? Data also published in Yan et al 2011 (Nat Comms) and data on NOAA from that paper, but from what I can tell, isotope data are same as in 2008 paper

Liu, X., Sun, L., Wei, G., Wang, Y., Yan, H., Liu, K. and Wu, X.: A 1,100-year palaeoenvironmental record inferred from stable isotope and trace element compositions of ostracode and plant caryopses in sediments of Cattle Pond, Dongdao Island, South China Sea, Journal of Paleolimnology, 40(4), 987–1002, doi:10.1007/s10933-008-9211-9, 2008.

Finnigan MAT 252 massspectrometer coupled to a Kiel II carbonate sampling device

sample was  homogenized  prior to division into aliquots for isotope and diatom  analyses; Sediment for isotopic analysis was reacted with 2% sodium hypochlorite to remove organic matter and rinsed five times. The sediment was then sieved at 63 mm to remove ostracodes, shell material, and charaphyte sheaths. The flowthrough from the sieve was collected, freezedried, homogenized, and analyzed for carbon and oxygen isotopes

The d18O record from the varved sediment from Crevice Lake is a proxy for hydroclimate, particularly discharge of the Yellowstone River, in Yellowstone National Park. Low d18O values are consistent with high flow of the Yellowstone River and, thus, wet winters with deep snow pack. They also correspond in general with tree-ring inferred estimates of increased precipitation in the YNP region. Prior to 2000 cal BP, decreasing d18O values suggest an increasingly wet climate or a gradual shift to winterdominated precipitation

Comparison of the oxygen-isotopic record with independent measures of climate suggests that the annual moisture balance is the primary isotopic control, with the seasonal timing of precipitation providing a possible secondary influence. High d18O values are associated with dry climate (e.g., evaporative enrichment of 18O) and/or wet summers relative to winters (higher d18O values of atmospheric precipitation).

with the seasonal timing of precipitation providing a possible secondary influence. High d18O values are associated with  dry climate (e.g., evaporative enrichment of 18O) and/or  wet summers relative to winters (higher d18O values of  atmospheric precipitation).

Geochemical evidence for hydroclimatic variability over the last 2460 years from Crevice Lake in Yellowstone National Park, USA

Stevens, L. R. and Dean, W. E.: Geochemical evidence for hydroclimatic variability over the last 2460 years from Crevice Lake in Yellowstone National Park, USA, Quaternary International, 188(1), 139–148, doi:10.1016/j.quaint.2007.11.012, 2008.

DK: Rejected: Does not meet criteria for geochronology. Youngest age is 2.8 ka. BM, ZK: 04/01/2019: wrong coordinates, should be W not E, should be S not N

online automated carbonate preparation system linked to a Finnigan Delta XL ratio mass spectrometer

all recognisable coarse shells and shell fragments handpicked from sediment sample prior to analysis

comparison with Quelccaya ice core record (see Baker et al. 2009)

d18O.lake = d18O.precipitation + [(1h)(permil* + Ck)] / [h + (1  h)(Qi/Qe)]

not reported. Lake surface temperature and evaporative flux assumed to remain constant

Baker, Paul A. , Fritz, Sherilyn C. , Burns, Stephen J. , Ekdahl, Erik , Rigsby, Catherine A.

Past Climate Variability in South America and Surrounding Regions

The Nature and Origin of Decadal to Millennial Scale Climate Variability in the Southern Tropics of South America: The Holocene Record of Lago Umayo, Peru

Baker, P. A., Fritz, S. C., Burns, S. J., Ekdahl, E. and Rigsby, C. A.: The Nature and Origin of Decadal to Millennial Scale Climate Variability in the Southern Tropics of South America: The Holocene Record of Lago Umayo, Peru, Developments in Paleoenvironmental Research, 301–322, doi:10.1007/978-90-481-2672-9_13, 2009.

Automated Finnigan CarboFlo system, interfaced with Finnigan MAT Delta-plus MS

check if chronology and/or sensor integration time. integrationTime "uncertainty type" given but no time. (GF)

The oxygen isotope composition of ostracod carapaces depends primarily on the d18O composition of the water and the tempera- ture at which carbonates precipitate (Craig, 1965; Stuiver, 1970). In tropical, closed-basin lakes within seasonally dry climates, the d18O value of lake water is controlled primarily by the evaporation to precipitation ratio (E/P) of the lake (Fontes and Gonfiantini, 1967; Gasse et al., 1990). During periods of increased (decreased) E/P ratios, the d18O value of lake water will go up (down) as kinetic fractionation processes lead to an increase (decrease) in concen- trations of 18O relative to 16O. Assuming that long-term tempera- ture changes in the tropics are less likely to affect d18O values in the lake than are changes in the E/P ratio (Covich and Stuiver, 1974; Curtis and Hodell, 1993), the d18O value of ostracod carapaces should indicate variations in the E/P ratio of the lake.

Lane, C. S., Horn, S. P., Mora, C. I. and Orvis, K. H.: Late-Holocene paleoenvironmental change at mid-elevation on the Caribbean slope of the Cordillera Central, Dominican Republic: a multi-site, multi-proxy analysis, Quaternary Science Reviews, 28(23-24), 2239–2260, doi:10.1016/j.quascirev.2009.04.013, 2009.

Hodgson, D. A., Roberts, S. J., Bentley, M. J., Carmichael, E. L., Smith, J. A., Verleyen, E., Vyverman, W., Geissler, P., Leng, M. J. and Sanderson, D. C. W.: Exploring former subglacial Hodgson Lake, Antarctica. Paper II: palaeolimnology, Quaternary Science Reviews, 28(23-24), 2310–2325, doi:10.1016/j.quascirev.2009.04.014, 2009.

Where water loss is mainly through evaporation as is likely for Lake Ashenge, the waters tend to have a variable and elevated oxygen isotope composition relative to regional rainfall (which tends to be negative). Measured d18Ocarb values are always higher than those of ambient precipitation as the lighter isotope 16O is preferentially lost to evaporation (Leng et al.,2006)...The isotope records from Ashenge therefore show large swings in composition as the ratio of precipitation to evaporation (P/E) has changed through time

Marshall, Michael H. , Lamb, Henry F. , Davies, Sarah J. , Leng, Melanie J. , Kubsa, Zelalem , Umer, Mohammed , Bryant, Charlotte

Climatic change in northern Ethiopia during the past 17,000degreesyears: A diatom and stable isotope record from Lake Ashenge

Marshall, M. H., Lamb, H. F., Davies, S. J., Leng, M. J., Kubsa, Z., Umer, M. and Bryant, C.: Climatic change in northern Ethiopia during the past 17,000 years: A diatom and stable isotope record from Lake Ashenge, Palaeogeography, Palaeoclimatology, Palaeoecology, 279(1-2), 114–127, doi:10.1016/j.palaeo.2009.05.003, 2009.

isotopic values d18O of calcite precipitating in the surface waters of Zoi¿½ar Lake obtained from a buoy and anchor rope concretion growth show values (between ?2 to +1? vs V-PDB) coherent with calcite formation in isotopic equilibriumwith epilimnetic lake waters (+1 to + 6??18Owater (V-SMOW))

XRD, SEM; calcite layer composed almost only by rhomboedric calcite crystals, 5?15 ?m long

However, the continuous enrichment of 18O, due to evaporation, during spring and summer results in heavier isotope values at the end of the warm seasons. Consequently, the isotopic oscillations can be interpreted as a reflection of changes in the intensity of the evaporation processes (Li and Ku,1997) that cancel out the opposite effect of the temperature increase (decreasing isotopic fractionation with increasing temperature; McCrea, 1950).

Isotopic values ?18O of calcite precipitating in the surface waters of Zo�ar Lake obtained from a buoy and anchor rope concretion growth show values (between ?2 to +1? vs V-PDB) coherent with calcite formation in isotopic equilibriumwith epilimnetic lake waters (+1 to + 6??18Owater (V-SMOW))

Marti¿½n-Puertas, Celia , Valero-Garci¿½s, Blas L. , Brauer, Achim , Mata, M. Pilar , Delgado-Huertas, Antonio , Dulski, Peter

Martin-Puertas, C., Valero-Garces, B. L., Brauer, A., Mata, M. P., Delgado-Huertas, A. and Dulski, P.: The Iberian–Roman Humid Period (2600–1600 cal yr BP) in the Zonar Lake varve record (Andalucia, southern Spain), Quaternary Research, 71(2), 108–120, doi:10.1016/j.yqres.2008.10.004, 2009.

check if chronology and/or sensor integration time. integrationTime "uncertainty type" given but no time or time units. (GF)

The high d18Oshell values, evaporite minerals, low carbonate content and steadily increasing Na concentration suggest that the salinity of Lake Kuhai remained high in zone 6.

Mischke, Steffen , Zhang, Chengjun , Bi¿½rner, Anko , Herzschuh, Ulrike

Lateglacial and Holocene variation in aeolian sediment flux over the northeastern Tibetan Plateau recorded by laminated sediments of a saline meromictic lake

Mischke, S., Zhang, C., Boerner, A. and Herzschuh, U.: Lateglacial and Holocene variation in aeolian sediment flux over the northeastern Tibetan Plateau recorded by laminated sediments of a saline meromictic lake, Journal of Quaternary Science, 25(2), 162–177, doi:10.1002/jqs.1288, 2010.

The dD of closed-basin tropical lakes such as Wandakara reflects the hydrologic balance of the lake, with drier conditions causing isotopically enriched lake water due to both the amount effect on precipitation and kinetic fractionation during evaporation from the lake surface, which favors the retention of deuterium relative to hydrogen in the lake water (Craig, 1961).

Short-chain (C16?C18) fatty acids in lake sediments are derived primarily from aquatic sources (Eglinton and Hamilton, 1967; Huang et al., 2002), and the principal control on their ?D is the ?D of lake water (Huang et al., 2002, 2004). ... "The ?D of closed-basin tropical lakes such as Wandakara reflects the hydrologic balance of the lake, with drier conditions causing isotopically enriched lake water due to both the amount effect on precipitation and kinetic fractionation during evaporation from the lake surface, which favors the retention of deuterium relative to hydrogen in the lake water (Craig, 1961). "

The shift toward grassland at AD 1000 must therefore have influenced the ?DC30 record due to biosynthetic fractionation differences between trees and grasses (Hou et al., 2007). Indeed, the enormous amplitude of shifts in ?DC30 relative to ?DC16 likely results from the replacement of forest with C4 grasslands during wet periods?a process driven by humans rather than by climate. The amplified ?DC30 response occurs because of a combination of the amount effect during wet periods and stronger isotopic fractionation by grasses relative to trees, both of which favor isotopically depleted ?DC30 (Hou et al., 2008).

The ?D of long-chain, terrestrially derived fatty acids is controlled by the ?D of the water used by plants, transpiration from leaf surfaces, and kinetic fractionation during biosynthesis (Hou et al., 2008; Sessions et al., 1999).  ... "Thus, although the first-order control on leaf wax ?D in the tropics is the ?D of meteoric waters, interactions between climate and vegetation suggest the potential for complex, non-linear responses of leaf wax ?D to rainfall variability."

If changes in vegetation surrounding Lake Wandakara were mainly driven by rainfall, ?13CC30 and ?DC30 should also be positively correlated: during intervals of drought shifts toward C4 ecosystems would occur, recorded by enriched ?DC30 values. However, ?13CC30 and ?DC30 are clearly negatively correlated (Fig. 5). In fact, large positive shifts in ?13CC30 are associated with depleted ?DC30 values, and peak ?13CC30 from AD 1200 to 1440 occurs during an interval of regionally wet climate conditions (Russell et al., 2007, Russell and Johnson, 2007). This suggests that the abrupt shifts toward C4 vegetation were not caused by climate but instead by human activities on the landscape, presumably forest clearance for agriculture (Ssemmanda et al., 2005).

Russell, James M. , McCoy, S.J. , Verschuren, D. , Bessems, I. , Huang, Y.

Russell, J. M., McCoy, S. J., Verschuren, D., Bessems, I. and Huang, Y.: Human impacts, climate change, and aquatic ecosystem response during the past 2000 yr at Lake Wandakara, Uganda, Quaternary Research, 72(3), 315–324, doi:10.1016/j.yqres.2009.06.008, 2009.

AA: This record should be removed: it is duplicated in LS14ZHJU (and is a shorter version of the latter record)

Sachs, Julian P. , Sachse, Dirk , Smittenberg, Rienk H. , Zhang, Zhaohui , Battisti, David S. , Golubic, Stjepko

Southward movement of the Pacific intertropical convergence zone AD 1400?1850

Sachs, J. P., Sachse, D., Smittenberg, R. H., Zhang, Z., Battisti, D. S. and Golubic, S.: Southward movement of the Pacific intertropical convergence zone AD 1400–1850, Nature Geoscience, 2(7), 519–525, doi:10.1038/ngeo554, 2009.

Semi-preparative HPLC-MS to isolate dinosterol, which was then acetylated and injected on a GC, Delta V IRMS system

dD values of lake surface water are controlled by the amount of rainfall, its isotopic composition and the amount of mixing with the underlying seawater. As rain also increases the density stratification in the lakes, decreasing mixing, surface water dD values are expected to be significantly lower during wet periods compared with dry periods. Conclusions of the paper are about moisture balance (P-E) in the tropical Pacific.

Permanent anoxia in the subsurface water confines phytoplankton, dominated by dinoflagellates and diatoms24, to the oxygenated, brackish and deuterium-depleted surface water where their lipid ?D values can be expected to closely co-vary with the surface water ?Dvalues25,26. ?D values of that water are controlled by the amount of rainfall, its isotopic composition and the amount of mixing with the underlying sea water. As rain also increases the density stratification in the lakes, decreasing mixing, surface water ?D values are expected to be significantly lower during wet periods compared with dry periods.  Zhang and Sachs 2007, Organic Geochemistry, 38: 582-608.

Permanent anoxia in the subsurface water confines phytoplankton, dominated by dinoflagellates and diatoms24, to the oxygenated, brackish and deuterium-depleted surface water where their lipid dD values can be expected to closely co-vary with the surface water dDvalues25,26. dD values of that water are controlled by the amount of rainfall, its isotopic composition and the amount of mixing with the underlying sea water. As rain also increases the density stratification in the lakes, decreasing mixing, surface water dD values are expected to be significantly lower during wet periods compared with dry periods.  Zhang and Sachs 2007, Organic Geochemistry, 38: 582-608.

Methodology in Smittenberg and Sachs, 2007, Journal of Chromatography, 1169:70-76

Costech Zero Blank Auto Sampler-Thermo/Finnigan TC/EA-Thermo Delta V Plus IRMS via Conflo III combustion interface

Sachs and Sachse 2008, GCA , 72:793-806. Conclusions of the paper are about moisture balance (P-E) in the tropical Pacific.

Sachs and Sachse 2008, GCA , 72:793-806; "dD values of lipids...were closely correlated with salinity, owing to a decrease in D/H fractionation between lipids and source water as salinity increases. TLE dD values can therefore be used as a salinity indicator in hypersaline evnrionments such as those at Christmas Island".

the only uncertainty information I have been able to find is as follows "The average standard deviation (sigma) of all measured samples was 3.8?" from Sachse and Sachs (2008) GCA, 72:793-806 (this paper was referenced in the method section of the main publication)

stepwise fluorination technique, which uses a CO2 laserablation system, coupled to a mass spectrometer, University of New Mexico, Albuquerque

Diatom extracts were screened for purity using a highpowered microscope, and a scanning electron microscope

Check entries in isotopeInterpretation2 & isotopeInterpretation3 (GF)

MJ: Longitude written in paper not the same as shown on map in paper.

Late Holocene excursions to lower d18Odiatom values suggest a reduc- tion of south-to-north storm trajectories delivered by meridional flow, which likely corresponds to pro- longed intervals when the Aleutian Low pressure system weakened.

Shifts of d18Odiatom values are likely not related to changes in diatom taxa or dissolution effects. Modern lake water falls along meteoric water line for the region

Schiff, Caleb J. , Kaufman, Darrell S. , Wolfe, Alexander P. , Dodd, Justin , Sharp, Zachary

Late Holocene stormtrajectory changes inferred from the oxygen isotope composition of lake diatoms, south Alaska

Schiff, C. J., Kaufman, D. S., Wolfe, A. P., Dodd, J. and Sharp, Z.: Late Holocene storm-trajectory changes inferred from the oxygen isotope composition of lake diatoms, south Alaska, Journal of Paleolimnology, 41(1), 189–208, doi:10.1007/s10933-008-9261-z, 2008.

DK: Chronlogy based on existing published version, but has been updated in 2018, but not yet publised. Upate affects ages older than 11 ka.

Analyses?18O of carbonate minerals were conducted on a Finnigan-MAT 252 isotope ratio mass spectrometer with a Kiel II automated carbonate preparation device;

Homogenized 1 cm subsamples were pretreated for isotope analysis by 24 h digestion in ~45 ml of 2.5% sodium hypochlorite, then sieved (125 ?m) to remove ostracode shells and other coarse materials

Oxygen isotopes point toward maximum evaporative forcing early in the Holocene, by or before 9000 cal. yr BP. Mineralogical indicators of lake salinity decline gradually after 6000 cal. yr BP but freshening was episodically reversed and modern lake geochemistry was achieved late in the Holocene, after 1400 cal. yr BP. The Lateglacial?Holocene transition is marked by an abrupt and sustained geochemical anomaly reflecting reduced evaporative forcing and lake freshening...Oxygen isotopes record a rich spectrum of high-frequency variation interpreted as dominantly transient response to fluid balance change, but are relatively insensitive to low-frequency changes better reflected in sediment mineralogy. Oxygen and carbon isotopes covary closely at high frequencies but are decoupled at low frequencies by longterm lake basin changes in carbon cycling.

The persistent dominance of endogenic carbonate minerals requires a dynamic balance between groundwater inflow, evaporative concentration and groundwater outflow. "Fluid balance"In groundwater-dominated lakes, sediment geochemistry becomes closely linked to changes in lake?groundwater exchange and groundwater recharge at all timescales.

Lateglacial and Holocene hydroclimate inferred from a groundwater flow-through lake, Northern Rocky Mountains, USA

Shapley, M. D., Ito, E. and Donovan, J. J.: Lateglacial and Holocene hydroclimate inferred from a groundwater flow-through lake, Northern Rocky Mountains, USA, The Holocene, 19(4), 523–535, doi:10.1177/0959683609104029, 2009.

Comparison with lake water, similar trend in both species analysed

Andersson, Sofia , Rosqvist, Gunhild , leng, Melanie j. , Wastegi¿½rd, Stefan , Blaauw, Maarten

Late Holocene climate change in central Sweden inferred from lacustrine stable isotope data

Andersson, S., Rosqvist, G., leng, M. j., Wastegard, S. and Blaauw, M.: Late Holocene climate change in central Sweden inferred from lacustrine stable isotope data, Journal of Quaternary Science, 25(8), 1305–1316, doi:10.1002/jqs.1415, 2010.

Has 'basis' for isotopeInterpretation3 but no further information

contiguous 0.5permil1.0cm intervals; analyses, samples were washed through a 109mm mesh, and 15 Charastem encrustations were manually selected from the residue except in samples that yielded fewer stems. The encrustations were bleached in 3% NaOCl solution, rinsed four times in doubly distilled water, airdried, and ground to powder.

The dominant role of winter precipitation (Pw) in the waterbalance of Takahula Lake suggests that the lake should be particularly  sensitive to interannual changes in the strength and position  of the AL. A westerly AL corresponds to increased moisture delivery  into interior Alaska, whereas an easterly AL results in storm  systems that cross the Coastal Range and the Alaska Range and cut  off winter moisture supply to interior Alaska

These exceptionally low values suggest that factors other than effective moisture must have contributed to the pronounced variations in the Takahula Lake d18O  record. Increased winter precipitation associated with a westerly Aleutian Low position may account for 1 permil of the d18O decrease. Other factors leading to the 18O-depletion during these periods probably  include decreased temperatures, as well as increased lake-ice cover and associated reductions in evaporation.

A lowering of lake level by 0.5m would turn the lake into a topographically closed basin. Under such conditions, evaporation becomes the main  process of water loss, and lake-water continues to become 18Oenriched  until d18O of the evaporating vapor equals d18O of the input (Gat and Levy, 1978; Leng and Marshall, 2004). In contrast, a more positive water balance than the present is expected to  shorten the lake?s water-residence time, reducing the influence of evaporation on the lake?s isotope composition (Craig, 1961). Thus  the d18OCc record can be used to infer qualitative changes in  effective moisture.

we employed the model developed by Bowen and Wilkinson (2002) and Bowen and Revenaugh (2003) to estimate the isotope composition of monthly precipitation atTakahula Lake.

We calculated a regional meteoric water line (RMWL) from
 precipitation dD and d18O data from Global Network of Isotopes in
 Precipitation (GNIP) (IAEA/WMO, 2004) sites in Bethel (60 4604800
 N, 161 4800000 W), Barrow (71 1800000 N, 156 4604800 W), Mayo
 (63 2201200 N, 135 3101200 W), and Whitehorse (60 4301200 N,
 135 401200 W)'

Clegg, B. F. and Hu, F. S.: An oxygen-isotope record of Holocene climate change in the south-central Brooks Range, Alaska, Quaternary Science Reviews, 29(7-8), 928–939, doi:10.1016/j.quascirev.2009.12.009, 2010.

Ostracods samples pretreated with 3% H2O2, then samples were split using a microsplitter.

The d18Onorm record of ostracod valves preserved in Blue Lake reflects a history of evaporative enrichment and fluctuating groundwa- ter recharge.

6000years of environmental changes recorded in Blue Lake, South Australia, based on ostracod ecology and valve chemistry

Gouramanis, C., Wilkins, D. and De Deckker, P.: 6000years of environmental changes recorded in Blue Lake, South Australia, based on ostracod ecology and valve chemistry, Palaeogeography, Palaeoclimatology, Palaeoecology, 297(1), 223–237, doi:10.1016/j.palaeo.2010.08.005, 2010.

Also, the instrumented lake level of Lake Qinghai and coeval d18OC variations is correlated over the last w50 years (Henderson et al., 2003). Because lake level is influenced by effective moisture, d18OC would be expected to be a good proxy for P/E.

Late Holocene isotope hydrology of Lake Qinghai, NE Tibetan Plateau: effective moisture variability and atmospheric circulation changes

A.C.G., H.: A carbon- and oxygen-isotope record of recent environmental change from Qinghai Lake, NE Tibetan Plateau, Chinese Science Bulletin, 48(14), 1463, doi:10.1360/02wd0272, 2003.

high-temperature pyrolysis using an on-line continuousflow isotope-ratio mass spectrometer

The lake was probably hydrologically closed until ?800 cal yr BP, but experienced higher lake levels ?9000e7500 and ?3300e800 cal yr BP and low lake levels during the intervening times

Monitoring of the isotopic composition of modern lake water and precipitation shows that, at present, the lake water traces the isotopic composition of precipitation, modified by a slight evaporative enrichment during the open-water season and a minor snowmelt signal.

carbonate d18O in older part of the record co-vary with cellulose data

Heikkila, Maija , Edwards, Thomas W.D. , Seppa, Heikki , Sonninen, Eloni

Sediment isotope tracers from Lake Saarikko, Finland, and implications for Holocene hydroclimatology

Heikkilae, M., Edwards, T. W. D., Seppae, H. and Sonninen, E.: Sediment isotope tracers from Lake Saarikko, Finland, and implications for Holocene hydroclimatology, Quaternary Science Reviews, 29(17-18), 2146–2160, doi:10.1016/j.quascirev.2010.05.010, 2010.

chronology in particular: based on pollen stratigraphy; uncertainties with hydrology and controls over d18O lake water

Holmes, J. , Arrowsmith, C. , Austin, W. , Boyle, J. , Fisher, E. , Holme, R. , Marshall, J. , Oldfield, F. , van der Post, K.

Climate and atmospheric circulation changes over the past 1000 years reconstructed from oxygen isotopes in lake-sediment carbonate from Ireland

Holmes, J., Arrowsmith, C., Austin, W., Boyle, J., Fisher, E., Holme, R., Marshall, J., Oldfield, F. and van der Post, K.: Climate and atmospheric circulation changes over the past 1000 years reconstructed from oxygen isotopes in lake-sediment carbonate from Ireland, The Holocene, 20(7), 1105–1111, doi:10.1177/0959683610369504, 2010.

on-line continuous-flow isotope-ratio mass spectrometer at the University of Waterloo Environmental Isotope Laboratory

Unfortunately, neither of these cellulose-inferred lakewater d18O records extends to the present, which precludes direct linking with time series of modern lakewater d18O measurements

Sediment samples were washed in 10% HCl to eliminate biogenic and mineral carbonates, freeze-dried, and gently dry-sieved using a 500-mm mesh. The sieving step removes the larger organic fragments, which have a greater potential to be derived from in-washed terrestrial material, while concentrating the fine organic fraction, derived primarily from zooplankton faecal pellets that deliver aquatic organic matter directly to the sediments (Edwards 1993). The fine-grained fraction was then processed through additional steps to remove non-cellulose organic components and minerogenic matter, including solvent extraction, bleaching, alkaline hydrolysis, oxyhydroxide leaching, and sodium polytungstate density separation

Data from surface waters sampled in the area (Fig. 3B) reveal evaporative enrichment in some lakes consistent with the predicted LEL, whereas data from Lake Spa? ime are strictly constrained to the LMWL, with an average composition identical to that of local groundwater.

Chronology in Hammarlund, Dan, et al. "Palaeolimnological and sedimentary responses to Holocene forest retreat in the Scandes Mountains, west-central Sweden." The Holocene 14.6 (2004): 862-876.

Data from surface waters sampled in the
area (Fig. 3B) reveal evaporative enrichment in some
lakes consistent with the predicted LEL, whereas data
from Lake Spa˚ ime are strictly constrained to the
LMWL, with an average composition identical to that
of local groundwater.

cellulose
d18O records are presented in Fig. 6 as inferred lakewater
d18O values using a constant cellulose–water isotopic
fractionation factor of 1.028

St. Amour, Natalie A. , Hammarlund, Dan , Edwards, Thomas W.D. , Wolfe, BRENT B.

New insights into Holocene atmospheric circulation dynamics in central Scandinavia inferred from oxygen-isotope records of lake-sediment cellulose

ST. AMOUR, N. A., HAMMARLUND, D., EDWARDS, T. W. D. and WOLFE, B. B.: New insights into Holocene atmospheric circulation dynamics in central Scandinavia inferred from oxygen-isotope records of lake-sediment cellulose, Boreas, 39(4), 770–782, doi:10.1111/j.1502-3885.2010.00169.x, 2010.

Finnigan Mat 251 isotope ratio gas mass spectrometer coupled to an automated carbonate preparation device (Kiel II).

Chronology established using 210Pb and 137Cs. Ages and sedimentation rates were calculated using a CRS model assuming a constant rate of supply of 210Pb to the sediment according to Appleby and Oldfield (1978).

Wrozyna, Claudia , Frenzel, Peter , Steeb, Philip , Zhu, Liping , van Geldern, Robert , Mackensen, Andreas , Schwalb, Antje

Stable isotope and ostracode species assemblage evidence for lake level changes of Nam Co, southern Tibet, during the past 600years

Wrozyna, C., Frenzel, P., Steeb, P., Zhu, L., van Geldern, R., Mackensen, A. and Schwalb, A.: Stable isotope and ostracode species assemblage evidence for lake level changes of Nam Co, southern Tibet, during the past 600years, Quaternary International, 212(1), 2–13, doi:10.1016/j.quaint.2008.12.010, 2010.

Finnigan MAT 252 isotope ratio mass spectrometer coupled to a Kiel II carbonate preparation device

chronological; resolution; isotope effects caused by different carbonate phases

Zhao, Cheng , Yu, Zicheng , Zhao, Yan , Ito, Emi , Kodama, Kenneth P. , Chen, Fahu

Holocene millennial-scale climate variations documented by multiple lake-level proxies in sediment cores from Hurleg Lake, Northwest China

Zhao, C., Yu, Z., Zhao, Y., Ito, E., Kodama, K. P. and Chen, F.: Holocene millennial-scale climate variations documented by multiple lake-level proxies in sediment cores from Hurleg Lake, Northwest China, Journal of Paleolimnology, 44(4), 995–1008, doi:10.1007/s10933-010-9469-6, 2010.

Kiel automated device for isotope ratio mass spectrometry on a Finnegan Delta XL,

D18O variations reflect changing water balance between groudwater inflow and water loss by evaporation (wet-dry cycles).High effective moisture supports more westerly storm trajectories and increased moisture delivery to the central Interior Yukon.

Recent observations of lake-water d18O, lake level, river discharge, and climate variations, suggest that changes in regional effective moisture (precipitation minus evaporation) are reflected by the lakes hydrologic balance. The observations indicate that the lake is currently 18O-enriched by summer evaporation and that during years of increased precipitation, when groundwater inflow rates to the lake increase, lakewater d18O values decrease.

Lake carbonatepermil18O records from the Yukon Territory, Canada: Little Ice Age moisture variability and patterns

Anderson, L., Finney, B. P. and Shapley, M. D.: Lake carbonate-δ18O records from the Yukon Territory, Canada: Little Ice Age moisture variability and patterns, Quaternary Science Reviews, 30(7-8), 887–898, doi:10.1016/j.quascirev.2011.01.005, 2011.

Optical microscopy and SEM imaging were used to verify sample purity

Check symbols in isotopeInterpretation2 section (GF); missing IntegrationTime units. -BK

Therefore, the Challa ?18Odiatom record is tuned to the underlying processes of local precipitation and, especially, seasonal evaporative losses from the lake surface, only modifi ed by small temperature effects.

An adjustment of ?0.2?/i¿½C increases d18Odiatom by 1? from 25 ka to 16 ka and by 0.5? during the late-glacial period and Younger Dryas, values still less than that during the late Holocene (Fig. 3).

Barker, P. A. , Hurrell, E. R. , Leng, M. J. , Wolff, C. , Cocquyt, C. , Sloane, H. J. , Verschuren, D.

Seasonality in equatorial climate over the past 25 k.y. revealed by oxygen isotope records from Mount Kilimanjaro

Barker, P. A., Hurrell, E. R., Leng, M. J., Wolff, C., Cocquyt, C., Sloane, H. J. and Verschuren, D.: Seasonality in equatorial climate over the past 25 k.y. revealed by oxygen isotope records from Mount Kilimanjaro, Geology, 39(12), 1111–1114, doi:10.1130/g32419.1, 2011.

SEM of calcite crystals to identify contamination by detrital limestone

d18O.precipitation over tropical South America controlled by Raleigh-type fractionation (see Vuille & Werner 2005)

primarily controlled by intensity of South America summer monsoon

exclusion of all other possible influencing processes (see Bird et al. 2011)

also Bird et al. (2011b) - http://www.pnas.org/content/108/21/8583.abstract

Bird, Broxton W. , Abbott, Mark B. , Rodbell, Donald T. , Vuille, Mathias

Holocene tropical South American hydroclimate revealed from a decadally resolved lake sediment ?18O record

Bird, B. W., Abbott, M. B., Rodbell, D. T. and Vuille, M.: Holocene tropical South American hydroclimate revealed from a decadally resolved lake sediment δ18O record, Earth and Planetary Science Letters, 310(3-4), 192–202, doi:10.1016/j.epsl.2011.08.040, 2011.

Complete replacement of the winter Indian monsoon source with a southeasterly/northwesterly source would deplete ?Dwax by about 35?, which is the amplitude of change observed between the mega- droughts interval and the Holocene. / "Relatively depleted ?Dwax values at Lake Malawi from ~3.1 ka to present likely reflect the modern hydrological controls on ?Dprecip, with source changes constituting a more limited role than the amount effect and overall intensity of the hydrological cycle. "

depends (orbital timescale: More Indian Monsoon moisture-->more enriched. Since 3ka: Indian source has been stable, so amount effect dominates: more rainfall, more intense hydrological cycle -->More depleted)

Leaf wax dD reflects "...variations in the ?D of precipitation (?Dprecip) through time in many systems (Hou et al., 2008; Huang et al., 2004). Observational data and isotope-enabled climate models indicate that ?Dprecip reflects the integrated atmospheric history of a water parcel, including source region, transport history, and convective, evaporative, and distillation processes." / "The Lake Malawi ?Dwax likely reflects the ?D of precipitation and associated changes in precipitation and vapor transport, not bio- synthetic or temperature effects."

Relatively depleted dDwax values at Lake Malawi from ~3.1 ka to present likely reflect the modern hydrological controls on dDprecip, with source changes constituting a more limited role than the amount effect and overall intensity of the hydrological cycle.

stratigraphic tie to piston core dated by varve counting and 210Pb

Konecky, Bronwen L. , Russell, James M. , Johnson, Thomas C. , Brown, Erik T. , Berke, Melissa A. , Werne, Josef P. , Huang, Yongsong

Atmospheric circulation patterns during late Pleistocene climate changes at Lake Malawi, Africa

Konecky, B. L., Russell, J. M., Johnson, T. C., Brown, E. T., Berke, M. A., Werne, J. P. and Huang, Y.: Atmospheric circulation patterns during late Pleistocene climate changes at Lake Malawi, Africa, Earth and Planetary Science Letters, 312(3-4), 318–326, doi:10.1016/j.epsl.2011.10.020, 2011.

The isotopic composition of this calcite [endogenic calcite in macrophyte coatings] is approximately in equilibrium with lake waters,

The isotopic composition of the Triassic limestone bedrock is characterized by relatively low oxygen isotope values (between -4.0 and -6.0%; average d18Ocalcite = -5.3%)...samples from units 6, 5 and 3 show d18Ocalcite values (-7.1% to -3.2%) similar to the isotopic signal of the bedrock (-4.6% to -5.2%), indicating a dominant clastic origin of the carbonate.

In the absence of contamination sources [units 1,2 4a and 4b], the two primary factors controlling d18Ocalcite values are moisture balance (precipitation minus evaporation) and the isotopic composition of lake waters (Griffiths et al. 2002)

Morellon, Mario , Valero-Garces, Blas , Gonzalez-Samperiz, Penelope , Vegas-Vilarrubia, Teresa , Rubio, Esther , Rieradevall, Maria , Delgado-Huertas, Antonio , Mata, Pilar , Romero, Oscar , Engstrom, Daniel R. , Lopez-Vicente, Manuel , Navas, Ana , Soto, Jesus

Climate changes and human activities recorded in the sediments of Lake Estanya (NE Spain) during the Medieval Warm Period and Little Ice Age

Morellon, M., Valero-Garces, B., Gonzalez-Samperiz, P., Vegas-Vilarrubia, T., Rubio, E., Rieradevall, M., Delgado-Huertas, A., Mata, P., Romero, O., Engstrom, D. R., Lopez-Vicente, M., Navas, A. and Soto, J.: Climate changes and human activities recorded in the sediments of Lake Estanya (NE Spain) during the Medieval Warm Period and Little Ice Age, Journal of Paleolimnology, 46(3), 423–452, doi:10.1007/s10933-009-9346-3, 2009.

automated carbonate preparation device (KIEL-III) coupled to a gas-ratio mass spectrometer (Finnigan MAT 252).

Sediment characterization by X-ray diffractometry was completed at the University of Pittsburgh?s Materials Micro-Characterization Laboratory using a Phillips X?Pert Powder Diffractometer over a 2? range of 10?80�. X-ray diffraction results indicate that calcite is the only detectable mineral in the fine-grained, carbonate sediment at Lime Lake.

Sediment sampleswere disaggregated for approximately 24 h in 7% H2O2 solution and sieved
at 63 μm to isolate authigenic (i.e., precipitated in-lake) carbonate material
and to limit contamination by biogenic carbonate shell material. The captured
<63 μm fraction of the sediment was settled from rinse water and then
centrifuged, and the remaining liquid was decanted. The resulting fine grained
 carbonate sediment was bleached (using a 50% bleach, 50% water
 solution), rinsed three times using deionized water, freeze-dried, and homogenized
using an agate mortar and pestle.

Our results indicate that during the Medieval Climate Anomaly (MCA) (900-1300 AD) the Pacific Northwest experienced exceptional wetness in winter and that during the Little Ice Age (LIA) (1450-1850 AD) conditions were drier, contrasting with hydroclimatic anomalies in the desert Southwest and consistent with climate dynamics related to the El Nii¿½o Southern Oscillation (ENSO) and the Pacific Decadal Oscillation (PDO).

Castor Lake water and sediment oxygen isotope values are primarily influenced by catchment water balance variations resulting from precipitation-evaporation forcing; To establish a meteoric water baseline for the Castor Lake record, we mean centered the independently dated (SI Appendix, Table S1) Lime Lake ?18O data and subtracted these variations from the mean centered Castor Lake ?18O values (Figs. 2 and 3) thereby isolating the isotopic influence of hydrologic forcing on the Castor lake-catchment system (8). The resulting ??18O record represents the cumulative isotopic effects of evaporation

Nelson, D. B. , Abbott, M. B. , Steinman, B. , Polissar, P. J. , Stansell, N. D. , Ortiz, J. D. , Rosenmeier, M. F. , Finney, B. P. , Riedel, J.

Drought variability in the Pacific Northwest from a 6,000-yr lake sediment record

Nelson, D. B., Abbott, M. B., Steinman, B., Polissar, P. J., Stansell, N. D., Ortiz, J. D., Rosenmeier, M. F., Finney, B. P. and Riedel, J.: Drought variability in the Pacific Northwest from a 6,000-yr lake sediment record, Proceedings of the National Academy of Sciences, 108(10), 3870–3875, doi:10.1073/pnas.1009194108, 2011.

Previous studies have shown it has a simple carbonate mineralogy (low-magnesium calcite,w0.26% Mg; J.M. Russell, unpubl. data; Bessems, 2007)

a negative excursion in the d18Ocarb profiles suggests reduced evaporative concentration of lake water. Although it is not straightforward to compare carbonate with water d18O values, d18O values are more similar to groundwater (c. 2&; K. Mills & J.M. Russell, unpubl. data), in contrast to current lake water values indicating net evaporation (values between A¾2 and A¾4&; K. Mills & J.M. Russell, unpubl. data).'

Ryves, David B. , Mills, Keely , Bennike, Ole , Brodersen, Klaus Peter , Lamb, Angela L. , Leng, Melanie J. , Russell, James M. , Ssemmanda, Immaculate

Environmental change over the last millennium recorded in two contrasting crater lakes in western Uganda, eastern Africa (Lakes Kasenda and Wandakara)

Ryves, D. B., Mills, K., Bennike, O., Brodersen, K. P., Lamb, A. L., Leng, M. J., Russell, J. M. and Ssemmanda, I.: Environmental change over the last millennium recorded in two contrasting crater lakes in western Uganda, eastern Africa (Lakes Kasenda and Wandakara), Quaternary Science Reviews, 30(5-6), 555–569, doi:10.1016/j.quascirev.2010.11.011, 2011.

Agilent GC 6890, Delta Plus XL IRMS via pyrolysis interface at 1445C

We interpret dDwax in the Challa sedimentary record as a proxy the strength of the ?East African Monsoon (EAM)?, in the sense that the monsoon strength is defined by zonal wind speed velocities during the two rainy seasons (OND and MAM).

Vegetation and humidity effects are negligble, "Thus, we assume in this study that dDwax represents mean annual dDP." ... "Instrumental measurements of the isotopic composition of East African precipitation are correlated with 850 hPa zonal wind speeds in the central Indian Ocean (5 Ne5 S, 60 Ee90 E), with stronger zonal wind speed resulting in more depleted precipitation (Vuille et al., 2005). Isotope-enabled modeling experiments confirm that shifts in zonal wind speed in the Indian Ocean e such as those that might occur during an IOZM event or during a strong Indian summer monsoon e result in isotopically-depleted rainfall throughout East Africa (Vuille et al., 2005)."

Notes to isotope interpretation parameter 1: (1) Zonal wind speed is implied to impact both rainfall amounts and moisture source, though not explicitly stated. (2) Note that zonal wind speeds in the paper refer to easterly (onshore) transport, opposite of the conventional "u wind" parameter where stronger u = stronger westerly wind.

Tierney, Jessica E. , Russell, James M. , Sinninghe Damsti¿½, Jaap S. , Huang, Yongsong , Verschuren, Dirk

Late Quaternary behavior of the East African monsoon and the importance of the Congo Air Boundary

Tierney, J. E., Russell, J. M., Sinninghe Damste, J. S., Huang, Y. and Verschuren, D.: Late Quaternary behavior of the East African monsoon and the importance of the Congo Air Boundary, Quaternary Science Reviews, 30(7-8), 798–807, doi:10.1016/j.quascirev.2011.01.017, 2011.

identified as in situ calcite by Scanning Electron Microscopy  (SEM) and analyses by Energy Dispersive Spectroscopy (EDS) that indicated rhombic crystal growth structures composed of nearly pure calcite"

"continuous intervals of 0.25 cm from 0 to 5 cm depth,   at 1.0 cm intervals from 5 to 69 cm depth and at spaced   intervals of 2.0 cm from 69 to 300 cm depth"

The middle to late Holocene d18O record corresponds with records of El Nii¿½o Southern Oscillation intensification that supports a teleconnection between Rocky Mountain climate and North Pacific sea-surface temperatures at decade to century time scales.

Drought periods (i.e., drier winters and/or a more rain-dominated seasonal precipitation balance) generally correspond with higher calcite d18O values, and vice-versa;although lake-water values are currently observed to change  through the ice-free season from ?16.7? to ?13.5? (n= 10), the late summer values are artificially elevated (inset of Fig. 3.).The lower, early summer values are similar to average weightedprecipitation-?18O, and similar to values inferred from near-surface  calcite-?18O prior to 1953 (see Fig. 3 in Anderson, 2011). It is on this basis that variations in through-flowing Bison Lake water-?18O are interpreted as precipitation-?18O and changes in the ratio of the seasonal precipitation balance between snowfall-dominated ?18O) and rainfall-dominated (higher ?18O).

Rocky Mountain hydroclimate: Holocene variability and the role of insolation, ENSO, and the North American Monsoon

Anderson, L.: Rocky Mountain hydroclimate: Holocene variability and the role of insolation, ENSO, and the North American Monsoon, Global and Planetary Change, 92-93, 198–208, doi:10.1016/j.gloplacha.2012.05.012, 2012.

Drought periods (i.e., drier winters and/or a more rain-dominated seasonal precipitation balance) generally correspond with higher calcite d18O values, and vice-versa;although lake-water values are currently observed to change  through the ice-free season from ?16.7? to ?13.5? (n= 10),  the late summer values are artificially elevated (inset of Fig. 3.).  The lower, early summer values are similar to average weighted  precipitation-?18O, and similar to values inferred from near-surface  calcite-?18O prior to 1953 (see Fig. 3 in Anderson, 2011). It is on  this basis that variations in through-flowing Bison Lake water-?18O are interpreted as precipitation-?18O and changes in the ratio of the seasonal precipitation balance between snowfall-dominated  ?18O) and rainfall-dominated (higher ?18O).

Variations in Yellow Lake past lake-water-?18O are interpreted in two ways. When the basin was over-flowing, past lake-water-?18O values are interpreted similarly to  Bison Lake that is in terms of the seasonal balance of precipitation.  When the basin closed, past lake-water-?18O values are interpreted  as secondary effects of summer evaporation: higher lake-water ?18O values reflect more summer evaporation, or less effective moisture  (precipitation?evaporation), whereas lower values reflect less evapo-  ration, or increased effective moisture.

Trace metal analysis indicates that ostracods are generally formed of low-Mg calcite

Australian ostracods precipitate calcite with approximately an 0.7 permil increase in d18O relative to their source water (Chivas et al., 2002). Large isotopic shifts (up to 8?)  preserved in this record suggest that any intra- or inter-species variability is significantly dampened

The rates of change of enrichment and depletion of both d18O and d13C (with respect to VPDB) are rapid, indicating large and rapid changes in the lake water due to variations in E/P.

Australian ostracods precipitate calcite with approximately an 0.7 ? increase in ?18O relative to their source water (Chivas et al., 2002). Large isotopic shifts (up to 8?)  preserved in this record suggest that any intra- or inter-species variability is significantly dampened

Increased seasonality (hotter and drier summers, cool wet winters) lead to periods of increased E/P, and increased variability in ostracod ?18O.

Gouramanis, C. , Dodson, J. , Wilkins, D. , De Deckker, P. , Chase, B.M.

Holocene palaeoclimate and sea level fluctuation recorded from the coastal Barker Swamp, Rottnest Island, south-western Western Australia

Gouramanis, C., Dodson, J., Wilkins, D., De Deckker, P. and Chase, B. M.: Holocene palaeoclimate and sea level fluctuation recorded from the coastal Barker Swamp, Rottnest Island, south-western Western Australia, Quaternary Science Reviews, 54, 40–57, doi:10.1016/j.quascirev.2012.05.007, 2012.

Finnigan MAT 251 mass spectrometer with a Kiel microcarbonate device

Selected samples were submitted for mineral identification by a random powder XRD method using a D500 Siemens X-ray diffractometer with ?/2? geometry, a curved graphite monochromator, a scintillation detector, and Cu K? radiation

Sample preparation followed methods described in De Deckker (1982)

Kemp, Justine , Radke, Lynda C. , Olley, Jon , Juggins, Steve , De Deckker, Patrick

Holocene lake salinity changes in the Wimmera, southeastern Australia, provide evidence for millennial-scale climate variability

Kemp, J., Radke, L. C., Olley, J., Juggins, S. and De Deckker, P.: Holocene lake salinity changes in the Wimmera, southeastern Australia, provide evidence for millennial-scale climate variability, Quaternary Research, 77(1), 65–76, doi:10.1016/j.yqres.2011.09.013, 2012.

Sediment samples were disaggregated for approximately 24 h in 7% H2O2 solution and sieved at 63 μm to isolate authigenic (i.e., precipitated in-lake) carbonate material and to limit contamination by biogenic carbonate shell material. The captured <63 μm fraction of the sediment was settled from rinse water and then centrifuged, and the remaining liquid was decanted. The resulting fine grained carbonate sediment was bleached (using a 50% bleach, 50% water solution), rinsed three times using deionized water, freeze-dried, and homogenizedsing an agate mortar and pestle.

Lime Lake d18O values, however, are controlled by the isotopic composition of meteoric water (i.e., rain and snowfall), which is influenced by the origin of atmospheric moisture, air mass trajectory, Rayleigh distillation, and air temperature

Steinman, B. A. , Abbott, M. B. , Mann, M. E. , Stansell, N. D. , Finney, B. P.

1,500 year quantitative reconstruction of winter precipitation in the Pacific Northwest

Steinman, B. A., Abbott, M. B., Mann, M. E., Stansell, N. D. and Finney, B. P.: 1,500 year quantitative reconstruction of winter precipitation in the Pacific Northwest, Proceedings of the National Academy of Sciences, 109(29), 11619–11623, doi:10.1073/pnas.1201083109, 2012.

Sediment samples
were disaggregated for approximately 24 h in 7% H2O2 solution and sieved

We interpret the Renner-Lime Lake ??18O record as a proxy for winter precipitation amounts. Note that the Renner- Lake ??18O dataset was produced by mean centering the two records and subtracting the latter from the former (i.e., the same method used to produce the Castor-Lime Lake ??18O dataset).

HP 6890 GC, AS 200 autosampler, Finnigan MAT Delta+ XL mass spectrometer

Leaf wax hydrogen isotopes exhibit a surprising amount of variability at the sub-decadal scale (Fig. 6). This high degree of variability indicates that leaf waxes are likely produced, transported and deposited in a relatively short period of time.

integrationtime info should be moved to Sensor Integration time columns? Also, check that integration time is 1-10yrs with uncertainty of 10 years? -BK

The remarkable similarity between d2Hwax and regional temperature indicates that d2Hwax is a useful proxy to reconstruct temper- ature at decadal- to sub-centennial-resolution.

The major source of water for plants in the Arctic, where permafrost precludes extensive groundwater systems, is precipitation, either as snowmelt or summer rain (Elberling et al. 2008). Thus, we hypothesize that d2Hwax in the Arctic is likely closely related to d2Hprecip. Leaf wax synthesis occurs during the summer months when plants are neither temper- ature- nor light-limited. The apparent fractionation (e) between leaf waxes and source waters varies with relative humidity (RH) and with potential evapotrans- piration (Sachse et al. 2012). Long-term average growing season (June, July, August) RH at Clyde River is 80% (Environment Canada, 2011). The eleven-month dataset from Silasiutitalik at the head of Clyde Inlet suggests that growing season RH is slightly lower inland, around 75% (Kangiqtugaapik (Clyde River) Weather Station Network, 2011). The n-alkanoic acids synthesized by plants that grow at 70?80% RH have an e of -100 to -120% relative to annual mean precipitation (Hou et al. 2008). The d2Hwax values from Ayr Lake sediments (-240 to -265 %) therefore suggest that source water d2H should range between -140 to -165% (assuming an e of -100%) and -120 to -145% (assuming an e of -120%). These calculated source water d2H values are within the range of measured summer d2Hprecip values for both Pond Inlet and Hall Beach, although the values obtained with the larger e are close to the maximum summer d2Hprecip values for Pond Inlet. We therefore hypothesize that plants in this catchment utilize summer precipitation as their main water source (Fig. 2). Variability in summer d2Hprecip, or utilization of small but varying amounts of winter precipitation, is likely driving variability in d2Hwax at Ayr Lake.

Bottom line: more snowmelt providing source water to plants causes pool of plant source water to be more 2H-depleted. "The major source of water for plants in the Arctic, where permafrost precludes extensive groundwater systems, is precipitation, either as snowmelt or summer rain (Elberling et al. 2008). Thus, we hypothesize that d2Hwax in the Arctic is likely closely related to d2Hprecip. Leaf wax synthesis occurs during the summer months when plants are neither temper- ature- nor light-limited. The apparent fractionation (e) between leaf waxes and source waters varies with relative humidity (RH) and with potential evapotrans- piration (Sachse et al. 2012). Long-term average growing season (June, July, August) RH at Clyde River is 80% (Environment Canada, 2011). The eleven-month dataset from Silasiutitalik at the head of Clyde Inlet suggests that growing season RH is slightly lower inland, around 75% (Kangiqtugaapik (Clyde River) Weather Station Network, 2011). The n-alkanoic acids synthesized by plants that grow at 70?80% RH have an e of -100 to -120% relative to annual mean precipitation (Hou et al. 2008). The d2Hwax values from Ayr Lake sediments (-240 to -265 %) therefore suggest that source water d2H should range between -140 to -165% (assuming an e of -100%) and -120 to -145% (assuming an e of -120%). These calculated source water d2H values are within the range of measured summer d2Hprecip values for both Pond Inlet and Hall Beach, although the values obtained with the larger e are close to the maximum summer d2Hprecip values for Pond Inlet. We therefore hypothesize that plants in this catchment utilize summer precipitation as their main water source (Fig. 2). Variability in summer d2Hprecip, or utilization of small but varying amounts of winter precipitation, is likely driving variability in d2Hwax at Ayr Lake."

Pond Inlet: 72°42'N, 77°57'W 33 m asl; Hall Beach: 68°46'N, 81°13'W 1 m asl

GNIP, IAEA; http://www.iaea.org/water, 10.1007/s10933-012-9584-7

Thomas, E. K., McGrane, S., Briner, J. P. and Huang, Y.: Leaf wax δ2H and varve-thickness climate proxies from proglacial lake sediments, Baffin Island, Arctic Canada, Journal of Paleolimnology, 48(1), 193–207, doi:10.1007/s10933-012-9584-7, 2012.

Pisidiidae shell fragments (between 1 and 5) were crushed and treated with H2O2 for 30 min to remove organic material. The samples were then rinsed three times with deionized water. Aliquots (*100 lg) were weighed for isotopic analysis

Subsequent to*3,000 cal yr BP, Quartz Lake became a relatively closed system, with isotopic characteristics of progressively stronger evaporative influence

The cause of the transition to closed-basin conditions may have been geomorphic rather than climatic (but probably less important after 2ka)

The lake-water data from Quartz Lake indicate
evaporation during the ice-free season is a substantial
influence on the d18O values of water from the site
today. For instance, the d18O and dD values of the
surface-water samples fall on a regional evaporative
line (REL) with a slope of 4.94, deviating largely from
the GMWL (Fig. 2)

Wooller, Matthew J. , Kurek, Joshua , Gaglioti, Benjamin V. , Cwynar, Les C. , Bigelow, Nancy , Reuther, Joshua D. , Gelvin-Reymiller, Carol , Smol, John P.

Wooller, M. J., Kurek, J., Gaglioti, B. V., Cwynar, L. C., Bigelow, N., Reuther, J. D., Gelvin-Reymiller, C. and Smol, J. P.: An ~11,200 year paleolimnological perspective for emerging archaeological findings at Quartz Lake, Alaska, Journal of Paleolimnology, 48(1), 83–99, doi:10.1007/s10933-012-9610-9, 2012.

Thermo Trace GC, ConFlo IV interface, Thermo Delta V isotope ratio mass spectrometer

not interpreted to reflect climate (note by Iso2k compiler: dD precip does not change seasonally in this part of Greenland, likely because source areas are proximal and carry relatively enriched moisture to this region throughout the year)

Winter snow melting during growing season. "dD values of long-chain n-alkanes (dDwax) reflect dD of water used by terrestrial vegetation after modification by biosynthetic processes (Sachse et al., 2012 and references therein). Soil moisture provides the source water for terrestrial plants, while lake water is the source for aquatic macrophytes and algae. dD of water in soils can be modified to some extent from dD of annual precipitation by evaporation. However, it has been shown that dDwax is unaltered by plants following leaf formation and therefore reflects dDwater used during leaf flush (Kahmen et al., 2011; Sachse et al., 2010; Tipple et al., 2013). In the Arctic, the majority of leaf formation takes place in late spring/early summer following the return of appreciable sunlight. Because snowmelt is the predominant water source available to plants at the time of leaf formation, the dDwax is potentially biased toward wintertime dDp (i.e. snowfall months). In Tasiilaq, the difference between precipitation-weighted annual average dDp (?92?) and precipitation- weighted average dDp during months with below zero average temperatures (October-April; ?96?) is negligible (Bowen, 2008; Cappelen et al., 2011), and thus, any changes in the timing of leaf formation during the Holocene, or in the seasonality of precipitation, are unlikely to have had much impact on dDwax."

Needs entry for isotopeInterpretation1_name. Inferred material is missing.

The extent of isotopic enrichment of surface waters from meteoric water is determined by the degree of evaporative enrichment of the water body (Leng and Anderson, 2003). Therefore, ... the ?D of lipids produced by aquatic plants (?Daq) tracks the degree of evaporative isotopic enrichment of lake water from meteoric water...."The relatively D-enriched values (more positive ?D) of ?D25 and ?D27 are consistent with our interpretation that these compounds reflect isotopically enriched lake water."

dD values of long-chain n-alkanes (dDwax) reflect dD of water used by terrestrial vegetation after modification by biosynthetic processes (Sachse et al., 2012 and references therein). Soil mois- ture provides the source water for terrestrial plants, while lake water is the source for aquatic macrophytes and algae. dD of water in soils can be modified to some extent from dD of annual precipitation by evaporation. However, it has been shown that dDwax is unaltered by plants following leaf formation and there- fore reflects dDwater used during leaf flush (Kahmen et al., 2011; Sachse et al., 2010; Tipple et al., 2013). In the Arctic, the majority of leaf formation takes place in late spring/early summer follow- ing the return of appreciable sunlight. Because snowmelt is the predominant water source available to plants at the time of leaf formation, the dDwax is potentially biased toward wintertime dDp (i.e. snowfall months). In Tasiilaq, the difference between precipitation-weighted annual average dDp (?92?) and precipitation- weighted average dDp during months with below zero average temperatures (October-April; ?96?) is negligible (Bowen, 2008; Cappelen et al., 2011), and thus, any changes in the timing of leaf formation during the Holocene, or in the seasonality of precipita- tion, are unlikely to have had much impact on dDwaxd

Needs entry for isotopeInterpretation1_name (GF). Inferred material is missing. ET: duplicate of LS13BAFLC

dD values of long-chain n-alkanes (dDwax) reflect dD of water used by terrestrial vegetation after modification by biosynthetic processes (Sachse et al., 2012 and references therein). Soil moisture provides the source water for terrestrial plants, while lake water is the source for aquatic macrophytes and algae. dD of water in soils can be modified to some extent from dD of annual precipitation by evaporation. However, it has been shown that dDwax is unaltered by plants following leaf formation and therefore reflects dDwater used during leaf flush (Kahmen et al., 2011; Sachse et al., 2010; Tipple et al., 2013). In the Arctic, the majority of leaf formation takes place in late spring/early summer following the return of appreciable sunlight. Because snowmelt is the predominant water source available to plants at the time of leaf formation, the dDwax is potentially biased toward wintertime dDp (i.e. snowfall months). In Tasiilaq, the difference between precipitation-weighted annual average dDp (?92?) and precipitation- weighted average dDp during months with below zero average temperatures (October-April; ?96?) is negligible (Bowen, 2008; Cappelen et al., 2011), and thus, any changes in the timing of leaf formation during the Holocene, or in the seasonality of precipita- tion, are unlikely to have had much impact on dDwaxd

?D values of long-chain n-alkanes (?Dwax) reflect ?D of water used by terrestrial vegetation after modification by biosynthetic processes (Sachse et al., 2012 and references therein). Soil mois- ture provides the source water for terrestrial plants, while lake water is the source for aquatic macrophytes and algae. ?D of water in soils can be modified to some extent from ?D of annual precipitation by evaporation. However, it has been shown that ?Dwax is unaltered by plants following leaf formation and there- fore reflects ?Dwater used during leaf flush (Kahmen et al., 2011; Sachse et al., 2010; Tipple et al., 2013). In the Arctic, the majority of leaf formation takes place in late spring/early summer follow- ing the return of appreciable sunlight. Because snowmelt is the predominant water source available to plants at the time of leaf formation, the ?Dwax is potentially biased toward wintertime ?Dp (i.e. snowfall months). In Tasiilaq, the difference between precip- itation-weighted annual average ?Dp (?92?) and precipitation- weighted average ?Dp during months with below zero average temperatures (October?April; ?96?) is negligible (Bowen, 2008; Cappelen et al., 2011), and thus, any changes in the timing of leaf formation during the Holocene, or in the seasonality of precipita- tion, are unlikely to have had much impact on ?Dwax.

GNIP data for Groennedal and Prins Christians Sund, near the study site

Groennedal: 61.22°N, 48.12°W, 27 m asl; Prins Christians Sund: 60.03°N 43.12°W, 76 m asl

Balascio, N. L. , DAndrea, W. J. , Bradley, R. S. , Perren, B. B.

Biogeochemical evidence for hydrologic changes during the Holocene in a lake sediment record from southeast Greenland

Balascio, N. L., D’Andrea, W. J., Bradley, R. S. and Perren, B. B.: Biogeochemical evidence for hydrologic changes during the Holocene in a lake sediment record from southeast Greenland, The Holocene, 23(10), 1428–1439, doi:10.1177/0959683613493938, 2013.

dDprecip reflects Australasian monsoon strength based on modern precipitation isotope data from nearby station (Bali). "At Bali, the closest isotopic monitoring site to Lake Lading, over 80% of precipitation measured from July 2003 to June 2006 fell between October and March (61% during Novembera€“February), coinciding with the southernmost extension of the ITCZ associated with summer intensification of the Australasian monsoon (Figure 1c). The weighted Octo- bera€“March average dDprecip during that time period was 18.72%, similar to the weighted annual (Julya€“June) average of 20.42%, reflecting the strong control of wet season dDprecip on the annual average dDprecip [Kurita et al., 2009]. While large-scale changes in atmospheric circulation could certainly cause the relationship between precipitation amount and dDprecip to vary, these modern observations indicate that dDprecip reflects Australasian monsoon strength."

Because plant waxes are produced year-round, we interpret dDwax to record weighted annual dDprecip, which is highly influenced by variations in the Australasian monsoon.

Daily precipitation amount and dD were measured during 2003–2006 as part of campaign by JAMSTEC.

Kurita, N., Ichiyanagi, K., Matsumoto, J., Yamanaka, M. D., & Ohata, T. (2009). The relationship between the isotopic content of precipitation and the precipitation amount in tropical regions. Journal of Geochemical Exploration, 102(3), 113–122.

Konecky, Bronwen L. , Russell, James M. , Rodysill, Jessica R. , Vuille, Mathias , Bijaksana, Satria , Huang, Yongsong

Intensification of southwestern Indonesian rainfall over the past millennium

Konecky, B. L., Russell, J. M., Rodysill, J. R., Vuille, M., Bijaksana, S. and Huang, Y.: Intensification of southwestern Indonesian rainfall over the past millennium, Geophysical Research Letters, 40(2), 386–391, doi:10.1029/2012gl054331, 2013.

; archiveType changed  was originally Lake sediment (LS); archiveType changed  was originally Lake sediment (LS)

I just moved this from the Rejected list  not sure why it was there and not herepermil Age model An et al. (2012)

Lu, Y., An, C., Wang, Z., Zhao, J., Wei, J., Wei, H., Tao, S., Huang, W, Ma, M.

Lu, Y., An, C., Wang, Z., Zhao, J., Wei, H., Tao, S., Huang, W. and Ma, M.: Mid-Holocene climate change in the eastern Xinjiang region indicated by the grain size and stable isotope record from Lake Barkol, northwest China, Environmental Earth Sciences, 68(8), 2163–2169, doi:10.1007/s12665-012-1899-1, 2012.

dual-inlet GV Instruments, Ltd. IsoPrime? stable isotope ratio mass spectrometer equipped with a dual inlet, MultiPrep? module and Gilson autosampler

Aggregates of ~30 adult ostracod carapaces of the genus Physocypria, with no evidence of corrosion, were isolated from sediment for oxygen isotope analysis at 1?2 cm intervals. Ostracod valves were soaked in 15 % H2O2, cleaned ultrasonically in deionized water, rinsed with methanol and dried at 60�C for 12 hours

More specifi cally, the ostracod-based oxygen isotope record from El Gancho, Nicaragua, indicates that wetter conditions prevailed from as early as ca. A.D. 600 until the end of the MCA, ca. A.D. 1250. An abrupt shift toward arid conditions occurred during the ~150 yr interval between the MCA and the LIA, and was followed by a generally drier climate that has persisted until present

Oxygen isotope values of El Gancho surface water samples are enriched by ~8? relative to local meteoric water (Fig. 3), indicating substantial water loss through both evaporation and nonfractionating outfl ow pathways (i.e., overfl ow and outseepage through the lake bed), and a resulting lake water isotopic sensitivity to changes in hydrologic balance. isotopic and hydrologic modeling supports these assertions, indicating that precipitation [amount] is the principle control on El Gancho lake water !18O values. For example, in response to modeled precipitation changes of i¿½50%, El Gancho exhibited water and ostracod !18O increases of >1.5? and decreases of >1.0?, respectively; largely as a result of hydrologic control of the proportions of water lost through evaporation and overfl ow (Table DR5).

Methodology detail at ftp://rock.geosociety.org/pub/reposit/2013/2013037.pdf

Stansell, N. D. , Steinman, B. A. , Abbott, M. B. , Rubinov, M. , Roman-Lacayo, M.

Lacustrine stable isotope record of precipitation changes in Nicaragua during the Little Ice Age and Medieval Climate Anomaly

Stansell, N. D., Steinman, B. A., Abbott, M. B., Rubinov, M. and Roman-Lacayo, M.: Lacustrine stable isotope record of precipitation changes in Nicaragua during the Little Ice Age and Medieval Climate Anomaly, Geology, 41(2), 151–154, doi:10.1130/g33736.1, 2013.

The effective moisture (ratio of precipitation to evaporation) is considered as the main factor controlling the ?D values of lipid n-alkanes in terrestrial plants (Polissar and Freeman, 2010). In a previous study, the ?D record from a loess profile in the Chinese Loess Plateau displayed a strong correlation to changes in the magnetic susceptibility (MS) over the past 130 ka, and the isoto- pic variation was thought to be strongly affected by aridity (Liu and Huang, 2005). Furthermore, a humidity control experiment in the field verified the correlation between D enrichment and rela- tive humidity (McInerney et al., 2011). A study of lipids from the Santa Barbara Basin from the past 1400 years also revealed the ?D of mid-chain acids to be partially correlated with existing data of drought severity (Li et al., 2011).

Variation in vegetation type (shrubs and grass) is the main factor influencing the [d2H of leaf waxes in] sediments of Lake Sugan, because of the dD values of Chenopodiceae shrubs are higher than those of grasses. We can still discuss the moisture history using the hydrogen-isotope record, because the vegetation type would be consistent with hydrological condition. [i.e., Chenopodiaceae shrubs tend to be more abundant in dry climates, and Chenopodiaceae shrubs have a smaller apparent fractionation, so dry climates would not only cause greater evaporative enrichment of plant source water, but more leaf waxes with relatively enriched d2H would be produced by Chenopodiaceae shrubs.] In the arid area of western China, vegetation type is controlled by moisture changes (Wu, 2011).  The authors conclude that variations in vegetation type (shrub or grass), which are caused by moisture changes, are the main factor controlling the δD records in the study area.

The effective moisture (ratio of precipitation to evaporation) is considered as the main factor controlling the ?D values of lipid n-alkanes in terrestrial plants (Polissar and Freeman, 2010). In a previous study, the ?D record from a loess profile in the Chinese Loess Plateau displayed a strong correlation to changes in the magnetic susceptibility (MS) over the past 130 ka, and the isoto- pic variation was thought to be strongly affected by aridity (Liu and Huang, 2005). Furthermore, a humidity control experiment in the field verified the correlation between D enrichment and relative humidity (McInerney et al., 2011). A study of lipids from the Santa Barbara Basin from the past 1400 years also revealed the dD of mid-chain acids to be partially correlated with existing data of drought severity (Li et al., 2011).

The effective moisture (ratio of precipitation to evaporation) is considered as the main factor controlling the dD values of lipid n-alkanes in terrestrial plants (Polissar and Freeman, 2010). In a previous study, the dD record from a loess profile in the Chinese Loess Plateau displayed a strong correlation to changes in the magnetic susceptibility (MS) over the past 130 ka, and the isoto- pic variation was thought to be strongly affected by aridity (Liu and Huang, 2005). Furthermore, a humidity control experiment in the field verified the correlation between D enrichment and relative humidity (McInerney et al., 2011). A study of lipids from the Santa Barbara Basin from the past 1400 years also revealed the dD of mid-chain acids to be partially correlated with existing data of drought severity (Li et al., 2011).

A 1700-year n-alkanes hydrogen isotope record of moisture changes in sediments from Lake Sugan in the Qaidam Basin, northeastern Tibetan Plateau

Wang, Z., Liu, W., Liu, Z., Wang, H., He, Y. and Zhang, F.: A 1700-year n-alkanes hydrogen isotope record of moisture changes in sediments from Lake Sugan in the Qaidam Basin, northeastern Tibetan Plateau, The Holocene, 23(9), 1350–1354, doi:10.1177/0959683613486941, 2013.

Late Glacial and Holocene record of climatic change in the southern Rocky Mountains from sediments in San Luis Lake, Colorado, USA

Yuan, F., Koran, M. R. and Valdez, A.: Late Glacial and Holocene record of climatic change in the southern Rocky Mountains from sediments in San Luis Lake, Colorado, USA, Palaeogeography, Palaeoclimatology, Palaeoecology, 392, 146–160, doi:10.1016/j.palaeo.2013.09.016, 2013.

These lines of evidence strongly suggest that conditions favor- able for B. braunii growth occur during moderate-to-strong El Nin?o events and thus that C34 botryococcene ?D records the hydrologic conditions of the lake during these events. In contrast, the avail- able evidence suggests that the dinoflagellate population persists throughout the varying hydrologic conditions experienced by El Junco Lake and thus that sedimentary dinosterol ?D records the long-term (decadal-to-centennial) mean lake conditions.

AA: This record is a duplicate of LS14ZHJU (and is a shorter version of the latter record). This study's unique record is dinosterol d2H, which LS14ATJU01A.

From this paper: "In particular, conditions favorable for B. braunii blooms are thought to occur during El Nin?o events in association with three distinct processes that promote olig- otrophic conditions and lake stratification. Firstly, the heavy rains associated with moderate-to-strong El Nin?o events are thought to dilute the nutrient pool and cause oligotrophic conditions. El Junco Lake is an endorheic lake (with the exception of occasional overflow conditions and possibly seepage) located within a caldera with a small catchment area consisting only of the narrow crater rim (Conroy et al., 2008). In such lakes the con- centration of nutrients tend to decrease as lake levels increase through dilution of the incoming nutrients (Smol et al., 2001; Magyari et al., 2009). Because monthly rainfall in this area can be an order of magnitude higher during strong El Nin?o events as com- pared to non-El Nin?o periods (cf., Fig. 4) and the lake has been re- ported to overflow during strong El Nin?o events, considerable dilu- tion and flushing of nutrients likely occur during these times. Sec- ondly, reduced nutrient input to the lake exacerbates oligotrophic conditions during strong El Nin?o events. A major source of nutri- ents to the lake is thought to be guano deposited directly into the lake by the large number of seabirds that frequent it (Colinvaux, 1968). Such a predominance of avian-derived nutrients has been documented in a number of lake systems (Manny et al., 1994; Marion et al., 1994). However, during strong El Nin?o events, this nutrient source is diminished as the Gala?pagos seabird population plummets in response to the massive fish die-offs associated with a deep thermocline and low ocean productivity in the EEP (Gibbs, 1987). Finally, El Nin?o events in the EEP are associated with con- ditions that increase water column stability and lake stratification, including warmer air temperatures, reduced cloud cover, and re- duced trade wind strength (Lewis Jr., 1983; O?Reilly et al., 2003; Ndebele-Murisa et al., 2010; Co?zar et al., 2012), conditions which have been shown to exacerbate nutrient depletion in the surface of oligotrophic lakes (O?Reilly et al., 2003). Increases in water column stability during El Nin?o events should further promote favorable conditions for the oil-rich, colony-forming B. braunii due to their buoyancy. In various lo- cations across the globe, B. braunii blooms have been strongly linked to increases in water column stability due to both their tolerance of oligotrophic conditions and their anti-sinking strategy (Kebede and Belay, 1994; Souza et al., 2008; Winder and Hunter, 2008). In particular, in a Columbian lake with conditions (including depth, pH, conductivity, and nutrient concentration) comparable to El Junco Lake, B. braunii blooms have been found to occur dur- ing the annual flood stage in association with nutrient flushing, oligotrophic conditions, and lake stratification (Pinilla, 2006), con- ditions that closely mimic moderate to strong El Nin?o events in El Junco Lake. These lines of evidence strongly suggest that conditions favor- able for B. braunii growth occur during moderate-to-strong El Nin?o events and thus that C34 botryococcene ?D records the hydrologic conditions of the lake during these events."

All botryococcene dD values were highly correlated with water dD values (R2>0.99). And, Zhang and Sachs 2007, Organic Geochemistry, 38: 582-608.

changes in rainfall amount are imprinted in the isotopic composition of botryococcenes, with negative (posi- tive) ?D values co-occurring with wetter (drier) periods.

Semipreparative HPLCMS to isolate dinosterol, which was then acetylated and injected on a GC, Delta V IRMS system. From Supplemental Methods: "Hydrogen isotope measurements of dinosterol were performed on a Finnigan Delta V Plus Isotope Ratio Mass Spectrometer (IRMS) coupled to a Thermo Trace GC Ultra with a Varian VF17ms FactorFour capillary column (60 m x 0.32 mm x 0.25 ?m) and a pyrolysis reactor according to the methods described in Atwood and Sachs (2012). Samples were injected into a split/splitless inlet in splitless mode at 310 �C. The oven temperature was ramped from 100 �C to 220 �C at a rate of 20 �C/min, then at 2 �C /min up to 325 �C where it was held for 17 min. The carrier gas, He, was held constant at 2.6 mL/min. The pyroloysis reactor was maintained at 1400 �C. Isotope values, expressed as ?D values, were calculated in Isodat software relative to VSMOW using a coinjection standard containing nC32, nC40, and nC44 of known ?D values (obtained from A. Schimmelmann, Indiana University, Bloomington, IN, USA). The measured isotope values of dinosterol were corrected for the addition of hydrogen atoms (of known ?D value) that occurred during acetylation. Triplicate analyses were typically performed on each sample and mean values and standard deviations reported. Instrument performance was evaluated using H2 reference gas and a prepared standard of nalkanes of known ?D values."

In closed (endorheic) lakes, lake water dD is driven by the ratio of precipitation to evaporation and the isotopic value of the precipitation which, in the tropics, is strongly negatively correlated with the amount of precipitation on monthly and longer timescales. The combination of these processes amplifies the response of lake water dD to changes in rainfall with lower (higher) dD values occurring during periods of wetter (drier) conditions. Changes in rainfall patterns can therefore be reconstructed from dD values of sedimentary algal lipids, due to the near perfect correlation between water dD and algal lipid dD values.

"In closed (endorheic) lakes, lake water dD is driven by the ratio of precipitation to evaporation and the isotopic value of the precipitation which, in the tropics, is strongly negatively correlated with the amount of precipitation on monthly and longer timescales. The combination of these processes amplifies the response of lake water dD to changes in rainfall with lower (higher) dD values occurring during periods of wetter (drier) conditions. Changes in rainfall patterns can therefore be reconstructed from dD values of sedimentary algal lipids, due to the near perfect correlation between water dD and algal lipid dD values."

Atwood, A. R. and Sachs, J. P.: Separating ITCZ- and ENSO-related rainfall changes in the Galapagos over the last 3 kyr using D/H ratios of multiple lipid biomarkers, Earth and Planetary Science Letters, 404, 408–419, doi:10.1016/j.epsl.2014.07.038, 2014.

Downcore variation involved subtle changes in distribution, C22 and C24 covarying and suggesting a similar source, perhaps partially aquatic, with an increase in recent decades perhaps related to indirect fertilization of the lake (Fig. 5a).

Rapid transfer from plant to sediment is likely within the small, steep-sided watershed, suggesting that the leaf wax record would be capable of reconstructing up to decadal resolution variation in leaf wax dD values.

These changes in moisture source have been further linked to SST anomalies (SSTa) in the Kuroshio Extension region of the N Pacific, which exerts steering on atmo- spheric circulation and hence moisture sources to the west coast of N America. ... These positive excursions may be linked to warm Kuroshio Extension SSTa, driv- ing greater amplitude waves in the circulation over the N Pacific entraining subtropical moisture sources but generally associated with drier conditions in coastal southern California. Conversely negative isotopic excursions centered on 300 and 800 yr BP may correspond to more N Pacific moisture flux and wetter conditions in coastal southern California, the former of these perhaps associ- ated with the Little Ice Age. In combination with other proxies recording wet/dry climate regime shifts, the information on mois- ture source from precipitation isotopes may thus be particularly helpful in understanding the dynamical causes of hydroclimate shifts. Warm SST anomaly --> less moisture flux -->more enriched precipitation. "Elevated dD values indi- cate more (sub)tropical moisture sources and/or drier conditions, whereas lower dD values are consistent with N Pacific moisture sources and/or more antecedent precipitation. "

Moisture flux from the subtropical North Pacific (driven by SST anomalies in the Kuroshio Extension region)

SEASONALITY: "First, during water uptake, plants are expected to sample the spring growing season precipitation, at the end of the wet season [October-March], as the temperature warms up and before the dry summer months (Feakins and Sessions, 2010; Kahmen et al., 2011; Tipple et al., 2013). During this time, the plants may record the isotopic signature of just a few storms each year heightening variability; however, sedimentary samples integrating a decade might average the signal from > 20 storms. " PARAMETER: "Paleoclimatic interpretation of the precipitation isotopic history recorded in the Crystal Cave has been suggested to record changes in moisture source primarily and local amount effect secondarily (McCabe-Glynn et al., 2013). ... Our record provides an extension of the Crystal Cave isotopic record, from a more southerly coastal location, but likely also records interdecadal variability in the same processes. ... We suggest that the plant leaf wax record preferentially captures spring precipitation isotopic anomalies integrated over decades, providing a sensitive record of atmospheric circulation and moisture source changes. "

SEASONALITY: "First, during water uptake, plants are expected to sample the spring growing season precipitation, at the end of the wet season [October-March], as the temperature warms up and before the dry summer months (Feakins and Sessions, 2010; Kahmen et al., 2011; Tipple et al., 2013). During this time, the plants may record the isotopic signature of just a few storms each year heightening variability; however, sedimentary samples integrating a decade might average the signal from > 20 storms. " PARAMETER: "Paleoclimatic interpretation of the precipitation isotopic history recorded in the Crystal Cave has been suggested to record changes in moisture source primarily and local amount effect secondarily (McCabe-Glynn et al., 2013). ... Our record provides an extension of the Crystal Cave isotopic record, from a more southerly coastal location, but likely also records interdecadal variability in the same processes."

Secondly, plant community changes in the catchment (or other ecological changes) may influence the dD record. Vegetation changes could reasonably have an influence on the mean catchment ewax/precip that lasts for decades, so this mecha- nism might operate too slowly to explain sample-to-sample vari- ability in the sediment, although it may contribute to the multi- decadal variability. We observed abundance variation in homo- logues downcore (Fig. 5), which could be consistent with ecological changes influencing dD values; however, the non-unique chain length distributions of different plant species (Bush and McIner- ney, 2013) make it impossible to draw unique solutions here.

Of all the homologues presented in this study, C28 is used for paleoclimate interpretation: "Of all the homologues (Fig. 7a), C26 and C28 showed the most coherent and reliable evidence for terrigenous vegetation sources downcore, and we relied on C28 for paleoclimate reconstruction as before (Feakins et al., 2012)."

Feakins, Sarah J. , Kirby, Matthew E. , Cheetham, Michael I. , Ibarra, Yadira , Zimmerman, Susan R.H.

Feakins, S. J., Kirby, M. E., Cheetham, M. I., Ibarra, Y. and Zimmerman, S. R. H.: Fluctuation in leaf wax D/H ratio from a southern California lake records significant variability in isotopes in precipitation during the late Holocene, Organic Geochemistry, 66, 48–59, doi:10.1016/j.orggeochem.2013.10.015, 2014.

Agilent 6890 GC, pyrolysis at 1440C, Thermo Scientific DeltaV Plus

SASM precipitation that falls on the Altiplano is ultimately derived from Atlantic Ocean moisture that has been transported across the Amazon Basin and lifted over the eastern cordillera of the Andes. Altiplano ?Dp thus integrates upstream effects including rainout and moisture recycling over the Amazon Basin, altitude effects associated with upslope moisture transport, and local effects such as the intensity of precipitation (?amount effect?) (Dansgaard, 1964). ... "Increased rainout along this trajectory, as well as increased local precipitation in the Andes, results in more depleted ?Dp, consistent with the continentality and amount effects that dominate ?Dp variability throughout most of tropical South America (Vuille et al., 2003). Accordingly, the intensity of the SASM is significantly negatively correlated with ?18O (and correspondingly ?D) of modern precipitation in the Cen- tral Andes, as well as throughout much of southern tropical South America (Vuille and Werner, 2005).

Results from both observational and modeling studies suggest that the dominant control on modern interannual Andean ?Dp variability is Rayleigh-type fractionation during rainout along the trajectory of moist air masses across the Amazon Basin up to the Andes (e.g., Rozanski et al., 1993; Hoffmann et al., 2003; Vimeux et al., 2005; Vuille and Werner, 2005). Increased rainout along this trajectory, as well as increased local precipitation in the Andes, results in more depleted ?Dp, consistent with the continentality and amount effects that dominate ?Dp variability throughout most of tropical South America (Vuille et al., 2003).

While the isotopic composition of precipitation appears to be the primary control on the structure of the LT ?Dwax record, it is clear that secondary effects also contribute to this signal. Most notably, the much larger range at LT (102h) than at Illimani (58h) over the past 19 kyr suggests the influence of compounding effects on LT ?Dwax, such as decreased regional precipitation, resulting in a more enriched ?Dp, and low local humidity, which would tend to further enrich plant source water by soil water evaporation and/or leaf transpiration. Since such local evapotranspiration feedbacks would be expected to act in step with ?Dp changes, this would serve to amplify the ?Dwax signal and increase its sensitivity to ?Dp variability.

Fornace, Kyrstin L. , Hughen, Konrad A. , Shanahan, Timothy M. , Fritz, Sherilyn C. , Baker, Paul A. , Sylva, Sean P.

A 60,000-year record of hydrologic variability in the Central Andes from the hydrogen isotopic composition of leaf waxes in Lake Titicaca sediments

Fornace, K. L., Hughen, K. A., Shanahan, T. M., Fritz, S. C., Baker, P. A. and Sylva, S. P.: A 60,000-year record of hydrologic variability in the Central Andes from the hydrogen isotopic composition of leaf waxes in Lake Titicaca sediments, Earth and Planetary Science Letters, 408, 263–271, doi:10.1016/j.epsl.2014.10.024, 2014.

Indian source: "Sacred Lake currently receives no Atlantic-derived precipi- tation, and its elevation, northeastern slope exposure, and rainfall seasonality make it particularly susceptible to changes in the Indian Ocean monsoons. In contrast, equatorial lakes in central Kenya (e.g. Lake Naivasha) and the western Rift Valley (e.g. Lake Edward, Uganda/ Congo) receive a mixture of Indian- and Atlantic-derived moisture, and hence are sensitive to both monsoons (Nicholson, 1996). " Moisture transport and temperature influence: "The strength of low-level equatorial westerlies in the Indian Ocean has been linked to East African lake levels as well as Mt. Kenyas glaciers, with stronger (weaker) winds inhibiting (enhanc- ing) precipitation in East Africa (Hastenrath, 2001). Overall, these west- erlies have increased in strength since the 1880s. This important Indian Ocean forcing may explain Sacred Lakes particular sensitivity to these changes, and recent drying may have also been locally enhanced by a re- cent rise in temperature (via an upward shift in the ZMR and/or in- creased evaporation of soil water)"

In East Africa, stable isotopes in modern precipitation have been shown to reflect large-scale atmospheric circulation processes (Vuille et al., 2005), and the ?18O of precipitation (and by inference, the ?D of precipitation) on Mt. Kenya has been shown to be a good indicator of moisture balance (Barker et al., 2001). Leaf wax ?D reflects ?Dprecip, after a series of offsets due to soil water evaporation, fractionation of leaf water relative to xylem water, and biosynthesis (Sachse et al., 2012).

Air temperature has 2 influences: "air temperature is important for the elevation of the zone of maximum rainfall (ZMR) on Mt. Kenya" and for soil/lake evaporation. "Recent drying may have also been locally enhanced by a recent rise in temperature (via an upward shift in the ZMR and/or increased evaporation of soil water)."

Konecky, Bronwen , Russell, James , Huang, Yongsong , Vuille, Mathias , Cohen, Lily , Street-Perrott, F. Alayne

Impact of monsoons, temperature, and CO2 on the rainfall and ecosystems of Mt. Kenya during the Common Era

Konecky, B., Russell, J., Huang, Y., Vuille, M., Cohen, L. and Street-Perrott, F. A.: Impact of monsoons, temperature, and CO2 on the rainfall and ecosystems of Mt. Kenya during the Common Era, Palaeogeography, Palaeoclimatology, Palaeoecology, 396, 17–25, doi:10.1016/j.palaeo.2013.12.037, 2014.

climate impact of the Westerlies was apparently not only restricted to the summer season but also significant during winter as indicated by recurrent episodes of enhanced allochthonous input through snowmelt

previously published inferrences: fraction reflects evapotranspiration during the growing season

δDn-C29 record of the Son Kol sediments can be used to infer information about past summer moisture conditions.

Aquatic samples with asterisks were corrected for the hardwater effect prior to calibration

Revised for Iso2k by D. Kaufman from original file: Sonk11D.Lauterbach.2014

Climatic imprint of the mid-latitude Westerlies in the Central Tian Shan of Kyrgyzstan and teleconnections to North Atlantic climate variability during the last 6000 years

Lauterbach, S., Witt, R., Plessen, B., Dulski, P., Prasad, S., Mingram, J., Gleixner, G., Hettler-Riedel, S., Stebich, M., Schnetger, B., Schwalb, A. and Schwarz, A.: Climatic imprint of the mid-latitude Westerlies in the Central Tian Shan of Kyrgyzstan and teleconnections to North Atlantic climate variability during the last 6000 years, The Holocene, 24(8), 970–984, doi:10.1177/0959683614534741, 2014.

integrationTime "uncertainty type" given but no time units. delete? -BK

The moisture variations at Sasikul Lake are consistent with the records in the westerlies-dominated Central Asian and northern Tibetan Plateau, suggesting regionally coherent changes in atmospheric circulation during at least the past millennium.

Lei, Y. , Tian, L. , Bird, B. W. , Hou, J. , Ding, L. , Oimahmadov, I. , Gadoev, M.

A 2540-year record of moisture variations derived from lacustrine sediment (Sasikul Lake) on the Pamir Plateau

Lei, Y., Tian, L., Bird, B. W., Hou, J., Ding, L., Oimahmadov, I. and Gadoev, M.: A 2540-year record of moisture variations derived from lacustrine sediment (Sasikul Lake) on the Pamir Plateau, The Holocene, 24(7), 761–770, doi:10.1177/0959683614530443, 2014.

Finnigan GasBench II with carbonate option coupled to a DELTA plus XL mass spectrometer

Prasad, Sushma , Anoop, A. , Riedel, N. , Sarkar, S. , Menzel, P. , Basavaiah, N. , Krishnan, R. , Fuller, D. , Plessen, B. , Gaye, B. , Ri¿½hl, U. , Wilkes, H. , Sachse, D. , Sawant, R. , Wiesner, M.G. , Stebich, M.

Prolonged monsoon droughts and links to Indo-Pacific warm pool: A Holocene record from Lonar Lake, central India

Prasad, S., Anoop, A., Riedel, N., Sarkar, S., Menzel, P., Basavaiah, N., Krishnan, R., Fuller, D., Plessen, B., Gaye, B., Roehl, U., Wilkes, H., Sachse, D., Sawant, R., Wiesner, M. G. and Stebich, M.: Prolonged monsoon droughts and links to Indo-Pacific warm pool: A Holocene record from Lonar Lake, central India, Earth and Planetary Science Letters, 391, 171–182, doi:10.1016/j.epsl.2014.01.043, 2014.

GasBench II linked to a MAT-253 ThermoFisher Scientific isotope ratio mass spectrometer.

general isotopic composition of the lake water follows the decreasing solar insolation over ~4200 yrs.

chronological; resolution; biological effects (for samples < 1 yr old)

Periodically low d18O and d13C values from individual subsamples

Taft, Linda , Mischke, Steffen , Wiechert, Uwe , Leipe, Christian , Rajabov, Ilhomjon , Riedel, Frank

Taft, L., Mischke, S., Wiechert, U., Leipe, C., Rajabov, I. and Riedel, F.: Sclerochronological oxygen and carbon isotope ratios in Radix (Gastropoda) shells indicate changes of glacial meltwater flux and temperature since 4,200 cal yr BP at Lake Karakul, eastern Pamirs (Tajikistan), Journal of Paleolimnology, 52(1-2), 27–41, doi:10.1007/s10933-014-9776-4, 2014.

Late Quaternary water depth changes in Hala Lake, northeastern Tibetan Plateau, derived from ostracod assemblages and sediment properties in multiple sediment records

Yan, D. and Wuennemann, B.: Late Quaternary water depth changes in Hala Lake, northeastern Tibetan Plateau, derived from ostracod assemblages and sediment properties in multiple sediment records, Quaternary Science Reviews, 95, 95–114, doi:10.1016/j.quascirev.2014.04.030, 2014.

Trace GC with PTV inlet in splitless mode, 30m DB-5 capillary column (J&W Scientific) with 0.25mm i.d. and 0.25 lm film, and was operated at a constant helium flow rate of 1 ml/min. The oven temperature pro- gram differed for each lipid class. For hydrocarbons, the starting temperature was 90 °C, rising to 230 °C at 13 °C/min, then to 325 °C at 5.5 °C/min, followed by 13 min at 325 °C. Effluent from the GC entered the GC-C III interface, a graphite-lined ceramic tube at 1400 °C, where quantitative pyrolysis to graphite, hydrogen gas and carbon monoxide occurred (Bur- goyne and Hayes, 1998). The hydrogen gas stream was introduced to the Finnigan Deltaplus XP mass spectrometer via an open split, where a flow of helium carried the H2 gas into the mass spectrometer.

El Junco Lake is presumed to have remained fresh and therefore its lake-water dD value is dictated solely by the isotopic composition of precipitation, and the relative rates of evaporation and precipitation. More negative lake-water dD values reflect a greater rate of rainfall relative to evaporation during wet periods. Conclusions of the paper are about moisture balance (P-E) in the tropical Pacific.

It is expected that dD values of botryococcene will decline when precipitation rates increase, possibly providing a metric for the severity of extreme rainfall events that are associated with El Nino events. (All botryococcene dD values were highly correlated with water dD values (R2>0.99). And, Zhang and Sachs 2007, Organic Geochemistry), 38: 582-608.

El Niño evolution during the Holocene revealed by a biomarker rain gauge in the Galápagos Islands

Zhang, Z., Leduc, G. and Sachs, J. P.: El Nino evolution during the Holocene revealed by a biomarker rain gauge in the Galapagos Islands, Earth and Planetary Science Letters, 404, 420–434, doi:10.1016/j.epsl.2014.07.013, 2014.

It is notable that the periods of d18O enrichment in the core are in agreement with the high relative abundance of the epiphytic, algal symbiont Sorites orbiculus and "The d13C values of Elphidium striatopunctatum co-vary, with d18O values indicating a warm, evaporative basin, where degassing of CO2 from the water leads to the concentration of 13C (Abu-Zied et al., 2011c; Lamb et al., 2002; Leng and Marshall, 2004). Therefore, the values of d18O and d13C were used as an evaporation index in the Shuaiba Lagoon."

14C dates calibrated using Intcal09 curve (Heaton et al., 2009; Reimer et al., 2009)

Palaeoenvironment, palaeoclimate and sea-level changes in the Shuaiba Lagoon during the late Holocene (last 3.6 ka), eastern Red Sea coast, Saudi Arabia

Abu-Zied, R. H. and Bantan, R. A.: Palaeoenvironment, palaeoclimate and sea-level changes in the Shuaiba Lagoon during the late Holocene (last 3.6 ka), eastern Red Sea coast, Saudi Arabia, The Holocene, 25(8), 1301–1312, doi:10.1177/0959683615584204, 2015.

"We used a Thermo Scientificdegrees Trace gas chromato graph equipped with an Rxi5ms column (30 m degrees 0.25 mm, film thickness 1 permilm) and a programmable temperature va porizing (PTV) injector operated in solvent split mode with an evaporation temperature of 60 permil C. The GC was con nected via a GC Isolink with pyrolysis/combustion furnace (at 1400/1000 permilC) and a Conflo IV interface to a DeltaVPlus isotope ratio mass spectrometer. The H+3 factor (Sessions et al., 2001) was determined daily to test measurement linearity of the system and accounted for 5.8 ppm mvpermil1 on average. Reference peaks of H2 bracket nalkanoic acid peaks during the course of a GCIRMS run; two of these peaks were used for the standardization of the isotopic analysis, while the remainders were treated as unknowns to assess pre cision. Except for the case of coelution, precision of these replicates was better than 0.6 permil."

Since temperature and precipitation amounts are anticor- related on an interannual timescale (Fig. 5), we interpret low ?D values to indicate both relatively cool and wet conditions. In addition to fluctuations in mean annual precipitation iso- topes, snowmelt and delivery to plants may vary. We suggest that a high proportional contribution of water derived from snowmelt, after relatively long and wet winters with high amounts of snowfall, can further lead to more negative ?D leaf wax values.

mainly growing season, with potential addition effects of snowmelt following wet winters

Higher isotopic values in the summer compared to the winter (Yao et al., 2013; Bowen and Revenaugh, 2003) suggest that monthly values are indeed driven by temperature. If these seasonal controls also determine interannual variations in the isotopic composition of precipitation then temperature is likely to be a major factor explaining the reconstructed hydrogen isotopic variability. A higher percentage of growing season rainfall (relative to total water used by plants) would result in higher deltaD values.

Higher isotopic values in the summer compared to the winter (Yao et al., 2013; Bowen and Revenaugh, 2003) suggest that monthly values are indeed driven by temperature. If these seasonal controls also determine interannual variations in the isotopic composition of precipitation then temperature is likely to be a major factor explaining the reconstructed hydrogen isotopic variability. A higher percentage of winter snowmelt (relative to total water used by plants) would result in lower deltaD values.

This amount effect lowers the summer precipitation isotopic com- position, dampens the seasonality of the mean precipitation of isotopic values and lowers the integrated annual precip- itation isotopic composition. Hence, in drier years average ?D values will be D-enriched relative to wetter years, and likewise warmer years will be D-enriched relative to colder years (Fig. 4b). Given the low precipitation amounts in this arid region today, the amount effect is likely to remain sec-ondary to the temperature controls on isotopic composition apparent in the seasonal cycle.

Aichner, B. , Feakins, S. J. , Lee, J. E. , Herzschuh, U. , Liu, X.

Highresolution leaf wax carbon and hydrogen isotopic record of the late Holocene paleoclimate in arid Central Asia

Aichner, B., Feakins, S. J., Lee, J. E., Herzschuh, U. and Liu, X.: High-resolution leaf wax carbon and hydrogen isotopic record of the late  Holocene paleoclimate in arid Central Asia, Climate of the Past, 11(4), 619–633, doi:10.5194/cp-11-619-2015, 2015.

We inspected samples to verify the absence of shells or large grains of calcite

changed IntegrationTime uncertainty type to "resolution" but should probably be "Chronological." Though, note that resolution doesn't really need to be in here because it can be calculated from the age model.-BK

We interpret changes in d18O as indicative of changes in the ratio of evaporation and precipitation (E/P)

Bhattacharya, Tripti , Byrne, Roger , Bahnel, Harald , Wogau, Kurt , Kienel, Ulrike , Ingram, B. Lynn , Zimmerman, Susan

Cultural implications of late Holocene climate change in the Cuenca Oriental, Mexico

Bhattacharya, T., Byrne, R., Boehnel, H., Wogau, K., Kienel, U., Ingram, B. L. and Zimmerman, S.: Cultural implications of late Holocene climate change in the Cuenca Oriental, Mexico, Proceedings of the National Academy of Sciences, 112(6), 1693–1698, doi:10.1073/pnas.1405653112, 2015.

lake residence time move to sensor/archiveIntegration Time? also, changed "approx 10 years" to "10" -BK

Dean, Jonathan R. , Jones, Matthew D. , Leng, Melanie J. , Noble, Stephen R. , Metcalfe, Sarah E. , Sloane, Hilary J. , Sahy, Diana , Eastwood, Warren J. , Roberts, C. Neil

Eastern Mediterranean hydroclimate over the late glacial and Holocene, reconstructed from the sediments of Nar lake, central Turkey, using stable isotopes and carbonate mineralogy

Dean, J. R., Jones, M. D., Leng, M. J., Noble, S. R., Metcalfe, S. E., Sloane, H. J., Sahy, D., Eastwood, W. J. and Roberts, C. N.: Eastern Mediterranean hydroclimate over the late glacial and Holocene, reconstructed from the sediments of Nar lake, central Turkey, using stable isotopes and carbonate mineralogy, Quaternary Science Reviews, 124, 162–174, doi:10.1016/j.quascirev.2015.07.023, 2015.

"Thermo Trace2000 GC equipped with an SGE SolGel-1ms column (60 m  0.25 mm  0.25 lm) and a PTV injector coupled to a Finnigan MAT 253 stable isotope mass spectrometer and a Finnigan GC combustion III interface. The H3+ factor was measured daily prior to dD analysis, with a mean value for the measurement peri- ods of 15.6 ± 0.3 (1r). An external FAME isotope standard (Mix F8, Indiana University Biogeochemical Laboratories) and an internal laboratory isotope standard, measured after every four to six sample analyses, were used to standardize and normalize sample isotope values. The precision of the standard analyses was 6±5& for dD analyses and 6±0.5& for d13C analyses. Most samples were run in duplicate or triplicate for both hydrogen and carbon isotope analysis, and the reported isotope ratio values are averages of replicate runs. Insufficient abundances for some long-chain FAME samples prevented replicate dD analyses."

Past variability in ?Dwax-corr reflects the combined effects of evaporative enrichment of soil and plant water D/H ratios and temporal variability in the isotopic composition of pre- cipitation, which, in this region, is primarily controlled by the amount effect (8, 27)...Therefore we interpret ?Dwax-corr values as a qualitative indicator of past water availability.

In the modern Maya Lowlands, ?Dwax is well correlated with precipitation amount and varies by 60? across an annual precipitation gradient of 2,500 mm (Fig. 2).

This modern variability in dDwax is strongly influenced by soil water evaporation (17), and it is possible that changes in potential evapotranspiration could also impact paleo records.

Physiological differences between plant groups also result in differing ?Dwax values between C3 trees and shrubs and C4 grasses (16), and we use ?13Cwax records to correct for the influence of vegetation change on ?Dwax values (25) (?Dwax-corr, SI Text and Fig. S1).

This modern variability in ?Dwax is strongly influenced by soil water evaporation (17), and it is possible that changes in potential evapotranspiration could also impact paleo records.

Douglas, Peter M. J. , Pagani, Mark , Canuto, Marcello A. , Brenner, Mark , Hodell, David A. , Eglinton, Timothy I. , Curtis, Jason H.

Drought, agricultural adaptation, and sociopolitical collapse in the Maya Lowlands

Douglas, P. M. J., Pagani, M., Canuto, M. A., Brenner, M., Hodell, D. A., Eglinton, T. I. and Curtis, J. H.: Drought, agricultural adaptation, and sociopolitical collapse in the Maya Lowlands, Proceedings of the National Academy of Sciences, 112(18), 5607–5612, doi:10.1073/pnas.1419133112, 2015.

no IntegrationTime given, but units/type are given. please clarify-BK

The carbonate isotope values also show an up core trend to more positive values with a particularly marked step in d13C values at 125 cm from ~-3 per mil to ~+2 per mil, in part explained by the shift in mineralogy; aragonite is 1.9 per mil (0.6 per mil) more positive in d13C (d18O) compared with calcite precipitated in waters with the same temperature and isotopic composition (Grossman, 1984; Grossman and Ku, 1986). Oxygen and hydrogen isotope ratios of the lake waters collected in 2007 show a clear evaporative signal (Supplementary Figure 1, available online), and d18O trends to more positive values likely represents a shift to more evaporative dominant conditions given the associated change from calcite to aragonite (e.g. Jones et al., 2006).

Jones, M. D. , Djamali, M. , Holmes, J. , Weeks, L. , Leng, M. J. , Lashkari, A. , Alamdari, K. , Noorollahi, D. , Thomas, L. , Metcalfe, S. E.

Human impact on the hydroenvironment of Lake Parishan, SW Iran, through the late-Holocene

Jones, M. D., Djamali, M., Holmes, J., Weeks, L., Leng, M. J., Lashkari, A., Alamdari, K., Noorollahi, D., Thomas, L. and Metcalfe, S. E.: Human impact on the hydroenvironment of Lake Parishan, SW Iran, through the late-Holocene, The Holocene, 25(10), 1651–1661, doi:10.1177/0959683615594242, 2015.

Modern lakewater defines a local evaporation line (LEL) distinct from global meteoric water line (GMWL) .

Age model based on 6 14C ages and correlated (see Wagner et al 2012)

Lacey, Jack H. , Francke, Alexander , Leng, Melanie J. , Vane, Christopher H. , Wagner, Bernd

A high-resolution Late Glacial to Holocene record of environmental change in the Mediterranean from Lake Ohrid (Macedonia/Albania)

Lacey, J. H., Francke, A., Leng, M. J., Vane, C. H. and Wagner, B.: A high-resolution Late Glacial to Holocene record of environmental change in the Mediterranean from Lake Ohrid (Macedonia/Albania), International Journal of Earth Sciences, 104(6), 1623–1638, doi:10.1007/s00531-014-1033-6, 2014.

Thermo Finnigan DeltaPlus IRMS linked to a Thermo Finnigan Gasbench II

Samples only used if TIC/TOC > 0.3; samples with very enriched d13C values assumed to have formed diagenetically; SEM-screened to exclude a detrital origin of carbonates

Carbonate record consists of ikaite-derived calcite; Negative correlation between amount of precipitation and west wind intensity (Mayr et al., 2007; Garreaud et al., 2013)

Oehlerich, M. , Mayr, C. , Gussone, N. , Hahn, A. , Holzl, S. , Lucke, A. , Ohlendorf, C. , Rummel, S. , Teichert, B.M.A. , Zolitschka, B.

Lateglacial and Holocene climatic changes in south-eastern Patagonia inferred from carbonate isotope records of Laguna Potrok Aike (Argentina)

Oehlerich, M., Mayr, C., Gussone, N., Hahn, A., Hoelzl, S., Luecke, A., Ohlendorf, C., Rummel, S., Teichert, B. M. A. and Zolitschka, B.: Lateglacial and Holocene climatic changes in south-eastern Patagonia inferred from carbonate isotope records of Laguna Potrok Aike (Argentina), Quaternary Science Reviews, 114, 189–202, doi:10.1016/j.quascirev.2015.02.006, 2015.

GC coupled to Delta V IRMS via pyrolysis interface operated at 1430 degrees C

Located in southern Ghana, the climate of Lake Bosumtwi is heavily influenced by the West African monsoon, which draws moisture onshore from the Gulf of Guineaduring the months of April-October as the monsoon trough migrates northward with the sun (Fig. S2). In winter the winds reverse, and the climate of southern Ghana is influenced by hot, dry northeasterly monsoon winds, which inhibit precipitation over much of North Africa.

As the hydrogen isotopic composition of precipitation in tropical West Africa is controlled mostly by the ?amount effect? (22), ?Dwax values are interpreted here as indicators of changes in wet season precipitation intensity, following corrections for global ice volume and vegetation type (Supplementary Section 2.3 and Fig. 5). Independent support for the ?Dwax record comes from an updated reconstruction of palaeolake-level variations at Lake Bosumtwi (Supplementary Section 2.2; ref. 23).

Shanahan, Timothy M. , McKay, Nicholas P. , Hughen, Konrad A. , Overpeck, Jonathan T. , Otto-Bliesner, Bette , Heil, Clifford W. , King, John , Scholz, Christopher A. , Peck, John

Shanahan, T. M., McKay, N. P., Hughen, K. A., Overpeck, J. T., Otto-Bliesner, B., Heil, C. W., King, J., Scholz, C. A. and Peck, J.: The time-transgressive termination of the African Humid Period, Nature Geoscience, 8(2), 140–144, doi:10.1038/ngeo2329, 2015.

"Thermo Scientific® Trace gas chromato- graph equipped with a Rxi-5ms column (30 m 0.25 mm, film thickness 1 mm) and a programmable temperature vaporizing (PTV) injector operated in solvent split mode with an evaporation tem- perature of 60 C. The GC was connected via a GC Isolink with a pyrolysis furnace (at 1400 C) via a Conflo IV interface to a Del- taVPlus isotope ratio mass spectrometer. The Hþ3 -factor was determined daily to test linearity and accounted for 6.1 ppm mV1 on average. Reference peaks of H2 were co-injected between n- alkanoic acid peaks during the course of a GCeIRMS run; two of these peaks were used for standardization of the isotopic analysis, while the remainders were treated as unknowns to assess preci- sion. Except for the case of co-elution, precision of these replicates was better than 0.6‰. The data were normalized to the VSMOW/ SLAP hydrogen isotopic scale by comparing with an external stan- dard containing 15 n-alkane compounds (C16 to C30) with known dD values obtained from A. Schimmelmann, Bloomington. Indiana University,"

Check inferred material. Should be lake water or soil water. Indicate amount effect in climate variable field. Check:isotopeInterpretation1_name: 'rainfall amount' should be 'P_isotope' if inferred from P_isotope?? G. Falster

The average monthly dD of precipitation in the interior of West Asia is correlated with average monthly precipitation at two meteoro- logical stations located 1365 km to the west and 390 km to the east of the Neor peat mire at the same latitude (Fig. 6).

Transition from the most positive dD values during the Younger Dryas to the most negative dD values during the early Holocene, followed by a return to more positive values during the middle to late Holocene indicate that moisture availability, moisture source, or most likely a combination of both varied between these time periods, with the wettest interval during the early Holocene.

Sharifi, A., Pourmand, A., Canuel, E. A., Ferer-Tyler, E., Peterson, L. C., Aichner, B., Feakins, S. J., Daryaee, T., Djamali, M., Beni, A. N., Lahijani, H. A. K. and Swart, P. K.: Abrupt climate variability since the last deglaciation based on a high-resolution, multi-proxy peat record from NW Iran: The hand that rocked the Cradle of Civilization?, Quaternary Science Reviews, 123, 215–230, doi:10.1016/j.quascirev.2015.07.006, 2015.

SMOW delta Deuterium [per mil SMOW] (dD) * PI: Wirth, Stefanie B (https://orcid.org/0000-0002-1276-8506, stefanie.wirth@alumni.ethz.ch)

Steinman, B. A., Pompeani, D. P., Abbott, M. B., Ortiz, J. D., Stansell, N. D., Finkenbinder, M. S., Mihindukulasooriya, L. N. and Hillman, A. L.: Oxygen isotope records of Holocene climate variability in the Pacific Northwest, Quaternary Science Reviews, 142, 40–60, doi:10.1016/j.quascirev.2016.04.012, 2016.

Lake N3 I´2Haq has a >100a€° range during the past 8 kyr, larger than the range of modern seasonal I´2Hprecip in Disko Bugt (Figures 1 and 2a). We interpret these large changes in I´2Haq to indicate changes in precipitation sea- sonality, with Arctic moisture sources contributing to the exceptionally low I´2H values. The magnitude and direc- tion of I´2Haq changes cannot be explained by changes in terrestrial plant contributions of C24 n-alkanoic acids, by Holocene temperature change, or by lake water residence time (Figures S6 and S7 in the supporting information).Lake N3 I´2Haq decreased steadily from !190 to !300a€° from 7.5 to 6 ka, in step with declining sea ice in Disko Bugt (Figures 2a and 2b) [Ouellet-Bernier et al., 2014]. Lake N3 I´2Haq remained low during the middle Holocene, synchronous with minimum regional sea ice. The Labrador Sea, an important moisture source region for wes- tern Greenland [Sodemann et al., 2008], had minimum sea ice cover from 6.5 to 3.5 ka (Figure 2b) [de Vernal et al., 2013]. Furthermore, sea ice reached a minimum in northern Baffin Bay and the Canadian Arctic from 6 to 3 ka [Ledu et al., 2010; de Vernal et al., 2013], creating a source for moisture that was 2H-depleted compared to mod- ern winter precipitation around Lake N3. Although Baffin Bay still had seasonal sea ice during the middle Holocene, sea ice would have formed later in the year [Markus et al., 2009]. A loss of sea ice during early winter, when evaporation is greatest, can cause large increases in early winter snowfall [Bintanja and Selten, 2014]. Finally, the West Greenland Current was both strong and warm 6 to 4 ka, likely due to an increased contribution of the warm Irminger Current to the West Greenland Current, resulting in regional warmth and providing energy to evaporate more moisture (Figures 2c and 2d) [Perner et al., 2013]. Winter insolation was low during the middle Holocene [Laskar et al., 2004], so there was likely a large contrast between winter air temperature and winter ocean surface temperature. This temperature contrast would cause high evaporation. Thus, we inter- pret the significant middle Holocene depletion of Lake N3 I´2Haq as an increase in winter precipitation, caused by the near total loss of sea ice cover in the Labrador Sea, and the loss of early winter sea ice and increased ocea- nic heat advection in Baffin Bay.

terrestrial plant leaf wax hydrogen isotope, possibly some aquatic waxes

Our interpretation of Lake N3 I´2Hterr as summer temperature is supported in several ways (Figure 3). First, I´2Hterr exhibits similar centennial-scale patterns during the past ~ 300 years as midge-inferred summer temperature anomalies at North Lake, western Greenland (Figure 3c) [Axford et al., 2013]. Coldest conditions in both records correspond with the Little Ice Age and end with warming in recent decades, a pattern also documented in Disko Bugt [Perner et al., 2013]. Second, the centennial-scale variability in Lake N3 I´2Hterr is remarkably similar to the 4 kyr-long record of annual average surface temperature at Greenland Ice Sheet Project 2 (GISP2), Greenland (r2 = 0.43) [Kobashi et al., 2011] (Figure 3b and Figure S5 in the supporting information), suggesting similar con- trols on late Holocene centennial-scale temperature at these sites, desGIte seasonal and elevation differences.

Thomas, Elizabeth K.; Briner, Jason P.; Ryan-Henry, John J.; Huang, Yongsong

A major increase in winter snowfall during the middle Holocene on western Greenland caused by reduced sea ice in Baffin Bay and the Labrador Sea

Thomas, E. K., Briner, J. P., Ryan‐Henry, J. J. and Huang, Y.: A major increase in winter snowfall during the middle Holocene on western Greenland caused by reduced sea ice in Baffin Bay and the Labrador Sea, Geophysical Research Letters, 43(10), 5302–5308, doi:10.1002/2016gl068513, 2016.

When interpreted in conjunction with other proxy records for moisture and aridity, and by controlling for plant type via detailed pollen stratigraphy and Iuapp data for modern plants, d2Hwax can be used to infer changes in moisture source area and transport history.

Thomas, Elizabeth K.; Huang, Yongsong; Clemens, Steven C.; Colman, Steven M.; Morrill, Carrie;  Wegener, Pamela; Zhao, Jiangtao

Changes in dominant moisture sources and the consequences for hydroclimate on the northeastern Tibetan Plateau during the past 32 kyr

Thomas, E. K., Huang, Y., Clemens, S. C., Colman, S. M., Morrill, C., Wegener, P. and Zhao, J.: Changes in dominant moisture sources and the consequences for hydroclimate on the northeastern Tibetan Plateau during the past 32 kyr, Quaternary Science Reviews, 131, 157–167, doi:10.1016/j.quascirev.2015.11.003, 2016.

n-fatty acid C28 [AfAE’A†a€™AfA¢A¢a€sA¬A…A¡AfAE’A¢a‚¬A¡Afa€sA‚Aug/g] (n-C28 FA) * PI: Wirth, Stefanie B (https://orcid.org/0000-0002-1276-8506, stefanie.wirth@alumni.ethz.ch

Carbon, organic, total [%] (TOC) * PI: Wirth, Stefanie B (https://orcid.org/0000-0002-1276-8506, stefanie.wirth@alumni.ethz.ch) * COMMENT: wt%

Computer tomograph value [HU] (CT value) * PI: Wirth, Stefanie B (https://orcid.org/0000-0002-1276-8506, stefanie.wirth@alumni.ethz.ch)

Wirth, S. B. and Sessions, A. L.: Plant-wax D/H ratios in the southern European Alps record multiple aspects of climate variability, Quaternary Science Reviews, 148, 176–191, doi:10.1016/j.quascirev.2016.07.020, 2016.

Thus, for the past ~5000 years of sedimentation, the n- alkanes in Hakluytvatnet (including short-, mid-, and long-chain homologues) derive predominantly from aquatic moss, and their dD values therefore reflect that of lake water.

The hydrogen isotopic composition (D/H; dD using the delta notation) of leaf wax n-al- kanes reflects the D/H of source water used by a plant after modification by evaporation and biosynthetic fractionation (Kahmen et al., 2013a,b; Sachse et al., 2004, 2012), and therefore is useful for paleohydrologic reconstructions. The movement of water through the hydrologic cycle (Dansgaard, 1964), as well as regional and seasonal climatological conditions (Bowen and Revenaugh, 2003), results in variations of stable isotopes (D/H and 18O/16O) of local precipitation. Algae and macrophytes incorporate hydrogen from lake water while terrestrial plants use hydrogen from soil moisture; both water sources are ultimately derived from local precipitation. Therefore, dD of different n-alkanes can be used to reconstruct the climatic factors controlling the isotopic composi- tion of lake water and precipitation (Balascio et al., 2013; Rach et al., 2014).

Balascio, Nicholas L.; D'Andrea, William J.; Gjerde, Marthe; Bakke, Jostein

Hydroclimate variability of High Arctic Svalbard during the Holocene inferred from hydrogen isotopes of leaf waxes

Balascio, N. L., D’Andrea, W. J., Gjerde, M. and Bakke, J.: Hydroclimate variability of High Arctic Svalbard during the Holocene inferred from hydrogen isotopes of leaf waxes, Quaternary Science Reviews, 183, 177–187, doi:10.1016/j.quascirev.2016.11.036, 2018.

Holocene multi-proxy environmental reconstruction from lake Hakluytvatnet, Amsterdamøya Island, Svalbard (79.5°N)

Gjerde, M., Bakke, J., D’Andrea, W. J., Balascio, N. L., Bradley, R. S., Vasskog, K., Olafsdottir, S., Roethe, T. O., Perren, B. B. and Hormes, A.: Holocene multi-proxy environmental reconstruction from lake Hakluytvatnet, Amsterdamoeya Island, Svalbard (79.5°N), Quaternary Science Reviews, 183, 164–176, doi:10.1016/j.quascirev.2017.02.017, 2018.

Please use positive/negative for isotope interpretation direction

we interpret the I´18Ocalcite variations from Lake Nuudsaku as a record of meteoric inputs

Stansell, N.D., Kein, E.S., Finkenbinder, M.S., Fortney, C.S., Dodd, J.P., Tereasmaa, J., Nelson, D.B.

A stable isotope record of Holocene precipitation dynamics in the Baltic region from Lake Nuudsaku, Estonia

Stansell, N. D., Klein, E. S., Finkenbinder, M. S., Fortney, C. S., Dodd, J. P., Terasmaa, J. and Nelson, D. B.: A stable isotope record of Holocene precipitation dynamics in the Baltic region from Lake Nuudsaku, Estonia, Quaternary Science Reviews, 175, 73–84, doi:10.1016/j.quascirev.2017.09.013, 2017.

Late-Holocene variations in our I´18O record display coherent patterns with regional glacier fluctuations at centennial to millennial scales, suggesting that I´18O minima were related to a combination of low temperatures and enhanced winter snowfall

Holocene climatic change in the Alaskan Arctic as inferred from oxygen-isotope and lake-sediment analyses at Wahoo Lake

Vachula, R. S., Chipman, M. L. and Hu, F. S.: Holocene climatic change in the Alaskan Arctic as inferred from oxygen-isotope and lake-sediment analyses at Wahoo Lake, The Holocene, 27(11), 1631–1644, doi:10.1177/0959683617702230, 2017.

MJ: Simple second order polynomila age depth model used from calibrated dates reported in paper

basis for anything to do with the d18O data in this paper is unclear

An 18,000-Year Record of Vegetation, Lake-Level and Climatic Change from Tigalmamine, Middle Atlas, Morocco

Lamb, H. F., Eicher, U. and Switsur, V. R.: An 18,000-Year Record of Vegetation, Lake-Level and Climatic Change from Tigalmamine, Middle Atlas, Morocco, Journal of Biogeography, 16(1), 65, doi:10.2307/2845311, 1989.

d180 values (relative to the PDB standard) in the TIC fraction, in hand-picked carbonate crystals,

6180 values (relative to the PDB standard) in the TIC fraction, in hand-picked carbonate crystals, and in L. ceriotuberosa are shown in Fig. 12b,c. Individual carbonate crystals and the TIC fraction of samples from shallow-lake intervals are isotopically enriched in 180, indicating the importance of evaporative removal of 180-depleted water vapor from the lake relative to the input of 180- depleted streamflow discharge. No 6180 data for ostracodes exist for the shallow-lake intervals since ostracodes were unable to survive the high salinities that characterized these times (Bradbury et al., 1989).

Benson, L. V., Meyers, P. A. and Spencer, R. J.: Change in the size of Walker Lake during the past 5000 years, Palaeogeography, Palaeoclimatology, Palaeoecology, 81(3-4), 189–214, doi:10.1016/0031-0182(91)90147-j, 1991.

move some chronIntegrationTime to Sensor/ArchiveIntegrationTime?-BK

In closed-basin lakes with seasonally dry cliamte, the 18O/16O ratio of lake water is controlled mainly by the ratio of evporatino to precipitation.

Hodell, D.A., Curtis, J.H., Jones, G.A., Higuera-Gundy, A., Brenner, M., Binford, M.W., Dorsey, K.T.

Hodell, D. A., Curtis, J. H., Jones, G. A., Higuera-Gundy, A., Brenner, M., Binford, M. W. and Dorsey, K. T.: Reconstruction of Caribbean climate change over the past 10,500 years, Nature, 352(6338), 790–793, doi:10.1038/352790a0, 1991.

DK: 18O on ostracodes. Another time series is published on gastropods. The two are very similar.

Individual gastropod shells were also picked from every 1-cm interval for stable isotopic analysis. Single specimens of Pyrgophorus coronatus were separated from the sieved 1400 mm fraction under 101 magnification. Gastropod shells were soaked in 15% H2O2 to remove organic matter cleaned and sonicated in deionized water, and ultimately rinsed with methanol before drying. Individual gastropod shells were ground to a fine powder using a mortar and pestle

If the d18O signal is controlled mainly by E/P, then the variation in d18O during the late Holocene suggests repeated multi-decadal wet/dry cycles that are superimposed upon longer-term, millennial patterns of abundant rainfall and drought.

This is demonstrated for Lake Punta Laguna by comparing the measured d18O values of lakewater, rainfall, and groundwater. Local groundwater and rainwater have depleted d18O values of 03.91 and 03.92?, respectively, whereas the lakewater is significantly enriched, averaging 0.93? (Table 3)

Climate Variability on the Yucatan Peninsula (Mexico) during the Past 3500 Years, and Implications for Maya Cultural Evolution

Curtis, J. H., Hodell, D. A. and Brenner, M.: Climate Variability on the Yucatan Peninsula (Mexico) during the Past 3500 Years, and Implications for Maya Cultural Evolution, Quaternary Research, 46(1), 37–47, doi:10.1006/qres.1996.0042, 1996.

Mean d1880c. of replicates from 15 individuals (instars 6 and 7) is 4.60% for the winter 19921993 (15~~0, = 9.5%0) and 4.68% for the winter 19931994 (6permil*OL = 9.50, Table 1). Actual d180c. in both seasons is enriched compared to the isotopic composition of a theoretical calcite formed isotopic equilibrium ( d180eq). The difference is +2.3 2 O.l%o to a 6permil80, calculated using the fractionation factors given by Friedman and OpermilNeil ( 1977) and exactly matches the vital offsets for adults and juveniles of these species found during a oneyear calibration study in Ammersee and Starnberger See, which will be presented and discussed elsewhere.

Check symbols in isotopeInterpretation2_coefficient. Has isotopeInterpretation3_basis but no other details. lake residence time move to sensorIntegration?-BK

the response of d180L to the temperature controlled variations in d18Op will be characteristic for each lake and, therefore, must be evaluated by hydrological investigations for any lake used for paleoclimatic reconstructions...d18OL of Lake Ammersee proved to be sensitive to mean air temperature variations with periods higher than 10 years and amplitudes larger than 0.3 Kelvin.

von Grafenstein, Ulrich , Erlenkeuser, Helmut , Muller, Jens , Trimborn, Peter , Alefs, Joachim

A 200 year midEuropean air temperature record preserved in lake sediments: An extension of the permil18Opair temperature relation into the past

Von Grafenstein, U., Erlenkeuser, H., Mueller, J., Trimborn, P. and Alefs, J.: A 200 year mid-European air temperature record preserved in lake sediments: An extension of the δ18Op-air temperature relation into the past, Geochimica et Cosmochimica Acta, 60(21), 4025–4036, doi:10.1016/s0016-7037(96)00230-x, 1996.

In a closed, low-latitude lake basin, the d18O values of the lake water, which are the main control on the d18O values of carbonates, are influenced largely by the balance between inflow (mainly shallow groundwater, in the case of Kajemarum) and evaporation (Talbot 1990). Thus, the d18O record in endogenic carbonate should largely reflect salinity.

Changes in d18O values that do not parallel those in Sr/Ca, however, are best explained by changes in water temperature, or in the 18O/16O ratio of precipitation. Changes in the isotopic composition of precipitation may be brought about by shifts in water-vapour source, air temperature (Andrews 1993) or cloud height. Variations in the intensity of monsoon convection may be important, since highly 18O-depleted rainfall is produced by the strong uplift that occurs in monsoon clouds with cold tops (Fontes et al. 1993).

Holmes, J. A. , Street-Perrott, F. A. , Allen, M. J. , Fothergill, P. A. , Harkness, D. D. , Kroon, D. , Perrott, R. A.

Holocene palaeolimnology of Kajemamm Oasis, Northern Nigeria: an isotopic study of ostracodes, bulk carbonate and organic carbon

HOLMES, J. A., STREET-PERROTT, F. A., ALLEN, M. J., FOTHERGILL, P. A., HARKNESS, D. D., KROON, D. and PERROTT, R. A.: Holocene palaeolimnology of Kajemamm Oasis, Northern Nigeria: an isotopic study of ostracodes, bulk carbonate and organic carbon, Journal of the Geological Society, 154(2), 311–319, doi:10.1144/gsjgs.154.2.0311, 1997.

VG Isocarb preparation system and triplecollectorVGPrismIImass spectrometer

Calculated 18O values for aragonite and calcite, precipitated in equilibrium with modern lake water (18Owater = + 2.6a€°) at a mean annual temperature of 25 C, yield values of 0.92a€° and 0.78a€°, respectively (Craig, 1965; Grossman & Ku, 1981). These theoretical values are close to mean values (0.85a€°, 0.47a€°, and 0.39a€°) for recent samples of Cochliogina sp., Pyrgophorus sp., and C. ilosvayi, respectively. This suggests that all three taxa precipitate carbonate near equilibrium with the water in which they live.

DK: 18O on gastropods. Another time series is published for another gastropod and an ostracode speices. All three are very similar, although ostracodes are less complete.

cleaned of organic material using 15% H2O2, then washed with deionized water, rinsed in methanol, and dried. Gastropods were cleaned in the same manner, except that specimens were additionally cleaned by sonication...Multiple (5) gastropod shells were ground to a fine powder with a mortar and pestle and a portion of the pulverized aragonite was loaded into stainless steel carrying boats for isotopic analysis.Multiple individuals, each living approximately one year, were used to average shortterm (i.e. yearly) changes in lake conditions.

Mean lake water was enriched in 18O by evaporation and was 3.6? greater than mean rainwater.

Calculated 18O values for aragonite and calcite, precipitated in equilibrium with modern lake water (18Owater = + 2.6‰) at a mean annual temperature of 25 C, yield values of 0.92‰ and 0.78‰, respectively (Craig, 1965; Grossman & Ku, 1981). These theoretical values are close to mean values (0.85‰, 0.47‰, and 0.39‰) for recent samples of Cochliopina sp., Pyrgophorus sp., and C. ilosvayi, respectively. This suggests that all three taxa precipitate carbonate near equilibrium with the water in which they live.

Interpretation of early Holocene (9000 until 7300 14C yrBP) oxygen isotopic results in terms of E/P is at odds with the strong evidence for moist conditions based on the presence of extensive lowland forest. The discrepancy between early Holocene pollen and 18Oresults in the PetenItza core can be reconciled if lakewater 18O is assumed to have been controlled by both regional climate and the changing surface area/volume ratio of the filling lake

One gastropod species data used here, also another gastropod species and ostracod records which show the same trends.

Curtis, Jason H. , Brenner, Mark , Hodell, David A. , Balser, Richard A. , Islebe, Gerald A. , Hooghiemstra, Henry

Curtis, J. H., Brenner, M., Hodell, D. A., Balser, R. A., Islebe, G. A. and Hooghiemstra, H.: Journal of Paleolimnology, 19(2), 139–159, doi:10.1023/a:1007968508262, 1998.

VG Isocarb preparation system. Isotopic ratios of purified CO2 gas were measured on-line by a triple-collector VG Prism Series II mass spectrometer

For stable isotope analysis, each 1 cm subsample was disaggregated by soaking in 3% H2O2 and subsequently sieved at 250 mm. The .250 mm fraction was collected on filter paper, dried at 60�C and transferred to glass scintillation vials. Ostracods and gastropods were separated from the matrix using a dissecting microscope at 10 � magnification. Adult specimens of the ostracod Cytheridella boldi were picked from the sieved 425?500 mm fraction, Heterocypris communis were picked from the 351?500 mm fraction, and Cypria obtusa were picked from the 250?300 mm fraction. Specimens of the gastropod Pyrgophorus sp. were separated from the sieved .1000 mm fraction. Ostracod valves were cleaned of organic material using 15% H2O2, then washed in deionized water, rinsed in methanol, and dried. Gastropods were cleaned in the same manner, except that specimens were cleaned further by sonication. Samples consisting of many monospecific ostracod carapaces (|15 C. boldi, |20 H. communis, |25 C. obtusa) were loaded into a stainless-steel carrying boat, crushed with a glass rod dipped in methanol and allowed to dry overnight. Numerous monospecific ostracod valves were used to constitute a sample to reduce variance that might result from running single, short-lived individuals whose isotopic signatures might reflect short-term (i.e., seasonal) water-column temperature and salinity conditions (Heaton et al., 1995)

Lake level also important as lake not always closed but Since ,3000 14C yr BP the level of Lake Valencia has been dropping. Lake closed in present day, but last 2k isotoeps realtively fresh suggesting more open system?

DK: Reject and defer to ostracode-based timeseries. Good for replication

One ostracod species used here but other shell typrsd show similar trends with values offset with a smaller range

Climate change in the Lake Valencia Basin, Venezuela, |12600 yr BP to present

Curtis, J. H., Brenner, M. and Hodell, D. A.: Climate change in the Lake Valencia Basin, Venezuela, ~12600 yr BP                 to present, The Holocene, 9(5), 609–619, doi:10.1191/095968399669724431, 1999.

interpreting the data as a record of changing seasonality and/or isotopic composition (and therefore source) of precipitation, are therefore preferred

higher d18O values should correlate with lower water levels, as inferred from the diatoms, indicating periods of reduced precipitation. In fact, the opposite appears to be the case - these two indicators tend to have a slight positive correlation rather than a negative one.

Lamb, Henry , Roberts, Neil , Leng, Melanie , Barker, Philip , Benkaddour, Abdelfattah , van der Kaars, Sander

Lamb, H., Roberts, N., Leng, M., Barker, P., Benkaddour, A. and van der Kaars, S.: Journal of Paleolimnology, 21(3), 325–343, doi:10.1023/a:1008099602205, 1999.

SON1997: T(sediments) = (Uk37-0.316)/(0.023); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual

Missing data in LiPD? Note to marine archive team- check basis entry (column BB) LJ 30/11/2018: missing data, were in v0.8 issue raised on Github

For calculating the residual d18O variability which is only due to salinity changes we further used alkenone-derived paleotemperatures to estimate the temperature effect (dTb), because alkenone records reflect salinity-independent temperature signals [Sonzogni et at., 1997b]: DTb = (Uk37 - SST)- T(-0.2). Here, dT is the difference between the measured alkenone- and the recent local annual average SST in the area of investigation (26.4�C). The factor b describes the relationship between d18O and temperature for the living G. tuber in the Indian Ocean (b = -0.2; Duplessy et at. [1981]).

Missing data in LiPD?  LJ 30/11/2018: missing data, were in v0.8 issue raised on Github

Urey, H. C. 1948. Oxygen isotopes in nature and in the laboratory. Science, 108:489?496.

Spero, H.J., Bijma, J., Lea, D.W., Bemis, B.E., 1997. Effect of seawater carbonate concentration on foraminiferal carbon and oxygen isotopes. Nature 390, 497-500.

SO90-56KA is varved see varved age model chron21 (Von Rad et al. 1999 QR Table 1); plus Krakatau (AD 1883) and Tambora ash (AD 1815) in boxcore SO90-39KG

d18Osw not estimated yet, but can be estimated using alkenones, NOT Mg/Ca. LJ: dont fully understand how they have derived the d18Osw estimates

Doose-Rolinski, Heidi , Rogalla, Ulf , Scheeder, Georg , Li¿½ckge, Andreas , von Rad, Ulrich

High-resolution temperature and evaporation changes during the Late Holocene in the northeastern Arabian Sea

Doose-Rolinski, H., Rogalla, U., Scheeder, G., Lueckge, A. and von Rad, U.: High-resolution temperature and evaporation changes during the Late Holocene in the northeastern Arabian Sea, Paleoceanography, 16(4), 358–367, doi:10.1029/2000pa000511, 2001.

McGregor, Helen V. , Evans, Michael N. , Goosse, Hugues , Leduc, Guillaume , Martrat, Belen , Addison, Jason A. , Mortyn, P. Graham , Oppo, Delia W. , Seidenkrantz, Marit-Solveig , Sicre, Marie-Alexandrine , Phipps, Steven J. , Selvaraj, Kandasamy , Thirumalai, Kaustubh , Filipsson, Helena L. , Ersek, Vasile

Robust global ocean cooling trend for the pre-industrial Common Era

McGregor, H. V., Evans, M. N., Goosse, H., Leduc, G., Martrat, B., Addison, J. A., Mortyn, P. G., Oppo, D. W., Seidenkrantz, M.-S., Sicre, M.-A., Phipps, S. J., Selvaraj, K., Thirumalai, K., Filipsson, H. L. and Ersek, V.: Robust global ocean cooling trend for the pre-industrial Common Era, Nature Geoscience, 8(9), 671–677, doi:10.1038/ngeo2510, 2015.

Decide if inferred material is surface or subsurface seawater. LJ: done 30/11/2018

d18O of seawater inferred from d18O carbonate and alkenone-derived temperature

Since d18Ow is linearly related to salinity, it is possible to reconstruct paleosalinity if an independent estimate of temperature is available [Duplessy et al., 1991; Rostek et al., 1993]. Here we use the d18O of the planktic foraminifer Neogloboquadrina pachyderma (dextral) and the alkenone temperature record for estimating paleosalinity variations.

PRA1988: T(cultures) = (Uk37-0.039)/(0.034), (Prahl et al., (1988); cultures E. huxleyi, 8-25i¿½C, n=22; R2=0.994); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Inadequate chronological constraints, final record that was entered contained an updated age model and dating constraints;

SST data from author not placed on age-depth scale, so I had to generate a control point-to-point linear interpolation using authors reported age control. All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

WARNING: no d18Osw in data set. Need to recalculate. Authors adjusted SST by -0.5 deg to correct for depth difference. SSS estimated with d18Osw, d18sw estimated using alkenones, NOT Mg/Ca, N pachy (d) used

High- and low-latitude climate control on the position of the southern Peru-Chile Current during the Holocene

Lamy, F., Ruehlemann, C., Hebbeln, D. and Wefer, G.: High- and low-latitude climate control on the position of the southern Peru-Chile Current during the Holocene, Paleoceanography, 17(2), 16–1–16–10, doi:10.1029/2001pa000727, 2002.

Decide if inferred material is surface or subsurface seawater. LJ 30/11/2018: missing data, were in v0.8 issue raised on Github

In Arctic water there is no difference between d18O values obtained from N. pachyderma (sin.) and N. pachyderma (dex.), while the differences increase going eastward in the Nordic Seas and into warmer Atlantic water masses [Johannessen, 1992]. Thus the varying contrast between the d18O of N. pachyderma (dex.) and N. pachyderma (sin.) can be used as an indicator of horizontal migration of the Arctic water/Atlantic water interface (Arctic Front).

Risebrobakken, B., Jansen, E., Andersson, C., Mjelde, E. and Hevroey, K.: A high-resolution study of Holocene paleoclimatic and paleoceanographic changes in the Nordic Seas, Paleoceanography, 18(1), n/a–n/a, doi:10.1029/2002pa000764, 2003.

Tedesco, K. and Thunell, R.: High resolution tropical climate record for the last 6,000 years, Geophysical Research Letters, 30(17), n/a–n/a, doi:10.1029/2003gl017959, 2003.

Decide if inferred material is surface or subsurface seawater. LJ: done 30/11/2018, added depth, uploaded edited LiPD file to dropbox

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to O2kLR_074

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement; see "Data (QC) tab" cell C6 for details; climateInterpretation_seasonality changed - was originally Annual

PRA1988: E. huxleyi culture-based calibration. No RMSE is reported in the original publication, so a RMSE was calculated by taking a regression off of the five culture T-UK37 datapoints reported in the publication.; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual

PRA1988: E. huxleyi culture-based calibration. No RMSE is reported in the original publication, so a RMSE was calculated by taking a regression off of the five culture T-UK37 datapoints reported in the publication.

d18Osw can be estimated, but authors chose not to do this because of depth and season habitat differences between d18O and ALK SST. multiple species of planktic foraminifera and SST estimates (Mg/Ca and alkenones, Alk was taken in Ocean2k)

Keigwin, L. D., Sachs, J. P. and Rosenthal, Y.: A 1600-year history of the Labrador Current off Nova Scotia, Climate Dynamics, 21(1), 53–62, doi:10.1007/s00382-003-0316-6, 2003.

Staubwasser, M., Sirocko, F., Grootes, P. M. and Segl, M.: Climate change at the 4.2 ka BP termination of the Indus valley civilization and Holocene south Asian monsoon variability, Geophysical Research Letters, 30(8), doi:10.1029/2002gl016822, 2003.

The ?18O of planktonic foraminiferal calcite is a function of two independent variables, the temperature at the time of calcification and the oxygen isotopic composition of seawater, with the latter variable being a measure of local salinity

Box core recovered with intact/undisturbed sediment-water interface.

Faunal correlation to another core (PL07-64 BC) with a varve stratigraphy

spliced record, Mg/Ca data available for box core, but authors did not calculate d18Osw

Black, D. E., Thunell, R. C., Kaplan, A., Peterson, L. C. and Tappa, E. J.: A 2000-year record of Caribbean and tropical North Atlantic hydrographic variability, Paleoceanography, 19(2), n/a–n/a, doi:10.1029/2003pa000982, 2004.

Black, D. E.: Eight Centuries of North Atlantic Ocean Atmosphere Variability, Science, 286(5445), 1709–1713, doi:10.1126/science.286.5445.1709, 1999.

N. pachyderma: 106-1000? not mentioned in paper, but from NOAA data sheet

A compilation of the _18O of modern Foraminifera, water temperature and salinity indicates that the isotopic composition of North Iceland Shelf Foraminifera is controlled primarily by temperature (Smith, 2001; Smith et al., in review). For example, Smith et al. (in review) found that a strong correlation (r21/40.74) exists between temperatures in the upper 50m of the water column and _18O of the planktonic species N. pachyderma (s). It is not surprising that foraminiferal _18O in this region is controlled primarily by temperature because modern hydrographic changes in North Iceland Shelf waters are dominated by temperature changes, with salinity playing a minor role (Smith, 2001; Smith et al., in review). The effects of temperature versus salinity on the _18O of North Iceland Shelf Foraminifera is discussed at length in a companion paper by Smith et al. (in review), which examines the same _18O records presented in this study.

Castaneda, I. S., Smith, L. M., Kristjansdottir, G. B. and Andrews, J. T.: Temporal changes in Holoceneδ18O records from the northwest and central North Iceland Shelf, Journal of Quaternary Science, 19(4), 321–334, doi:10.1002/jqs.841, 2004.

Decide if inferred material is surface or subsurface seawater. LJ 30/11/2018: missing data, were included in v0.8. issue raised on Github

Thermo Electron Delta plus XL mass spectrometer using high temperature conversion.

Inferred material needed. ; "isotope interpretation1,2,3" is missing -BK

Sauer, P. E., Eglinton, T. I., Hayes, J. M., Schimmelmann, A. & Sessions, A. L. Compound-specific D/H ratios of lipid biomarkers from sediments as a proxy for environmental and climatic conditions. Geochim. Cosmochim. Acta 65, 213–222 (2001)

Urey, H. C. 1948. Oxygen isotopes in nature and in the laboratory. Science, 108:489-496.

only 2 age control points, not in O2kLR. Excludepermil SST available from UK37:d18Osw not added

Climatic controls on central African hydrology during the past 20,000 years

SchefuSS, E., Schouten, S. and Schneider, R. R.: Climatic controls on central African hydrology during the past 20,000 years, Nature, 437(7061), 1003–1006, doi:10.1038/nature03945, 2005.

Disentangling marine, soil and plant organic carbon contributions to continental margin sediments: A multi-proxy approach in a 20,000 year sediment record from the Congo deep-sea fan

Weijers, J. W. H., Schouten, S., SchefuSS, E., Schneider, R. R. and Sinninghe Damste, J. S.: Disentangling marine, soil and plant organic carbon contributions to continental margin sediments: A multi-proxy approach in a 20,000 year sediment record from the Congo deep-sea fan, Geochimica et Cosmochimica Acta, 73(1), 119–132, doi:10.1016/j.gca.2008.10.016, 2009.

not provided. The details of the sampling and analytical procedures are given by Sachs and Lehman [1999]. But that publication neither mentions the instrument etc

WARNING. Documentation is extremely poor for this record. d18Osw has to be estimated, multiple species of planktic foraminifera and SST estimates (MAT and alkenones, alk was taken in Ocean2k)

The 8200 year B.P. event in the slope water system, western subpolar North Atlantic

Keigwin, L. D., Sachs, J. P., Rosenthal, Y. and Boyle, E. A.: The 8200 year B.P. event in the slope water system, western subpolar North Atlantic, Paleoceanography, 20(2), n/a–n/a, doi:10.1029/2004pa001074, 2005.

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to O2kLR_066

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement.; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

ANA2003: Anand multi species sediment trap calibration.; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

WARNING: d18Of measurements probably affected by cushing. 0.2 permil should be added. in the archived data, extra results with different levels of smoothing of sw d18O

Florida Current surface temperature and salinity variability during the last millennium

Lund, D. C. and Curry, W.: Florida Current surface temperature and salinity variability during the last millennium, Paleoceanography, 21(2), n/a–n/a, doi:10.1029/2005pa001218, 2006.

native Mg/Ca ratio from which SST was calculated; values are from Lunds "Avg Mg/Ca" column and are in units of mmol/mol; note that in original source, there are also MgCa estimates for std. dev & std. error

; paleoData_variableName changed - was originally native_MgCa; paleoData_variableName changed - was originally Mg_Ca; paleoData_variableName changed - was originally Mg_Ca; archiveType changed - was originally Marine sediment (MS)

HVM, BM, 20/4/2016 Atlantic0326aLund2006_MgCa_MC125_GreatBahamaBank

; paleoData_variableName changed - was originally temp_C; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to LPD7c7e19c5

0.18 1sd, based on 4 replicate measurements of 10 shells per sample

in the archived data, extra results with different levels of smoothing of sw d18O

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement.

; paleoData_variableName changed - was originally MgCa; paleoData_variableName changed - was originally Mg_Ca; paleoData_variableName changed - was originally Mg_Ca; archiveType changed - was originally Marine sediment (MS)

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater.

HVM, BM, 20/4/2016 Atlantic0326bLund2006_MgCa_MC118_GreatBahamaBank

; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to LPDefb3d2b0

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Dataset contains NaN values and datapoints whose chronology is not QCd

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater.; "isotope interpretation1,2,3" is missing -BK

Richey J.N; Poore, R.Z; Flower, B.P; Quinn, T.M; Hollander, D.J.

Richey, J. N., Poore, R. Z., Flower, B. P. and Quinn, T. M.: 1400 yr multiproxy record of climate variability from the northern Gulf of Mexico, Geology, 35(5), 423, doi:10.1130/g23507a.1, 2007.

Hydrogen isotope ratios were determined by isotope ratiopermilmonitoring gas chromatography mass spectrometry (irmGCMS) on a ThermoFinnigan Deltaplus  XP equipped with a Trace GC and Combustion III interface, using methods adapted from Sessions et al.  [1999] and Sauer et al.  [2001]. The Trace GC was equipped with a PTV inlet operated in splitless mode, a 30 m DB5 capillary column with 0.25 mm ID and 0.25 m m film thickness.

time series split, but not updated in v0.10. Final QC in next version

in areas of strong contrast between the d D value of precipitation and seawater, and high amounts of rainfall (e.g., in the tropics close to river deltas), any changes in alkenone d D values caused by species or growth rate variations are likely to be secondary to the first order effects caused by freshwater fluxes.

dD values measured in alkenones from marine sediments can be used to reconstruct past changes in freshwater supply to the ocean and hence precipitation and river runoff.

Eastern tropical Pacific hydrologic changes during the past 27,000 years from D/H ratios in alkenones

Pahnke, K., Sachs, J. P., Keigwin, L., Timmermann, A. and Xie, S.-P.: Eastern tropical Pacific hydrologic changes during the past 27,000 years from D/H ratios in alkenones, Paleoceanography, 22(4), n/a–n/a, doi:10.1029/2007pa001468, 2007.

HVM, BM, 20/4/2016 Pacific0118Stott2007_MD98-2176 WDC-paleoclimatology Data Contribution Series # 2007-092 Readme for Stott et al., (2007) notes calibration with Anand et al., (2003).

ANA2003: Mg/Ca=0.38*exp(0.09*SST), multiple species; Mg/Ca =0.449*exp(0.09*SST), G ruber, (Anand et al., (2003); sediment trap; error i¿½1.2i¿½C); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

Temperature (oC) = 16.5 – 4.80(d18Oc – d18Ow); following 10.1038/nature02903

LJ (03AUG2017) not relevant for 2k, but raw data had 2 different ages for 671 cm

CALIB 5.0. Original radiocarbon dates are from Stott et al. 2004 Nature (DOI:10.1038/nature02903).

Southern Hemisphere and Deep-Sea Warming Led Deglacial Atmospheric CO2 Rise and Tropical Warming

Stott, L., Timmermann, A. and Thunell, R.: Southern Hemisphere and Deep-Sea Warming Led Deglacial Atmospheric CO2 Rise and Tropical Warming, Science, 318(5849), 435–438, doi:10.1126/science.1143791, 2007.

HVM, BM, 20/4/2016 Pacific0185Stott2007_MD98-2181 WDC-paleoclimatology Data Contribution Series # 2007-092 Readme for Stott et al., (2007) notes calibration with Anand et al., (2003).

planktonic foraminifera carbonate: G. ruber ss (white): size not provided

The site is also located within the Pacific Warm Pool (7), where the ?18O and Mg/Ca of planktonic foraminifera record the temperature and salinity of western tropical Pacific surface water (8, 9).

Calibrated dates not provided in literature sources but SST data provided on calibrated age model (CALIB 5.02). Original radiocarbon dates are disseminated in Stott et al. 2002 Science (DOI:10.1126/science.1071627) and Stott et al. 2004 Nature (DOI:10.1038/nature02903).

using d18O ruber, data partly presented previously in Super ENSO and Global Climate Oscillations at Millennial Time Scales Lowell Stott1,*, Christopher Poulsen1, Steve Lund1, Robert Thunell2 Science  12 Jul 2002: Vol. 297, Issue 5579, pp. 222-226 DOI: 10.1126/science.1071627

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater. LJ done, 30/11/2018

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater. Data need to be removed

To estimate the paleosalinity (S; psu) from the d18Oswcorr, the regional d18Oswcorr?salinity relationship for the eastern equatorial Pacific by Fairbanks et al. (1992) [S i¿½ (d18Osw+8.77)/0.26] was applied, which has a similar slope as modelled by Delaygue et al. (2000) for the Southeast Pacific.

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement;i¿½see "Data (QC) tab" cell C6 for details; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

WARNING: no d18Osw in data set. Need to recalculate. Authors adjusted SST by -1.0 deg to correct for depth difference. SSS estimated with d18Osw, d18sw estimated using alkenones, NOT Mg/Ca, N pachy (d) used

Mohtadi, Mahyar , Romero, Oscar E. , Kaiser, Ji¿½ri¿½me , Hebbeln, Dierk

Cooling of the southern high latitudes during the Medieval Period and its effect on ENSO

Mohtadi, M., Romero, O. E., Kaiser, J. and Hebbeln, D.: Cooling of the southern high latitudes during the Medieval Period and its effect on ENSO, Quaternary Science Reviews, 26(7-8), 1055–1066, doi:10.1016/j.quascirev.2006.12.008, 2007.

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater. D18Oseawater missing

Foraminifera, often living deeper in the water column, may record thermocline temperatures, which are set by ventilation during the winter months.

planktonic foram calcite: N. incompta 150-212 (oxidative + reductive cleaning)

WARNING: duplicate of MS07RCSNA02. Kept MS07RCSNA02 because properly filled out

Came, R. E., Oppo, D. W. and McManus, J. F.: Amplitude and timing of temperature and salinity variability in the subpolar North Atlantic over the past 10 k.y., Geology, 35(4), 315, doi:10.1130/g23455a.1, 2007.

DEK2002: G. ruber core top calibration with a depth correction to account for dissolution effects

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater. D18Ocarbonate missing

The d18Osw is extracted by means of the Mg/Ca-based SST estimate with analyzed d18O and temperature d18Ocalcite- d18Osw relationship. d18Osw is related linearly to salinity.

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Contains NaN values

The stable hydrogen isotopic composition of C37:2 was measured on a Thermo DELTA V GC?IRMS. Instrument performance and the H3+ factor were monitored on a daily basis using a reference H2 gas and a mixture of n-alkanes of known isotopic composition (Zhang and Sachs, 2007).

These are the dD values originally archived as MS13GLGG, but merged with this time series as it is the same core

As in Pahnke et al., 2007, Paleoceanography: ""in areas of strong contrast between the d D value of precipitation and seawater, and high amounts of rainfall (e.g., in the tropics close to river deltas), any changes in alkenone d D values caused by species or growth rate variations are likely to be secondary to the first order effects caused by freshwater fluxes."

Our results illustrate that changes in atmospheric circulation can trigger changes in precipitation isotopes in a counter-intuitive manner that ultimately impacts surface salinity estimates based on seawater isotopic values.

not clear which paleotemperature eq use. Bemis 1998 presents several

155,000 Years of West African Monsoon and Ocean Thermal Evolution

Weldeab, S., Lea, D. W., Schneider, R. R. and Andersen, N.: 155,000 Years of West African Monsoon and Ocean Thermal Evolution, Science, 316(5829), 1303–1307, doi:10.1126/science.1140461, 2007.

Holocene changes in eastern equatorial Atlantic salinity as estimated by water isotopologues

Planktonic foraminifera ?18O values show no significant variability, indicating no major variations in SST and SSS during the past 3.2 kyrs

data presented in peer reviewed publication, sparse methods in thesis: due to influence of tsunami deposits the interval 51–140 cm might well be disturbed and the interval 140–248 cm should be interpreted carefully, especially above 198 cm

Alt-Epping, U., Stuut, J.-B. W., Hebbeln, D. and Schneider, R.: Variations in sediment provenance during the past 3000 years off the Tagus River, Portugal, Marine Geology, 261(1-4), 82–91, doi:10.1016/j.margeo.2008.11.008, 2009.

A companion reconstruction of d18O of sea water?a sea surface salinity and hydrology indicator?indicates a tight coupling with the East Asian monsoon system and remote control of IPWP hydrology on centennial?millennial timescales, rather than a dominant influence from local SST variation.

HVM, BM, 20/4/2016Pacific0335aOppo2009_MC31,BJ8-03-32GGC,BJ8-03-34GGC Combination of Oppo et al., (2009) data from the three cores recovered from the same drill site. Data sorted based on age.

ANA2003: Mg/Ca=0.38*exp(0.09*SST), multiple species; Mg/Ca =0.449*exp(0.09*SST), G ruber, (Anand et al., (2003); sediment trap; error i¿½1.2i¿½C); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual; LJ20161212: for SST estimates in 34GGC 0.25 was added to the Mg/Ca values (I don't know why)

2,000-year-long temperature and hydrology reconstructions from the Indo-Pacific warm pool

Oppo, D. W., Rosenthal, Y. and Linsley, B. K.: 2,000-year-long temperature and hydrology reconstructions from the Indo-Pacific warm pool, Nature, 460(7259), 1113–1116, doi:10.1038/nature08233, 2009.

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater.;  "isotope interpretation1,2,3" is missing -BK

LJ 12/12/2018: LiPD file contained many errors, would like to see before QC approval

d18Ow = (4.64-SQRT(4.64^2-0.36*(16.1-T)))/0.18+d18Oc-0.52+0.27, vital effect correction 0.52

TH2009: for G. inflata, based on core tops. Thornalley et al. assume an exponential constant of 0.10 using Barker et al., 2005, Quat Sci Rev as a justification, then fit the preexponential constant using regional core top data.

native Mg/Ca ratio from which SST was calculated; values are from foram G. bulloides, are are in units of mmol/mol

; paleoData_variableName changed  was originally native_MgCa; paleoData_variableName changed  was originally Mg_Ca; paleoData_variableName changed  was originally Mg_Ca; archiveType changed  was originally Marine sediment (MS)

; paleoData_variableName changed  was originally temp_C; paleoData_units changed  was originally deg C; climateInterpretation_seasonality changed  was originally MJJ; climateInterpretation_seasonality changed  was originally 5/6/2007; climateInterpretation_seasonality changed  was originally 5 6 2007; archiveType changed  was originally Marine sediment (MS)

BAR2005: Mg/Ca=0.794*exp(0.10*SST), (Barker et al., (2005), in combination with Thornalley et al., (2009); error degrees1.3degreesC)

HVM, BM, 20/4/2016 Atlantic0220Thornalley2009__RApiD121K_Mg/Ca_bulloides Used the G. bulloides record from this core as it was reported as nearsurface.

; paleoData_variableName changed  was originally temp_C; paleoData_units changed  was originally deg C; climateInterpretation_seasonality changed  was originally MJJ; climateInterpretation_seasonality changed  was originally 5 6 2007; archiveType changed  was originally Marine sediment (MS)

TH2009: for G. bulloides, based on core tops. Thornalley et al. assume an exponential constant of 0.10 using Barker et al., 2005, Quat Sci Rev as a justification, then fit the preexponential constant using regional core top data.

All O2KLR records have been qualitycontrolled according to protocols published in Nature Geoscience supplement.

South Iceland Rise, subpolar North Atlantic, marine sediment Mg/Ca SST

Holocene oscillations in temperature and salinity of the surface subpolar North Atlantic

Thornalley, D. J. R., Elderfield, H. and McCave, I. N.: Holocene oscillations in temperature and salinity of the surface subpolar North Atlantic, Nature, 457(7230), 711–714, doi:10.1038/nature07717, 2009.

McGregor, Helen V. , Evans, Michael N. , Goosse, Hugues , Leduc, Guillaume , Martrat, Belen , Addison, Jason A. , Mortyn, P. Graham , Oppo, Delia W. , Seidenkrantz, MaritSolveig , Sicre, MarieAlexandrine , Phipps, Steven J. , Selvaraj, Kandasamy , Thirumalai, Kaustubh , Filipsson, Helena L. , Ersek, Vasile

LJ 12/12/2018 age model based on dated tephra layers, data available in 10.1038/sdata.2016.425

we recall that the ?18O of foraminiferal calcite reflects changes not only in sea surface temperatures (SSTs) but also in sea-water isotopic composition.

Taricco, C., Ghil, M., Alessio, S. and Vivaldo, G.: Two millennia of climate variability in the Central Mediterranean, Climate of the Past, 5(2), 171–181, doi:10.5194/cp-5-171-2009, 2009.

; paleoData_variableName changed - was originally depthUpper_cm; paleoData_variableName changed - was originally depth_top; paleoData_variableName changed - was originally depth_top; archiveType changed - was originally Marine sediment (MS); archiveType changed - was originally Marine sediment (MS)

original composite dataset from Richter et al. (2009) - PLEASE USE QC DATA FOR ANALYSIS!!!!

; archiveType changed - was originally Marine sediment (MS); archiveType changed - was originally Marine sediment (MS)

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to LPD47182517

Converted into calcification temperatures with the species-specific equation of Anand et al. (2003) based on data from Elderfield and Ganssen (2000)  (ANA2003)

; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally AMJJ; archiveType changed - was originally Marine sediment (MS); archiveType changed - was originally Marine sediment (MS)

native Mg/Ca ratio from which SST was calculated; values are from foram G. bulloides, and are in units of mmol/mol

; paleoData_variableName changed - was originally MgCa; paleoData_variableName changed - was originally Mg_Ca; paleoData_variableName changed - was originally Mg_Ca; archiveType changed - was originally Marine sediment (MS); archiveType changed - was originally Marine sediment (MS)

; paleoData_variableName changed - was originally depthLower_cm; paleoData_variableName changed - was originally depth_bottom; paleoData_variableName changed - was originally depth_bottom; archiveType changed - was originally Marine sediment (MS); archiveType changed - was originally Marine sediment (MS)

HVM, BM, 20/4/2016 Atlantic0058Richter2009__ENAM9606,M200309_Mg/Ca

ANA2003: G. bulloides, based on coretop data from Elderfield and Ganssen, 2000, Nature

Seawater ?18O (?18Ow in ? vs. V-SMOW) was estimated from Mg/Ca-derived calcification temperatures and ?18O of foraminiferal calcite (?18Oc in ? vs. PDB) by rearranging the isotopic paleotemperature equation of Shackleton (1974) (T = 16.9 ? 4 i¿½ (?18Oc ? ?18Ow)) and solving for ?18Ow. A V-SMOW vs. V-PDB correction of ?0.20? was applied, consistent with the correction factor common at time of publication of the Shackleton equation (see Bemis et al., 1998). Based on an analytical error of i¿½0.06? for ?18Oc and a combined analytical and calibration error of i¿½1 i¿½C for T (Mg/Ca), the uncertainty for reconstructed ?18Ow is estimated as i¿½0.26?.

ENAM9606,M200309_North Atlantic_marine sediment Mg/Ca SST based om Globigerina bulloides

Late Holocene (0?2.4kaBP) surface water temperature and salinity variability, Feni Drift, NE Atlantic Ocean

Richter, T. O., Peeters, F. J. C. and van Weering, T. C. E.: Late Holocene (0–2.4kaBP) surface water temperature and salinity variability, Feni Drift, NE Atlantic Ocean, Quaternary Science Reviews, 28(19-20), 1941–1955, doi:10.1016/j.quascirev.2009.04.008, 2009.

European Union FP5 (PACLIVA, Patterns of Climate variability in the North Atlantic - T.O.R., T.C.E.v.W.). Dutch Science Foundation (NWO) within RAPID initiative (VAMOC, Variability of Atlantic Meridional Overturning Circulation - F.J.C.P., T.C.E.v.W.)

not explicitly mentioned, refs to papers that use Bemis et al 1998

LJ (03AUG2017): the age models for Mg/Ca and d18O are not consistent. This is the linearly interpolated d18O age model

ANA2003: Anand multi species sediment trap calibration.; paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally Annual

planktonic foraminifera carbonate: G. ruber ss (white): 212-300; oxidative-reductive cleaning

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Identical to LPD30c5b95c; Datapoints close to 0 CE are not constrained and hence not included

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement.; climateInterpretation_seasonality changed - was originally Annual

Holocene evolution of the Indonesian throughflow and the western Pacific warm pool

Linsley, B. K., Rosenthal, Y. and Oppo, D. W.: Holocene evolution of the Indonesian throughflow and the western Pacific warm pool, Nature Geoscience, 3(8), 578–583, doi:10.1038/ngeo920, 2010.

The hydrogen isotopic composition of the C28 , C30  and C32 n? acids (as FAMEs) was determined by gas chromatography? isotope ratio monitoring? mass spectrometry (GC? IR? MS) with a Thermo Finnigan Delta XL mass spectrometer at Brown University. H2  gas of a known isotopic composition was used as a working reference standard, and all analyses were performed in triplicate. Mass balance corrections were made for the added methyl group.

Marine archive team- check inferred materials and differentiate between surface and subsurface seawater.; change "inferred material" to seawater? and, address "isotope interpretation1" (should "rainfall amount" be "salinity" or "d18Osw" ? "rainfall amount" can go into "climate variable" fields -BK. LJ (13/12/2018), these are terrestrial biomarkers preserved in marine sediment

more depleted d Dwax  values in our paleorecord indicate an invigorated regional hydrological cycle, essentially a stronger Indonesian monsoon (IM), and conversely enriched d Dwax  values suggest reduced hydrologic intensity and a weak IM.

dD of C30 fatty acid. Different entries correspond to 2 diff cores from same site, 31MC (upper core) and 34GGC (deeper core). * NOTE: Earliest/Most recent year is in CE

Coordinated hydrological regimes in the Indo‐Pacific region during the past two millennia

Tierney, J. E., Oppo, D. W., Rosenthal, Y., Russell, J. M. and Linsley, B. K.: Coordinated hydrological regimes in the Indo-Pacific region during the past two millennia, Paleoceanography, 25(1), doi:10.1029/2009pa001871, 2010.

HVM, BM, 20/4/2016 Pacific1577Newton2011_MD982177 Data archived as Mg/Ca values only. Data converted to SST using the calibration of Dekens et al., (2002), as per the original publication.

; paleoData_variableName changed  was originally temp_C; paleoData_units changed  was originally deg C; climateInterpretation_seasonality changed  was originally Annual; archiveType changed  was originally Marine sediment (MS); archiveType changed  was originally Marine sediment (MS)

DEK2002: Mg/Ca=0.38*exp(0.09*[SST0.61 (core depth km)]), (Dekens et al., (2002); core tops; G ruber)

est. SST = (ln Mg/Ca/0.38)/0.09+0.61 (core depth (km)); LJ (01AUG2017) note that depth correction NOT applied

; archiveType changed  was originally Marine sediment (MS); archiveType changed  was originally Marine sediment (MS)

the ?sw can be directly converted to salinity using a relationship developed for the western tropical Pacific (Morimoto et al., 2002)

LJ (01AUG2017) linearly interpolated missing ages using O2K data

d18Osw not estimated yet, and age model should be retrieved from the Ocean2k SST database

In original online data source, Newton et al only provide Mg/Ca ratios, so these had to be converted to Mg/Ca SST using equations in paper. Also, no agedepth model was provided, though 14C date information was, so a direct pointtopoint linear interpolation age model was generated. All O2KLR records have been qualitycontrolled according to protocols published in Nature Geoscience supplement.

Newton, A., Thunell, R. and Stott, L.: Changes in the Indonesian Throughflow during the past 2000 yr, Geology, 39(1), 63–66, doi:10.1130/g31421.1, 2010.

HVM, BM, 20/4/2016 Pacific0291Newton2011_MD98-2160 Data archived as Mg/Ca values only. Data converted to SST using the calibration of Dekens et al., 2002, as per the original publication

; paleoData_variableName changed - was originally temp_C; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally marine sediments; paleoData_units changed - was originally deg C

DEK2002: Mg/Ca=0.38*exp(0.09*[SST-0.61 (core depth km)]), (Dekens et al., (2002); core tops; G ruber). LJ (01AUG2017) the depth correction was NOT applied by the authors

DEK2002: Mg/Ca=0.38*exp(0.09*[SST-0.61 (core depth km)]), (Dekens et al., (2002); core tops; G ruber)

LJ (01AUG2017) missing ages linearly interpolated assuming constant sed rate

oxidative cleaning only; archiveType changed - was originally Marine sediment (MS)

Mixed planktic forams (marine reservoir correction 75 +/- 80 yrs)

d18Osw not estimated yet, and age model should be retrieved from the Ocean2k SST database. Not clear which paleotemperature equation used: Bemis et al 1998 contains several.

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement. Dataset recorded in this file is truncated to last 2000 years.

Mg/Ca?based SST estimates are often subtracted from d18Oc to yield estimates of seawater d18O (d18Osw) [e.g., Lund and Curry, 2006; Richey et al., 2007].

Only 1s calib age error quoted. Calibration curve and method: Fairbanks et al. 2005 http://radiocarbon.ldeo.columbia.edu/research/radcarbcal.htm

Regional climate variability in the western subtropical North Atlantic during the past two millennia

Saenger, C., Came, R. E., Oppo, D. W., Keigwin, L. D. and Cohen, A. L.: Regional climate variability in the western subtropical North Atlantic during the past two millennia, Paleoceanography, 26(2), n/a–n/a, doi:10.1029/2010pa002038, 2011.

G. inflata as associated to the wintertime eastern branch of the Azores Current

N. pachyderma var. dextral as a winter deep-dwelling species linked with the Portugal Current

surface sediment spatial distribution of species unveils G. bulloides as the coastal upwelling species

Pb210 top 40.4 cm of sediment noted spliced depth corrected for compaction. OrigiNaNl depth 34-35 cm; Pb210 age of reaching background equilibrium (PO287-26B) 74 (mBq/g) calcuted using 0.47 cm/yr

Climate of the last millennium at the southern pole of the North Atlantic Oscillation: an inner-shelf sediment record of flooding and upwelling

Abrantes, F., Rodrigues, T., Montanari, B., Santos, C., Witt, L., Lopes, C. and Voelker, A.: Climate of the last millennium at the southern pole of the North Atlantic Oscillation: an inner-shelf sediment record of flooding and upwelling, Climate Research, 48(2), 261–280, doi:10.3354/cr01010, 2011.

Individual Foraminifera Analysis, d18O values are averages for each depth analysed; age model unclear. There seems to be a reversal around 12 cm in the core, but this is not taken into account

Khider, D., Stott, L. D., Emile-Geay, J., Thunell, R. and Hammond, D. E.: Assessing El Nino Southern Oscillation variability during the past millennium, Paleoceanography, 26(3), n/a–n/a, doi:10.1029/2011pa002139, 2011.

Werner, K., Spielhagen, R. F., Bauch, D., Hass, H. C., Kandiano, E. and Zamelczyk, K.: Atlantic Water advection to the eastern Fram Strait — Multiproxy evidence for late Holocene variability, Palaeogeography, Palaeoclimatology, Palaeoecology, 308(3-4), 264–276, doi:10.1016/j.palaeo.2011.05.030, 2011.

Sejrup, H. P., Haflidason, H. and Andrews, J. T.: A Holocene North Atlantic SST record and regional climate variability, Quaternary Science Reviews, 30(21-22), 3181–3195, doi:10.1016/j.quascirev.2011.07.025, 2011.

HVM, BM, 20/4/2016 Mediterranean1157abMoreno2012_MINMC-2_MINMC-1_alk(Muller) The higher-resolution alkenone record was selected. The authors also note that the G. bulloides Mg/Ca records spring upwelling SSTs whereas alkenones represent annual average SSTs. Alkenone data were measured in two cores (MINMC06-1 and MINMC06-2) from the same site. These two records were combined with the data sorted based on age.

MUE1998: T(sediments) = (Uk?37-0.044)/0.033, (M?ller et al., (1998); global (60S-60N), 0-29?C, annual at 0 m, n=370, R2=0.958)

; paleoData_variableName changed - was originally native_UK_37; archiveType changed - was originally Marine sediment (MS)

quality-controlled data from Moreno et al. (2012) that was used in the O2K-LR analysis; alkenone data were measured in two cores (MINMC06-1 and MINMC06-2) from the same site; these two records were combined with the data sorted based on age.

The Mg/Ca temperature record has been used to extract the temperature effect of the d18O from G. bulloides to obtain the sea water d18O (d18Osw), which is associated with salinity and thus becomes a proxy for sea surface salinity (SSS).

planktonic foraminifera carbonate. G bulloides size not provided; reductively cleaned

Authors did not provide paleotemperature equation. D18Osw values calculated using K&O97.

Pb210 top 3.25cm (MINMC06-1) and 3.75cm (MINMC06-2) of sediment; MINMC06-1 Cs-137 present top 2.5cm

d18Osw not estimated yet, alk (used for SST in ocean2k) and Mg/Ca on bulloides are available, Mg/Ca should be used. These are actually two parallel records! Poor documentation, no information how d18O was measured or how d18Osw was estimated. The initial entry contained some info on instrument (MAT 252) and precision (0.08) and paleotemp eq (Shackleton), but LJ cant find it in the paper (Shackleton is not even cited). Who filled this out?

UK37 derived sea surface temperatures of sediment cores MINMC06-1 and MINMC06-2, Minorca contourite.

The Medieval Climate Anomaly in the Iberian Peninsula reconstructed from marine and lake records

Moreno, A., Perez, A., Frigola, J., Nieto-Moreno, V., Rodrigo-Gamiz, M., Martrat, B., Gonzalez-Samperiz, P., Morellon, M., Martin-Puertas, C., Corella, J. P., Belmonte, A., Sancho, C., Cacho, I., Herrera, G., Canals, M., Grimalt, J. O., Jimenez-Espejo, F., Martinez-Ruiz, F., Vegas-Vilarrubia, T. and Valero-Garces, B. L.: The Medieval Climate Anomaly in the Iberian Peninsula reconstructed from marine and lake records, Quaternary Science Reviews, 43, 16–32, doi:10.1016/j.quascirev.2012.04.007, 2012.

The ?18O composition of foraminifera records both the oxygen isotopic composition of seawater (?18Oseawater) and the calcification temperature (through the kinetic fractionation effect) [Emiliani, 1955]. Shell ?18O and Mg/Ca calcification temperature values for G. ruber are substituted into the oxygen isotope paleotemperature equation [Shackleton, 1974] to solve the ?18Oseawater.

CLE2008: Cleroux et al., 2008 North Atlantic core top calibration for G. ruber (white); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally JJA; climateInterpretation_seasonality changed - was originally 6 7 2008

CLE2008: Cleroux et al., 2008 North Atlantic core top calibration for G. ruber (white)

d18Osw not estimated yet, also data for P. obliquiloculata, but not on pangaea

High-resolution sea surface reconstructions off Cape Hatteras over the last 10 ka

Cleroux, C., Debret, M., Cortijo, E., Duplessy, J.-C., Dewilde, F., Reijmer, J. and Massei, N.: High-resolution sea surface reconstructions off Cape Hatteras over the last 10 ka, Paleoceanography, 27(1), n/a–n/a, doi:10.1029/2011pa002184, 2012.

Mueller, J., Werner, K., Stein, R., Fahl, K., Moros, M. and Jansen, E.: Holocene cooling culminates in sea ice oscillations in Fram Strait, Quaternary Science Reviews, 47, 1–14, doi:10.1016/j.quascirev.2012.04.024, 2012.

LJ 12/12/2018. Added raw d18O carbonate. isotope data have depth

low-light paleotemperature equation derived for Orbulina universa ( Bemis et al., 1998 and Lea et al., 2000)

The specimens were cleaned following the UCSB standard foraminifera cleaning procedure without the DTPA step ( Lea et al., 2000 and Martin and Lea, 2002).; archiveType changed - was originally Marine sediment (MS)

DEK2002: Mg/Ca=0.38*exp(0.09*[SST-0.61 (core depth km)]), (Dekens et al., (2002); core tops; G ruber); paleoData_units changed - was originally deg C; climateInterpretation_seasonality changed - was originally annual; archiveType changed - was originally Marine sediment (MS)

These are the original, not quality controlled data. O2kLR recommends only using the Quality controlled data.Dataset chronology not QCd; Final entry truncated.

All O2K-LR records have been quality-controlled according to protocols published in Nature Geoscience supplement. Core length not reported, deepest 14C date at 286.5 cm; climateInterpretation_seasonality changed - was originally Annual; archiveType changed - was originally Marine sediment (MS)

NB thickness is not reported it is assumed it is 1 cm sections Calib6.0

Saraswat, Rajeev , Lea, David W. , Nigam, Rajiv , Mackensen, Andreas , Naik, Dinesh K.

Deglaciation in the tropical Indian Ocean driven by interplay between the regional monsoon and global teleconnections

Saraswat, R., Lea, D. W., Nigam, R., Mackensen, A. and Naik, D. K.: Deglaciation in the tropical Indian Ocean driven by interplay between the regional monsoon and global teleconnections, Earth and Planetary Science Letters, 375, 166–175, doi:10.1016/j.epsl.2013.05.022, 2013.

Following Lea et al. (2000), the Mg/Ca-based temperature and ?18Ocalcite were used to calculate ?18Osw estimates.

Element2 ICP-MS at Woods Hole Oceanographic Institution or an Element XR ICP-MS at Rutgers University

reductive cleaning step; Mg/Ca calibration adjusted to account for 10% reduction in Mg/Ca ratio

Gibbons, F. T., Oppo, D. W., Mohtadi, M., Rosenthal, Y., Cheng, J., Liu, Z. and Linsley, B. K.: Deglacial δ18O and hydrologic variability in the tropical Pacific and Indian Oceans, Earth and Planetary Science Letters, 387, 240–251, doi:10.1016/j.epsl.2013.11.032, 2014.

LJ (04/12/2017): the Paleoceanography and NGeo age models differed where samples from G. bulloides were merged for measurements. This age model probably needs redoing.

d18Osw =-(4.64-SQRT(4.64^2-0.36*(16.1-temperature)))/0.18+d18Oc+0.27. Note that the values archived at NCDC contained a -0.68 permil vital effect correction, but according to P. Moffa-Sanchez this is uncertain and possibly applied with the wrong sign. So it is left out here

d18Osw =-(4.38-SQRT(4.38^2-0.4*(16.9-temperature)))/0.2+d18Oc+0.2. Note that the values archived on NCDC contained a typo

Moffa-Sanchez, P., Hall, I. R., Barker, S., Thornalley, D. J. R. and Yashayaev, I.: Surface changes in the eastern Labrador Sea around the onset of the Little Ice Age, Paleoceanography, 29(3), 160–175, doi:10.1002/2013pa002523, 2014.

Moffa-Sanchez, P., Born, A., Hall, I. R., Thornalley, D. J. R. and Barker, S.: Solar forcing of North Atlantic surface temperature and salinity over the past millennium, Nature Geoscience, 7(4), 275–278, doi:10.1038/ngeo2094, 2014.

Thermo Scientific Element XR Inductive Coupled Plasma Mass Spectrometry

Bartels-Jonsdottir, H. B., Voelker, A. H. L., Abrantes, F. G., Salgueiro, E., Rodrigues, T. and Knudsen, K. L.: High-frequency surface water changes in the Tagus prodelta off Lisbon, eastern North Atlantic, during the last two millennia, Marine Micropaleontology, 117, 13–24, doi:10.1016/j.marmicro.2015.03.001, 2015.

ICP-OES [Agilent Technologies, 700 Series with autosampler (ASX-520 Cetac) and micro-nebulizer]

splice of GeoB6211-1 and GeoB6211-2, age model is after Voigt et al. Needs updating to account for higher resolution of Chiessi

Voigt, I., Chiessi, C. M., Prange, M., Mulitza, S., Groeneveld, J., Varma, V. and Henrich, R.: Holocene shifts of the southern westerlies across the South Atlantic, Paleoceanography, 30(2), 39–51, doi:10.1002/2014pa002677, 2015.

Thus by comparison of sea surface changes during the past several decades, it is reasonable to interpret the foraminiferal isotopic data mostly in terms of SST change.

record contains two subcores from same box core; in the paper theyve been aligned using CaCO3 and 14C

Keigwin, L. D.: The Little Ice Age and Medieval Warm Period in the Sargasso Sea, Science, 274(5292), 1504–1508, doi:10.1126/science.274.5292.1504, 1996.

N. dutertrei d18O as indicator of conditions near the base of the local thermocline

G. ruber white d18O as monitor of annual average conditions in the near surface (see abstract)

G. ruber pink d18O as monitor of summer-fall nonupwelling season conditions

G. bulloides d18O (see abstract): sea surface conditions during the winter-spring upwelling season

Lin, H.-L., Peterson, L. C., Overpeck, J. T., Trumbore, S. E. and Murray, D. W.: Late Quaternary climate change from δ18O records of multiple species of planktonic foraminifera: High-resolution records from the Anoxic Cariaco Basin, Venezuela, Paleoceanography, 12(3), 415–427, doi:10.1029/97pa00230, 1997.

Basically, the oxygen isotope record represents the glacial- interglacial eustatic sea level change. This change is superimposed by small-scale variations of the freshwater influence by precipitation and runoff, i.e., +0.2960 for the glacial and deglaciation and reaching as high as +0.796o in the Holocene.

averaged calendar ages used in smooth-spline fit (see ref2 for discussion).

Wang, L., Sarnthein, M., Grootes, P. M. and Erlenkeuser, H.: Millennial reoccurrence of century-scale abrupt events of East Asian Monsoon: A possible heat conveyor for the global deglaciation, Paleoceanography, 14(6), 725–731, doi:10.1029/1999pa900028, 1999.

Master Shell Growth Chronology,  Arctica islandica, normalized, standard chronology

All micromilled samples were analyzed at the ISU Stable Isotope Laboratory for δ18O and δ13C on a ThermoFinnigan Delta Plus XL mass spectrometer coupled with a GasBench II and CombiPal autosampler.

QC certified, pending change in unique ID to reflect 2016 publication date

The unsmoothed I´18Oshell time series exhibits a relatively strong, negative relationship with the annual AMO index (ra€‰=a€‰aˆ’0.55; adjusted pa€‰<a€‰0.001; Januarya€“December) over 113 yr (1900a€“2012).

The annual d18Oshell time series each show relatively strong, negative correlations with a broad swath of North Atlantic SSTs during the satellite era

A. islandica appears to pre-cipitate its aragonitic shell matrix in oxygen isotopic equilib-rium with ambient seawater (e.g., Weidman et al. 1994). Thus,oxygen isotope values ofA. islandicashell material reflect sea-water temperature and seawater isotopic composition (relatedto salinity) (Marsh et al. 1999; Sch€one et al. 2004; Wanamakeret al. 2009).

Mette, Madelyn; Wanamaker, Alan D.; Carroll, Michael L.; Ambrose, William G.; Retelle, Michael J.

Linking large-scale climate variability withArctica islandicashell growth and geochemistry in northern Norway

Mette, M. J., Wanamaker, A. D., Carroll, M. L., Ambrose, W. G. and Retelle, M. J.: Linking large-scale climate variability withArctica islandicashell growth and geochemistry in northern Norway, Limnology and Oceanography, 61(2), 748–764, doi:10.1002/lno.10252, 2015.

datasetName (column B) is invalid; "isotope interpretation1,2,3" are missing -BK DMT 1/14 Isotope interp fixed.  Not sure how to fix column B (Nick issue?)

Modern drought conditions in western Sahel unprecedented in the past 1600 years

Carre, M., Azzoug, M., Zaharias, P., Camara, A., Cheddadi, R., Chevalier, M., Fiorillo, D., Gaye, A. T., Janicot, S., Khodri, M., Lazar, A., Lazareth, C. E., Mignot, J., Mitma Garcia, N., Patris, N., Perrot, O. and Wade, M.: Modern drought conditions in western Sahel unprecedented in the past 1600 years, Climate Dynamics, 52(3-4), 1949–1964, doi:10.1007/s00382-018-4311-3, 2018.

Trace ThermoFisher GC, Finnigan GC Combustion III module, Finnigan MAT Delta+ XL mass spectrometer at Carnegie Institution

; archiveType changed - was originally Terrestrial Sediment/Loess (SL)

isotope interpretation 1 should be P_isotope? and move "precipitation amount" to climate fields. -BK

dDn-C26 data unambiguously if perhaps qualitatively reflect changes in precipitation despite potentially confounding influences of vegetation type and other factors. "The dD values of the fatty acids from land-plant sources (n-C26, n-C28, n-C30) were significantly correlated to one another in each site"

precipitation occurs in closest proximity to the bulk of global cloud formation and its dD values are most influenced by its amount. dD values de- crease as precipitation amount increases (Risi et al., 2008). Additional factors shape the dD values of fatty acids in land-plants as well but their consideration below suggests that our dDn-C26 sequences were unambiguously if qualita- tively reflecting changes in amount of precipitation.

Plant to plant differences in fractionations between dD values of n-alkyl compounds and their precipitation source may introduce the greatest error in interpreting rainfall amount.

Terwilliger, Valery J. , Eshetu, Zewdu , Disnar, Jean-Robert , Jacob, Ji¿½ri¿½my , Paul Adderley, W. , Huang, Yongsong , Alexandre, Marcelo , Fogel, Marilyn L.

Environmental changes and the rise and fall of civilizations in the northern Horn of Africa: An approach combining ?D analyses of land-plant derived fatty acids with multiple proxies in soil

Terwilliger, V. J., Eshetu, Z., Disnar, J.-R., Jacob, J., Paul Adderley, W., Huang, Y., Alexandre, M. and Fogel, M. L.: Environmental changes and the rise and fall of civilizations in the northern Horn of Africa: An approach combining δD analyses of land-plant derived fatty acids with multiple proxies in soil, Geochimica et Cosmochimica Acta, 111, 140–161, doi:10.1016/j.gca.2012.10.040, 2013.

HP 6890 GC, AS 200 autosampler, Finnigan GC Combustion III module, Finnigan MAT Delta+ XL mass spectrometer at Brown University and Trace ThermoFisher GC, Finnigan GC Combustion III module, Finnigan MAT Delta+ XL mass spectrometer at Carnegie Institution

The oxygen fractionation between these modern straw stalactites and the average drip water corresponds to the equilibrium fractionation calculated from the O?Neil et al. (1969) calcite?water calibration at cave temperatures of 16i¿½C (Peqiin) and 18i¿½C (Soreq).

The association of minimum d18O values in speleothems with high cave water stands indicative of increased rainfall on land, and the coincidence of the corresponding low d18O G. ruber values with sapropel events indicative of enhanced rainfall above the Mediterranean Sea, demonstrate that both land and sea systems simultaneously experienced enhanced rainfall during these events

The modern analog supporting the association of enhanced rainfall with minimum speleothem I´18O values is the present-day relationship between decreasing rainfall I´18O and increasing annual rainfall amount (Fig. 4).

Bar-Matthews, M. , Ayalon, A. , Gilmour, M. , Matthews, A. , Hawkesworth, C. J.

Bar-Matthews, M., Ayalon, A., Gilmour, M., Matthews, A. and Hawkesworth, C. J.: Sea–land oxygen isotopic relationships from planktonic foraminifera and speleothems in the Eastern Mediterranean region and their implication for paleorainfall during interglacial intervals, Geochimica et Cosmochimica Acta, 67(17), 3181–3199, doi:10.1016/s0016-7037(02)01031-1, 2003.

Bar-Matthews, M., Ayalon, A. and Kaufman, A.: Late Quaternary Paleoclimate in the Eastern Mediterranean Region from Stable Isotope Analysis of Speleothems at Soreq Cave, Israel, Quaternary Research, 47(2), 155–168, doi:10.1006/qres.1997.1883, 1997.

modified dental drill with 500 micro meter diameter drill bit, sampling at 1-3 mm intervals

repetition test comparing stable isotopic records from 3 cave sites (Cold Water Cave, Cresco, Iowa; Mystery Cave, Wykoff, Minnesota; Spring Valley Cave, Spring Valley, Monnesota), similar stable isotopic signals of the records indicate that they reflect environmental rather than kinetic effects.

known effects of photosynthesis pathways used by plants on the d13C of soil CO2 and of evaporation on soil water d18O

the position between the ecotone of desiduous forests and prairy

more positive values of d13C indicate a spread of C4 prairy grasses and decline of C3 forest plants, more positive d18O indicates evaporation of soil water which is stronger in the prairy environment than in the forsest

effects of temperature on d18O in rainfall and alterations of the d18O of soil- and ground water due to evaporation

Difference between the d13C of soil CO2 in areas with C3 and C4 vegetation

Denniston, R. F., Gonzalez, L. A., Baker, R. G., Asmerom, Y., Reagan, M. K., Edwards, R. L. and Alexander, E. C.: Speleothem evidence for Holocene fluctuations of the prairie-forest                 ecotone, north-central USA, The Holocene, 9(6), 671–676, doi:10.1191/095968399674716399, 1999.

"Oxygen isotope analyses were performed at the Isotope Laboratory, Institute of Karst Geology, Guilin, China, using a VG MM-903 gas mass spectrometer (for Dongge Cave D3 and D4 analyses, except for D4 between 15.81 ky and 9.98 ky); at the State Key Laboratory of Loess and Quaternary Geology, Insti- tute of Earth Environment, Xi?an, China, using a Finni- gan MAT 252 Kiel Device III (Dongge Cave D4 be- tween 15.81 and 9.98 ky); and on a Finnigan MAT 251 at the Nanjing Institute of Geology and Paleontology, Chinese Academy of Sciences (Hulu Cave H82 be- tween 15.34 and 16.30 ky before the present)."

sample D4 and H82 from Hulu Cave (Wang, et al., 2001) replicate, however "In detail, D3 and D4 do not replicate perfectly, with some times characterized by differences in  18O that are large as compared to analytical error but small compared to the amplitude of the record (Fig. 2). These discrepancies are likely due to kinetic effects, water/rock interactions, and/or differential evapora- tion of water at the land surface."

There is little evidence for kinetic fractionation on the basis of C and O isotope correlations. C and O isotope ratios do not correlate strongly for any of the three stalag- mites in this study or even for portions of these stalagmites. The highest R2 value for any of the three stalagmites is 0.27 (table S6). Because the top of D4 was deposited in isotopic equilibrium and because a portion of D4 replicates the Hulu record, D4 is less likely to have been affected by kinetic effects or water/rock interactions than D3.

ZK (07/01/2019): Pre-Holocene part of the D4 stal. No data from the past 2000yrs

Interpretations of changes in precipitation d18O have focused on (i) the correlation be- tween mean annual temperature and  18O of modern meteoric precipitation [for temperatures  10i¿½C (15)] and (ii) the anticorrelation between rainfall amount and precipitation d18O [the ?amount effect? (15)]. However, modern precipitation d18O trends basically result from the progressive removal of water vapor from air masses as they move from moisture source regions, resulting in decreasing water vapor and precipitation d18O, which explains the first-order observation of lower precipitation d18O values at higher lat- itudes. Precipitation d18O at Hulu/Dongge is therefore largely a measure of the fraction of water vapor removed from air masses be- tween the tropical Indo-Pacific and southeastern China.

To estimate absolute amounts of rainfall integrated from sources to southeast China, we must make assumptions about absolute humidity in tropical source regions. Even assuming a glacial relative humidity as high as today?s and only a modest tropical temper- ature depression (2.5i¿½C), we calculate an ab- solute tropical glacial vapor pressure that is 85% of today?s and 79% of mid-Holocene/ Last Interglacial values (at a mid-Holocene temperature 1i¿½C greater than today and con- stant relative humidity). Coupled with the Rayleigh calculations, the amount of precip- itation integrated between tropical sources and southeast China is today  87% of mid- Holocene/Last Interglacial values and was  65% of mid-Holocene/Last Interglacial val- ues at glacial times corresponding to the heaviest Hulu/Dongge calcite  18O values, indicating that this region was significantly drier during glacial times.

R. E. Criss, Principles of Stable Isotope Distribution (Oxford Univ. Press, New York, 1999), p. 108.

ZK (07/01/2019): Pre-Holocene part of the D4 stal, NM: It looks like this one does now have data from the past 2k. I've made this the only primary timeseries. ZK (07/01/2019): Pre-Holocene part of the D4 stal. No data from the past 2000yrs

Yuan, D.: Timing, Duration, and Transitions of the Last Interglacial Asian Monsoon, Science, 304(5670), 575–578, doi:10.1126/science.1091220, 2004.

Yuan, D., H. Cheng, R.L. Edwards, C.A. Dykoski, M.J. Kelly, M. Zhang, J. Qing, Y. Lin, Y. Wang, J. Wu, J.A. Dorale, Z. An, and Y. Cai

on-line, automated, carbonate preparation system linked to a Finnigan Delta XL ratio mass spectrometer at the University of Massachusetts

; archiveType changed - was originally Speleothem (SP); archiveType changed - was originally Speleothem (SP)

Thus, changes in convective intensity within the SASM/SACZ may significantly contribute to and reinforce the effect that the location of this system has on the d18O of precipitation.

Cruz, F. W., Burns, S. J., Karmann, I., Sharp, W. D., Vuille, M., Cardoso, A. O., Ferrari, J. A., Silva Dias, P. L. and Viana, O.: Insolation-driven changes in atmospheric circulation over the past 116,000 years in subtropical Brazil, Nature, 434(7029), 63–66, doi:10.1038/nature03365, 2005.

white, densely crystalline low-Mg calcite,  showing columnar-shape crystals in thin section

The d13C profile shows no correlation with d18O in any of the section profiles

the relationship between temperature and isotopic composition results from a mixing of different types of precipitation that varies with temperature.

Tuning delivers a high correlation between y18O in SPA 12 and D14C (r =0.61). The maxima of d18O coincide with solar minima (Dalton, Maunder, Sporer, Wolf, as well as with minima at around AD 700, 500 and 300).

Mangini, A., Spoetl, C. and Verdes, P.: Reconstruction of temperature in the Central Alps during the past 2000 yr from a δ18O stalagmite record, Earth and Planetary Science Letters, 235(3-4), 741–751, doi:10.1016/j.epsl.2005.05.010, 2005.

statistically significant positive covariation between d18O and d13C (r=0.55,n=103, p<0.01)

The four diverse proxies attained extreme values ca. 4.1?3.8 ka, which corresponds to an interval of reduced moisture  reaching the cave interior."   "A simultaneous reduction in rainfall across the Mediterranean and the northern sector of the Middle East is actually consistent with a positive NAO phase (Cullen and deMenocal, 2000; Hurrell et al., 2003)."

Variations in NAO (related to the amount of rainfall. Season not specified)

Drysdale, R., Zanchetta, G., Hellstrom, J., Maas, R., Fallick, A., Pickett, M., Cartwright, I. and Piccini, L.: Late Holocene drought responsible for the collapse of Old World civilizations is recorded in an Italian cave flowstone, Geology, 34(2), 101, doi:10.1130/g22103.1, 2006.

The analyses were performed in two locations: (1) Institute of Earth Environment, Xi?an, China and (2) the Minnesota Isotope Laboratory, Minneapolis, USA. Both locations use a Finnigan-MAT 252 mass spectrometer fitted with a Kiel Carbonate Device III.

Yuan et al. [12] observed that other northern low- latitude sites around the world (Venezuela, [24]; and Israel, [25]) record y18O changes similar to China that are inverted with respect to the y18O record in Greenland. However, these sites do not record the strong seasonal difference in precipitation observed in China. To broaden the interpretation of y18O values to these other sites, Yuan et al. [12] modified the previous explanation by describing how changes in the percentage of water vapor lost prior to reaching the subtropics varied over time using a Rayleigh fractionation model [26]. Integrated rainfall from  tropical sources to SE China during glacial times was calculated to be 65% of that during the mid-Holocene [12]. Thus, following this interpretation, changes in the proportion of precipitation reaching China corre- late with changes in Greenland temperature. The Yuan et al. [12] mechanism provides a single explanation for the fact that the y18O relationship seen in the northern tropics and subtropics at multiple sites is inverted with respect to Greenland.,evidence of equilibrium found from (1) lack of correlation between d18O and d13C and (2) Replicated sample from the same cave with different dripwater properties,groundwater d18O,from 1 to 19,,,,years,,,,,,Fraction of water vapor lost from an air mass,2,year,,,,,,,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1OyOWgsBrRwp5sjVgqS1GFO2wnRkwGNY4wUXIpib45N4 SP06RACA01,SP06RACA,,SP06RACA01,Speleothem (SP),,Carlsbad.Rasmussen.2006,2006,10.1029/2006GL025714,,,,,,,,,, ,,,,32.1,104.26,,Carlsbad cave,,,LaminaeThickness,mm,Annual growth bands from two stalagmites sampled in two nearby caves,,number and thickeness of stalagmite layers,rainfall amount,Pacific-modulated precipitation variability during the late Holocene from the southwestern USA: mechanisms driving drought cycles,annual,,the thickness of the laminae decrease during periods of drought,,,,The data are supported by U-Th results,,,years,It has been demonstrated that some speleothems from the Guadalupe Mountains in southeastern New Mexico are annually banded, and variations in band thickness and mineralogy can be used as a record of regional relative moisture [Asmerom and Polyak, 2004].,,Changes in precipitation over relatively short time periods are indicated by hiatuses in stalagmite growth and large-scale shifts in band thickness,,,no isotopic analyes here,1,,,,,,,,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1bxnCwCgUbDr2MFZp193p1MHzpsTuqPZuBYBzy1LcMCU SP07ASUS01A,SP07ASUS,,SP07ASUS01A,Speleothem (SP),,Asmerom, P,2007,10.1130/G22865A.1,,,,,,,,,, ,,,,32.083,-105.1667,,Pink Panter Cave, New Mexico,,,d18O,parts per mil,stable isotopes (d18O),,calcite powder,rainfall amount,more positive d18O values are interpreted to represent wetter conditions,under present conditions, wet years often have higehr amount of winter rain, but d18O may reflect high summer rain, winter rain, or both,negative,observed negative correlation between summer monsoon rainfall amount and d18O,,groundwater d18O,7-71,,,,years,observed negative correlation between summer monsoon rainfall amount and d18O,,negative,,,isotopic composition of rainfall,2,,,,,,,,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1TLPUcn1ABQX_Rf5RWRDie6kyNZ6ZrNhq04Dpv-l2FvQ SP07DEUS01A,SP07DEUS,,SP07DEUS01A,Speleothem (SP),,Denniston, RF,2007,10.1016/j.yqres.2007.04.001,,,,,,,,,, ,,,,38.9,-92.3,,Devils Icebox Cave, Missouri,,,d18O,parts per mil,stable isotopes (d18O),,calcite powder,rainfall amount,more poritive d13C values reflect less rainfall amount,,negative,The influence of vegetation changes and changes in the water residence time on d13C of DIC. Drier conditions cause an increase of C4 plants in the vegetation and longer residence times of water in the bedrock (increasing the contribution of bedrock carbonate to DIC). Either one would cause an increase of d13C in the speleothem. Temperature changes may have a similar effect but would also affect d18O. Since d18O values are stable a temperature effect therefore can be eliminated.,repetition test comparing d18O and d13C of two speleothems shows similar trends,d13C of DIC; groundwater d18O,10-100,age model,,,years,,,,,,precipitation amount,,,,,,,,,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1CKvU6bQUbaqK0SdowSO09No7Z9Hfx3wxtlzWgwIMamk SP07DEUS01A_d13C,SP07DEUS,,,Speleothem (SP),,Denniston, RF,2007,10.1016/j.yqres.2007.04.001,,,,,,,,,, ,,,,38.9,-92.3,,Devils Icebox Cave, Missouri,,,d13C,parts per mil,stable isotopes (d13C)  ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1CKvU6bQUbaqK0SdowSO09No7Z9Hfx3wxtlzWgwIMamk SP07FLOM01A,SP07FLOM,,SP07FLOM01A,Speleothem (SP),,Fleitmann, D,2007,10.1016/j.quascirev.2003.06.019,,,,,,,,,, ,,,,17.17,54.3,,Qunf Cave, Oman,,,d18O,parts per mil,stable isotopes d18O,,calcite powder,Indian Summer Monsoon,more negative values of d18O are interpreted as indicative of increased monsoon strength,year round,negative,Based on previously published results from Oman and Yemen, we interpret the oxygen isotope ratios of stalagmite calcite to primarily reflect variations in the amount of rainfall (termed ??amount effect??; Dansgaard, 1964;Rozanski et al., 1992), with more negative d18O reflecting higher monsoon rainfall (Burns et al., 1998, 2001, 2003; Neff et al., 2001; detailed discussion in Fleitmann et al., 2004). This interpretation is substantiated by isotopic time series of tropical precipitation (Dansgaard, 1964; Rozanski et al., 1992; Johnson and Ingram, 2004) and paleoclimate records from the ASM domain (e.g., Wei and Gasse, 1999; Wang et al., 2001, 2005; Dykoski et al., 2005), which confirm the inverse relationship between d18O and the amount of precipitation in regions affected by monsoons"

East Asian Monsoon Strength; more negative values of d18O are interpreted as indicative of increased monsoon strength

DYKOSKI, C., EDWARDS, R., CHENG, H., YUAN, D., CAI, Y., ZHANG, M., LIN, Y., QING, J., AN, Z. and REVENAUGH, J.: A high-resolution, absolute-dated Holocene and deglacial Asian monsoon record from Dongge Cave, China, Earth and Planetary Science Letters, 233(1-2), 71–86, doi:10.1016/j.epsl.2005.01.036, 2005.

observed negative correlation between summer monsoon rainfall amount and d18O

under present conditions, wet years often have higehr amount of winter rain, but d18O may reflect high summer rain, winter rain, or both

more positive d18O values are interpreted to represent wetter conditions

summer is the main rainfall season with moisture sources primarily in the Gulf of Mexico and generally high values (~-3 permil) - these values however change depending on the amount of rainfall; winter rain has lower amounts and sources in the Pacific Ocean with lower values (~-11 permill).

Asmerom, Y., Polyak, V., Burns, S. and Rassmussen, J.: Solar forcing of Holocene climate: New insights from a speleothem record, southwestern United States, Geology, 35(1), 1, doi:10.1130/g22865a.1, 2007.

repetition test comparing d18O and d13C of two speleothems shows similar trends

LCB: Two stals from the same cave are not cleraly distinguished in the lipdverse. This happens with all names ending 01A 02A 03A, for example

d18O values are comparatively stable which is interpreted to reflect stable temperature in the region.

Increase of d13C may generally be associated with increase of the proportion of C4 plants in the vegetation or increase of the contribution of bedrock carbonate to the DIC - both are more likely in drier conditions. Stable d18O values suggest that changes in temperature were minor.

The influence of vegetation changes and changes in the water residence time on d13C of DIC. Drier conditions cause an increase of C4 plants in the vegetation and longer residence times of water in the bedrock (increasing the contribution of bedrock carbonate to DIC). Either one would cause an increase of d13C in the speleothem. Temperature changes may have a similar effect on d13C as would changes  in the rainfall amount but would also affect d18O. Since d18O values are stable a temperature effect therefore can be eliminated.

Denniston, R. F., DuPree, M., Dorale, J. A., Asmerom, Y., Polyak, V. J. and Carpenter, S. J.: Episodes of late Holocene aridity recorded by stalagmites from Devil’s icebox Cave, Central Missouri, USA, Quaternary Research, 68(1), 45–52, doi:10.1016/j.yqres.2007.04.001, 2007.

automated carbonate system linked to a VG PRISM ratio mass spectrometer (except for stalagmite D1 that isotope ratios were measured on a Delta-plusXL mass spectrometer equipped with an automated carbonate preparation system Kiel III)

Replicate results from 4 samples that overlap during certain periods of time

Based on previously published results from Oman and Yemen, we interpret the oxygen isotope ratios of stalagmite calcite to primarily reflect variations in the amount of rainfall (termed ??amount effect??; Dansgaard, 1964;Rozanski et al., 1992), with more negative d18O reflecting higher monsoon rainfall (Burns et al., 1998, 2001, 2003; Neff et al., 2001; detailed discussion in Fleitmann et al., 2004). This interpretation is substantiated by isotopic time series of tropical precipitation (Dansgaard, 1964; Rozanski et al., 1992; Johnson and Ingram, 2004) and paleoclimate records from the ASM domain (e.g., Wei and Gasse, 1999; Wang et al., 2001, 2005; Dykoski et al., 2005), which confirm the inverse relationship between d18O and the amount of precipitation in regions affected by monsoons

Indian Summer Monsoon; more negative values of d18O are interpreted as indicative of increased monsoon strength

Fleitmann, D., Burns, S. J., Neff, U., Mudelsee, M., Mangini, A. and Matter, A.: Palaeoclimatic interpretation of high-resolution oxygen isotope profiles derived from annually laminated speleothems from Southern Oman, Quaternary Science Reviews, 23(7-8), 935–945, doi:10.1016/j.quascirev.2003.06.019, 2004.

Finnigan MAT 252 mass spectrometer equipped with a Kiel II Carbonate Device at the Minnesota Isotope Laboratory

Low(high)Botuvera? speleothem d18O indicates intensified (weakened) SASM activity, more (less) Amazon moisture contribution and higher (lower) rainfall in southern Brazil.

Wang, X., Auler, A. S., Edwards, R. L., Cheng, H., Ito, E., Wang, Y., Kong, X. and Solheid, M.: Millennial-scale precipitation changes in southern Brazil over the past 90,000 years, Geophysical Research Letters, 34(23), n/a–n/a, doi:10.1029/2007gl031149, 2007.

HS-4 and HS-6 overlapped neatly (another sample from Heshang cave)

Hendy test; lack of correlation between d13C and d18O; replicated stalagmite; prediction from equilibrium constraints matches top values

Secondary controls can, however, be removed from the d18O record by comparing d18O from two stalagmites growing along the same atmospheric moisture transport pathway. As long as both stalagmites grew without kinetic or evaporative modification of their d18O signals, then the difference between d18O at the two sites only reflects loss of moisture from the atmosphere by rainfall as the air travels between them. The magnitude of the difference in d18O between the two sites reflects the amount of rain removed.

Hu, C., Henderson, G. M., Huang, J., Xie, S., Sun, Y. and Johnson, K. R.: Quantification of Holocene Asian monsoon rainfall from spatially separated cave records, Earth and Planetary Science Letters, 266(3-4), 221–232, doi:10.1016/j.epsl.2007.10.015, 2008.

GasBench II coupled to a ThermoFinnigan DeltaPlusXP isotope ratio mass spectrometer

Sr/Ca ratios can be used to reconstruct relative rates of epikarstic moisture transport because low moisture levels can cause 1) increased drip water residence times, leading to 2) Ca drawdown via calcite precipitation in the overlying epikarst, which increases Sr/Ca ratios in the residual drip waters and their dependent speleothems

Springer, G. S., Rowe, H. D., Hardt, B., Edwards, R. L. and Cheng, H.: Solar forcing of Holocene droughts in a stalagmite record from West Virginia in east-central North America, Geophysical Research Letters, 35(17), doi:10.1029/2008gl034971, 2008.

AA (2019-03-08): Data is wonky (e.g. age ranges from -8E9 to 8E9). LCB: Time should cover the last 14k. MJ (30/12/19) there are two speleothems in the paper, one covers the last c. 4k, one from c. 4 to c. 14ka.

AA (2019-03-08): Data is wonky (e.g. age ranges from -8E9 to 8E9)

Fossil dripwater in stalagmites reveals Holocene temperature and rainfall variation in Amazonia

Van Breukelen, M. R., Vonhof, H. B., Hellstrom, J. C., Wester, W. C. G. and Kroon, D.: Fossil dripwater in stalagmites reveals Holocene temperature and rainfall variation in Amazonia, Earth and Planetary Science Letters, 275(1-2), 54–60, doi:10.1016/j.epsl.2008.07.060, 2008.

"stable isotopic composition on a Thermo? Finnigan Delta Plus Mass Spectrometer at Lanzhou University, China,"

A Hendy Test (S3) shows no substantial isotopic fractionation along the same growth layer and correlations between ?18O and ?13C are statistically insignificant, suggesting that the stalagmite calcite was deposited in isotopic equilibrium (Fig. S3). This agrees with observations from modern carbonate?water stable isotope systematics (S4) from the same cave.

The correlation coefficient between calcite ?18O and annual precipitation is r = -0.64 (n = 48, Figure S4). This anti- correlation on multi-decadal to interannual timescales is consistent with previous observations on orbital and millennial timescales from Wanxiang Cave (S4) and Hulu and Dongge Caves (S1, S2).

Summer AM precipitation is driven by the thermal contrast between Asia and the tropical Indo-Pacific and therefore should be linked to regional temperature change (16). Based on an ECHO-G climate model simulation (SOM), we modeled Chinese air temperature for the past millennium, with results that were broadly con- sistent with our record (r = ?0.46 and n = 345 data points), particularly with regard to centen- nial and multicentennial time scales and with regard to the distinct double peak in both model output and record during the MWP (Fig. 3A).

Zhang, P., Cheng, H., Edwards, R.L., Chen, F., Wang, Y., Yang, X., Liu, J., Tan, M., Wang, X., Liu, J., An, C., Dai, Z., Zhou, J., Zhang, D., Jia, J., Jin, L., Johnson, K.R.

Zhang, P., Cheng, H., Edwards, R. L., Chen, F., Wang, Y., Yang, X., Liu, J., Tan, M., Wang, X., Liu, J., An, C., Dai, Z., Zhou, J., Zhang, D., Jia, J., Jin, L. and Johnson, K. R.: A Test of Climate, Sun, and Culture Relationships from an 1810-Year Chinese Cave Record, Science, 322(5903), 940–942, doi:10.1126/science.1163965, 2008.

Finnigan Delta V Advantage mass spectrometer equipped with an automated carbonate preparation system (Gas Bench-II) at the Institute of Geological Sciences, University of Bern.

Precision of d13C and d18O measurements is 0.06% and 0.07% (1s-error) respectively.

Isotope profiles of all stalagmites are very similar, indicating that So-1 d18O and d13C values are not biased by site-, cave- or sample-specific effects (e.g., kinetic fractionation effects), and furthermore that the So-1 record can be used with confidence for environmental and climatic reconstructions.

TP: elevation estimate from Google Earth. ZK, BM 04/01/2019:  we thought we have to change 'Moisture source' to 'precipitation_Isotope' in column BG; but we can not add a single term to the interpretation, even the direction of the interpretation is problematic ... so one possible solution would be to change this record from 'primary timeseries' to non 'primary timeseries'? but discussed with Bronwen during and we have to discuss this further before qualifying as  'FALSE' in column CB (intended mainly for sites with 2 possible records ans flagging the one to be used)

Fleitmann, D., Cheng, H., Badertscher, S., Edwards, R. L., Mudelsee, M., Goektuerk, O. M., Fankhauser, A., Pickering, R., Raible, C. C., Matter, A., Kramers, J. and Tueysuez, O.: Timing and climatic impact of Greenland interstadials recorded in stalagmites from northern Turkey, Geophysical Research Letters, 36(19), doi:10.1029/2009gl040050, 2009.

LR06-B1 - continuous-flow GV2003 gas-source isotope ratio mass spectrometer at the University of Newcastle, Australia; LR06-B3 - automated individual-carbonate reaction Kiel device coupled to a Finnigan MAT-251 dual-inlet stable isotope mass spectrometer at the Research School of Earth Sciences, ANU.

To assess interlaboratory performance, 143 replicate samples from stalagmite LR06- B1were run on the GV2003 (at U. Newcastle) and the Finnigan MAT-251 (at ANU).

This isotopic difference is related primarily to the stronger convergence and uplift of water vapour over the southern Indonesian maritime continent during austral summer.

Australian-Indonesian Summer monsoon; More negative d18O values correspond to stronger amount

changes in the seasonal balance of summer versus winter rainfall

Griffiths, M. L., Drysdale, R. N., Gagan, M. K., Zhao, J. -x., Ayliffe, L. K., Hellstrom, J. C., Hantoro, W. S., Frisia, S., Feng, Y. -x., Cartwright, I., Pierre, E. S., Fischer, M. J. and Suwargadi, B. W.: Increasing Australian–Indonesian monsoon rainfall linked to early Holocene sea-level rise, Nature Geoscience, 2(9), 636–639, doi:10.1038/ngeo605, 2009.

TP: elevation estimate from Google Earth, AA: Decimal separators have been lost from the ages and isotope values (2019-03-08); BM (15/03/2019) info added using the LiPDverse_refers to Cascayunga Cave Speleothem CAS-A), issues sent using GitHub

TP: elevation estimate from Google Earth, AA: Decimal separators have been lost from the ages and isotope values (2019-03-08); BM (15/03/2019) info added using the LiPDverse_refers to Cascayunga Cave Speleothem CAS-D, issues sent using GitHub

Reuter, J., Stott, L., Khider, D., Sinha, A., Cheng, H. and Edwards, R. L.: A new perspective on the hydroclimate variability in northern South America during the Little Ice Age, Geophysical Research Letters, 36(21), doi:10.1029/2009gl041051, 2009.

An online automated carbonate preparation system linked to a VG Prism II isotope ratio mass spectrometer at the University of Southern California

equilibrium is evidenced by the lack of correlation among d18O and d13C, several Hendy test in laminations and calculations of explected d18O in modern calcite knowing cave temperatue and d18O from dripwaters (in a previous paper, Sinha et al. GRL (2007)

No chron data in current LiPD file, needs updating, updated fiel sent to Nick 31/12/19 (MJ)

more positive values of d18O are interpreted to reflect less rainfall throughout the "amount effect"

more negative values of d18O are interpreted as indicative of increased summer monsoon precipitation

Berkelhammer, M., Sinha, A., Mudelsee, M., Cheng, H., Edwards, R. L. and Cannariato, K.: Persistent multidecadal power of the Indian Summer Monsoon, Earth and Planetary Science Letters, 290(1-2), 166–172, doi:10.1016/j.epsl.2009.12.017, 2010.

Finnigan MAT-252 mass spectrometer equipped with Kiel Carbonate Device III in the Institute of Earth Environment, Chinese Academy of Sciences

equilibrium is evidenced by the Hendy test in several laminae and the lack of correlation among d18O and d13C

LCB (28/03/2019): one of the SP10CACN stals is at higher resolution but I cannot distinguish which is which in lipdverse to pick it as the primary one

Cai, Y., Tan, L., Cheng, H., An, Z., Edwards, R. L., Kelly, M. J., Kong, X. and Wang, X.: The variation of summer monsoon precipitation in central China since the last deglaciation, Earth and Planetary Science Letters, 291(1-4), 21–31, doi:10.1016/j.epsl.2009.12.039, 2010.

 A total of 1413 sub-samples for ?18O measurements were performed on a Finnigan MAT-253 mass spectrometer linked to an on-line automated preparation system (Kiel Carbonate Device) at the college of Geography Science, Nanjing Normal University.

Given differences in dating errors and resolution, the ?18O records are virtually identical during contemporaneous growth periods, providing a robust replication test for equilibrium calcite deposition.

BM (14/03/2019) info sent using GitHub: These are multiple entities for one cave: Sanbao cave,  lipd file has just sb49 (tab sb49 in the attachment), please add the other 5: dong et al., 2010, the holocene sanbao2010.xlsx, Stalagmite sb44 (tab sb44), Stalagmite sb43 (tab sb43) - relevant for Iso2k, Stalagmite sb26 (tab sb26) - relevant for Iso2k, Stalagmite sb27 (tab sb27), Stalagmite sb10 (tab sb10)

Weighted mean annual ?18O value for the period from 1988?1996 was ?7.0?, with more neg- ative   in summer months (average ~ ?9.5?, SMOW) and more positive ?18O in winter months (average ~ ?4.5?, SMOW). Therefore, more negative ?18O values are consistent with a greater contribution of summer rainfall

East Asian summer monsoon strength; more negative values of d18O are interpreted as indicative of increased monsoon precipitation

Jinguo Dong, Yongjin Wang, Hai Cheng, Hardt, B., Edwards, R. L., Xinggong Kong, Jiangying Wu, Shitao Chen, Dianbing Liu, Xiuyang Jiang and Kan Zhao: A high-resolution stalagmite record of the Holocene East Asian monsoon from Mt Shennongjia, central China, The Holocene, 20(2), 257–264, doi:10.1177/0959683609350393, 2010.

final record was smoothed with a 212 year filter and resampled at 60 year itnervals

lack of correlation of d18O and d13c along the growth axis; repetition test showing similar records for contemporaneous samples

BD missing, & column AW: is the included data series before or after filtering?  LCB: AFTER

LCB(29/03/2019): the first tab in lipdverse should be the primary series (no hiatuses). Don't know which one it is

changes of d18O in speleothems reflect changes of the average d18O of rainfall in the region related to rainfall seasonality

observed present day correlation between rainfall seasonality and d18O at a nearby station of the Global Network for Isotopes in precipitation

Changes in the strength of the Bermuda high cause variations of the amount of summer rain at the site; higher summer rain leads to more positive d18O in rainfall

Hardt, B., Rowe, H. D., Springer, G. S., Cheng, H. and Edwards, R. L.: The seasonality of east central North American precipitation based on three coeval Holocene speleothems from southern West Virginia, Earth and Planetary Science Letters, 295(3-4), 342–348, doi:10.1016/j.epsl.2010.04.002, 2010.

characteristics and physical conditions of Tzabnah cave, a Hendy test and isotopic equilibrium calculations (Sharp, 2007)

A calibration between Chaac ?18O and the instrumental record of precipitation from a meteorological station in Mi¿½rida indicates a significant correlation between the two signals (r=?0.62, P=0.023) with a slope of ?176 mm??1 increase in Chaac ?18O (Fig. 4). The strength of the relationship between Chaac ?18O and rainfall amount is similar to that observed between rainfall amount data from adjacent meteorological stations (0.2brb0.7, Pb0.01).

Uncertainty are just incremental integers in original document, which may be in error

Medina-Elizalde, M., Burns, S. J., Lea, D. W., Asmerom, Y., von Gunten, L., Polyak, V., Vuille, M. and Karmalkar, A.: High resolution stalagmite climate record from the Yucatan Peninsula spanning the Maya terminal classic period, Earth and Planetary Science Letters, 298(1-2), 255–262, doi:10.1016/j.epsl.2010.08.016, 2010.

on-line, automated carbonate preparation system linked to a triple collector gas source mass spectrometer at the University of Innsbruck.

Three Hendy tests were carried out, i.e. at 10mm (AD 70), 20mm (837 BC) and 33mm (1453 BC), based on 7, 7 and 5 samples, respectively. The variations of d18O along individual growth layers, expressed in I”d18O, are 0.31, 0.74 and 0.18%, respectively. The correlation between oxygen and carbon in one of the three layers, at 200 mm, is high, R=0.9 (P<0.01) indicating that kinetic effects may have occurred. The other two test did not show fractionation.

this relationship is supported by the observed similarities with both regional and hemispheric temperature reconstructions available for the past 500 and 2000 years, respectively

During cold climate periods, relatively less winter contribution to the cave drip water will result in relatively higher d18O values and vice versa.  Depleted/enriched oxygen isotopesisotopes are interpreted mainly to indicate relatively more/less winter precipitation and higher/lower summer evaporation reflecting warmer/colder conditions.

Three Hendy tests were carried out, i.e. at 10mm (AD 70), 20mm (837 BC) and 33mm (1453 BC), based on 7, 7 and 5 samples, respectively. The variations of d18O along individual growth layers, expressed in Δd18O, are 0.31, 0.74 and 0.18%, respectively. The correlation between oxygen and carbon in one of the three layers, at 200 mm, is high, R=0.9 (P<0.01) indicating that kinetic effects may have occurred. The other two test did not show fractionation.

average time resolution from 22 years at the top to 5 years at the base.

SUNDQVIST, H. S., HOLMGREN, K., MOBERG, A., SPATL, C. and MANGINI, A.: Stable isotopes in a stalagmite from NW Sweden document environmental changes over the past 4000 years, Boreas, 39(1), 77–86, doi:10.1111/j.1502-3885.2009.00099.x, 2010.

Automated individual-carbonate reaction (Kiel) device coupled with a Finnigan MAT252 mass spectrometer at the National Institute of Water and Atmospheric Research (NIWA).

Replication of the isotope signal in other stalagmites from other caves

not said, but ages were determined by TIMS or alpha-counting (info from Williams et al., 2005)

Evident relationship of speleothem ?18O and temperature, which is generally positive (Williams et al. 2004, 2005, Whittaker 2008). It is probable that significant changes to d18Op would have resulted from perturbations in oceanic and atmospheric circulation patterns that altered the relative mix of vapour from subtropical and sub-Antarctic sources

Changes in annual temperature modulated by oceanic circulation and gradients

There is a presend-day positive relationship between ?18O of precipitation and temperature of +0.35? / i¿½C.,Calculations with dripwater d18O values and calcite d18O values,,1 to 10,lamina counting, high resolution sampling to 100 microns,temperature,,year,,,,,,rainfall amount and source,,,,,,,,,,,,,https://docs.google.com/spreadsheets/d/1WNzh05-BveXAV0WvY6duO7iRR_drkRSgmosDu0BBmyU

Williams, P., Neil, H. and Zhao, J.-X.: Age frequency distribution and revised stable isotope curves for New Zealand speleothems: palaeoclimatic implications, International Journal of Speleology, 39(2), 99–112, doi:10.5038/1827-806x.39.2.5, 2010.

Williams, P. W., King, D. N. T., Zhao, J.-X. and Collerson, K. D.: Late Pleistocene to Holocene composite speleothem 18O and 13C chronologies from South Island, New Zealand—did a global Younger Dryas really exist?, Earth and Planetary Science Letters, 230(3-4), 301–317, doi:10.1016/j.epsl.2004.10.024, 2005.

poor correlation of d18O and d13C along the growth axis which is assumed to show low influence of kinetic fractionation. Hendy tests were not performed since sampling along single laminae was too difficult

observed cyclicity in the record and comparability with other pelaoclimate records which vary in phase with north Atlantic changes and ENSO

higher values are related to less rainfall - this can be realted to less moisture influex from the Caribbean due to a southward shift of the ITCZ in phases when high amounts of meltwater enter the cooling north Atlantic Ocean; after ~4.3 ka the connection to the north Atalatic is lost and ENSO becomes more important with warm ENSO events (El Nino) causing higher d18O

It is expected that the summer rainwater I´18O composition in southwestern Mexico is inversely proportional to the rainfall amount (Dansgaard, 1964). This is because southwestern Mexico is influenced by the same wind and climate patterns and moisture sources as Guatemala and Belize (Amador et al., 2006), where the amount effect has been observed to dominate the I´18O composition of rainfall and groundwater.

The main rainfall season is between May and October and associated with the ITCZ, moisture sources are in the Caribbean. Little rain falls in winter with sources in the Pacific Ocean. The amount effect leads to shifts of d18O in areas of Guatemala and Belize that are influenced by the same wind and climate patterns and moisture sources.

Bernal, J. P., Lachniet, M., McCulloch, M., Mortimer, G., Morales, P. and Cienfuegos, E.: A speleothem record of Holocene climate variability from southwestern Mexico, Quaternary Research, 75(1), 104–113, doi:10.1016/j.yqres.2010.09.002, 2011.

ThermoFisher DeltaplusXL isotope ratio mass spectrometer coupled to a ThermoFisher GasBench II.

the precision of the d13C and d18O values expressed as the 1-sigma standard deviation is 0.06 and 0.08%,

There is kinetic isotope fractionation: Strongly positive correlation between d13C and d18O values in the younger segments with Dd13C/Dd18O slopes of 1?1.5. The older parts of the cores are characterized by a significantly lower degree of correlation and typically lower slopes. Linear fits of d13C vs. d18O in cores PFU8 and PFU9 show comparable slopes (1?1.5) but typically lower coefficients (in particular PFU8). Modern calcite precipitates also exhibit a strongly positive correlation of C and O isotope values (R2=0.87). A comparison of the drill core d18O values with calculated modern O isotopic equilibrium values based on monitoring data reveals O isotopic compositions close to isotopic equilibrium only for the calcite d18O minima.

Four cores, 25mm in diameter and up to 50 cm long (PFU6, 7, 8, 9) from different parts of the flowstone as well as modern calcilte precipitates

Annual and homogenized precipitation data of the nearby station Nauders, however, reveal good correspondence with observed C and O isotope changes on a decadal timescale, considering the age uncertainties and different temporal resolution

variations in paleoprecipitation amount on a multi-annual timescale (On longer timescales, however, the flowstone?s growth dynamics have to be considered)

There is kinetic osotope fractionation: Strongly positive correlation between d13C and d18O values in the younger segments with Dd13C/Dd18O slopes of 1?1.5. The older parts of the cores are characterized by a significantly lower degree of correlation and typically lower slopes. Linear fits of d13C vs. d18O in cores PFU8 and PFU9 show comparable slopes (1?1.5) but typically lower coefficients (in particular PFU8). Modern calcite precipitates also exhibit a strongly positive correlation of C and O isotope values (R2=0.87). A comparison of the drill core d18O values with calculated modern O isotopic equilibrium values based on monitoring data reveals O isotopic compositions close to isotopic equilibrium only for the calcite d18O minima.

Lack of seasonal signal in stable isotopic composition + the drip-water trace element concentrations strongly suggesta that most of the water discharging into this cave has a mean residence time well in excess of one year.

uncertainty is higher on long timescales due to flowstone?s growth dynamics

10833’E, 46857’N (Klapferloch Cave (Austrian register no 2132/5)

Boch, R. and Spoetl, C.: Reconstructing palaeoprecipitation from an active cave flowstone, Journal of Quaternary Science, 26(7), 675–687, doi:10.1002/jqs.1490, 2011.

on-line, automated, carbonate preparation system linked to a Finnigan Delta Plus Advantage at the University of Sao Paulo

LCB (29/03/2019): One of the two does not cover the last 2k. The other one should be primary

d18O in precipitation is primarily controlled by the amount effect over areas such as northern Minas Gerais, where precipitation is fundamentally the result of SAMS activity

Strikis, N. M., Cruz, F. W., Cheng, H., Karmann, I., Edwards, R. L., Vuille, M., Wang, X., de Paula, M. S., Novello, V. F. and Auler, A. S.: Abrupt variations in South American monsoon rainfall during the Holocene based on a speleothem record from central-eastern Brazil, Geology, 39(11), 1075–1078, doi:10.1130/g32098.1, 2011.

equilibrium is evidenced by (1) the lack of correlation among d18O and d13C, (2) the application of fractionation equation with current d18O values in dripwaters and cave temperature and (3) replication with other caves

The interpretation is made for an older section of the sample. Last 2k data was not the focus of the manuscript

A low correlation between δ13C and δ18O values (r2=0.133) argues against kinetically driven fractionation during speleothem growth according to traditional Hendy criteria. This suggests that the speleothem most likely grew under isotopic equilibrium conditions. Fluctuations in δ18O values result mainly from changes in δ18O value of the drip water. In low latitude areas, the “amount effect”, i.e. a relationship where the δ18O of meteoric precipitation is negatively correlated with precipitation amount, is the major controlling factor of precipitation δ18O (Dansgaard, 1964; Rozanski et al., 1993) and often overshadows the dependence of δ18O on temperature in Asian monsoon regions (Araguas-Araguas et al., 1998, Wei and Gasse, 1999).

Cai, Y., Zhang, H., Cheng, H., An, Z., Lawrence Edwards, R., Wang, X., Tan, L., Liang, F., Wang, J. and Kelly, M.: The Holocene Indian monsoon variability over the southern Tibetan Plateau and its teleconnections, Earth and Planetary Science Letters, 335-336, 135–144, doi:10.1016/j.epsl.2012.04.035, 2012.

Hendy tests: stable d18O along growth layers and lack of correlation between d18O and d13C along growth layers

observed correlation between rainfall d18O and temperature; commonly found relationship of d13C with cave hydrology and biomass above the cave

positive for d18O-temperature relation, negative for d13C-precipiation amount

d18O changes of speleothems reflect effects of temperature on raifnall d18O, rainfall amounts affect cave hydrology and biomass density above the cave, which is recorded in d13C of speleothems

Speleothem d18O gets heavier as temperature increases, therefore this is P_isotope driven

age model: Markov Chain Monte-Carlo sampling and Bayesian statistics implemented in OxCal 4.1

commonly found relationship of d13C with cave hydrology and biomass above the cave

rainfall amounts affect cave hydrology and biomass density above the cave, which is recorded in d13C of speleothems

An increase in precipitation may cause lower speleothem d13C directly through its effects on cave hydrology and indirectly through its influence on surface biomass.

Regional climate in the Pacific Northwest is strongly influenced by atmosphere–ocean interactions that originate in the Pacific Ocean on seasonal, interannual, decadal and presumably also longer timescales. Strong seasonality develops from contrasts in ocean– continent heating, with relatively warm and dry summers associated with the northward migration of the Pacific subtropical high, and cool and wet winters associated with an intensification of the Aleutian low. Southward displacement of the Pacific subtropical high-pressure cell by the Aleutian low-pressure system brings a predominance of southwesterly winds and abundant precipitation during winter months.

Ersek, V., Clark, P. U., Mix, A. C., Cheng, H. and Lawrence Edwards, R.: Holocene winter climate variability in mid-latitude western North America, Nature Communications, 3(1), doi:10.1038/ncomms2222, 2012.

measured using an online, automated carbonate preparation system linked to a triple collector gas source mass spectrometer at the University of Innsbruck

Owing to the low cave temperature kinetic isotope effects are minimal (Mangini et al., 2005; Vollweiler et al., 2006).

Spannagel ?18O records and growth phases are in agreement with the ?18O pattern in Greenland ice cores on millennial to orbital timescales (Spi¿½tl and  Mangini, 2007 Spi¿½tl et al., 2006), with sediment proxies and growth of deep-sea corals from the North Atlantic (Frank et al., 2009; Mangini et al., 2005) and with other stalagmites from central Europe (Mangini et al., 2007). Trouet et al. (2009) found and discussed similarities of Spannagel speleothem ?18O values in  relation to their NAO reconstruction for the past 1000 yr based on speleothem data from Scotland (Proctor et al., 2000) and tree-ring data from Morocco (Esper et al., 2007). In addition, the super-regional character of our alpine location was explicitly demonstrated in a proxy intercomparison study investigating teleconnections between the tropical Pacific and mid-latitude regions (Graham et al., 2007).

variations in air temperature due to large-scale atmospheric patterns

The observed strong decrease in the ?18O by about 1.5? between 11 and 10 ka, for example, is rather a change of the source region than a pure temperature  effect. Based on this assumption, during the deglaciation the trajectories more frequently followed southerly routes. Towards the transition into the Holocene the main contribution of precipitation probably originated from more northern regions of the Atlantic, where the surface ocean is generally more depleted in 18O (LeGrande and Schmidt, 2006).

Average resolution of each stal 5.1 yr (SPA12), 3.5 yr (SPA128), 8 yr (SPA70), 4 yr (SPA127) and 1.6 yr (SPA133).

iscam method (Fohlmeister et al., 2012), based on simulations and correlation calculations between pairs of climate  records (this is a stack of 5 records). Point-wise linear interpolation between data points. Typical age errors are smaller than 2%.

Fohlmeister, J., Vollweiler, N., Spoetl, C. and Mangini, A.: COMNISPA II: Update of a mid-European isotope climate record, 11 ka to present, The Holocene, 23(5), 749–754, doi:10.1177/0959683612465446, 2012.

1 year record of weekly monitoring of rainfall d18O near the cave

The age model was computed in MATLAB® based on a cubic interpolation between the 230Th ages, its distance from the stalagmite top, and the corresponding dating errors. Multiple age models are produced to account for the analytical uncertainties and the errors in the location of each drill hole (assumed to be <0.2 mm). Therefore, multiple iterations of the age model were calculated assuming a normally distributed deviation from the 230Th age and the standard deviation given by the error range (Monte Carlo simulation). Iterations with reversals were dropped and an ensemble of 100 age models was created (i.e., all reversals could be removed within the error margins). In this model the median age in the distribution was used for each point.

Rainfall amount and d18O of rainfall depend on the position of the ITCZ and frequency of ENSO

Kennett, D. J., Breitenbach, S. F. M., Aquino, V. V., Asmerom, Y., Awe, J., Baldini, J. U. L., Bartlein, P., Culleton, B. J., Ebert, C., Jazwa, C., Macri, M. J., Marwan, N., Polyak, V., Prufer, K. M., Ridley, H. E., Sodemann, H., Winterhalder, B. and Haug, G. H.: Development and Disintegration of Maya Political Systems in Response to Climate Change, Science, 338(6108), 788–791, doi:10.1126/science.1226299, 2012.

(1) The most recent stalagmite ?18O values are anticorrelated with Basin of Mexico precipitation, showing our record to be a robust proxy for rainfall amount. (2) Smothed ?18O data and Tacubaya wet season (May through November, MJJASON, comprising 95% of the annual total) rainfall (1880?2010 CE) is strongly anticorrelated. (3) Observational studies of tropical rainfall

9 yr smoothed rainfall and ?18O data (1878?1988 CE) are correlated at r=-0.89, suggesting a a ca. 9yr transit time (the chronology was adjusted accordingly)

Lachniet, M. S., Bernal, J. P., Asmerom, Y., Polyak, V. and Piperno, D.: A 2400 yr Mesoamerican rainfall reconstruction links climate and cultural change, Geology, 40(3), 259–262, doi:10.1130/g32471.1, 2012.

Given that the precipitation regime in the study area is quite similar to the one at Brasilia station it is rea- sonable to assume that most of the isotopic fractionation is primarily related to total rainfall amount, which is charac- terized by more negative values during the wet season and more positive ones during the dry season.

Novello, V. F., Cruz, F. W., Karmann, I., Burns, S. J., Strikis, N. M., Vuille, M., Cheng, H., Lawrence Edwards, R., Santos, R. V., Frigo, E. and Barreto, E. A. S.: Multidecadal climate variability in Brazil’s Nordeste during the last 3000 years based on speleothem isotope records, Geophysical Research Letters, 39(23), n/a–n/a, doi:10.1029/2012gl053936, 2012.

The major features (growht banding thickness) are replicated in other speleothems from the same cave and other caves in the region

Because Bat Cave relative humidity today varies between 70% and 95%, dry conditions are interpreted, in part, to reflect greater kinetic fractionation, resulting in higher ?13C and ?18O values in the stalagmite calcite. The stalagmite was sampled close to the entrance

Both isotopes and the thickness of the laminae decrease during periods of drought

Monsoon strenght and correlated drought periods over the past millennium

?13C and ?18O values were measured at an average interval of 10 y. The annual band thickness data were smoothed and sampled at 10-y interval evenly (the average resolution of the isotopic data) for statistical analysis

U-Th age model, lamina counting and good correlation with local tree ring chronology

Evidence of primary features such as aragonite layers, well-preserved delicate fossils, and growth banding, indicating a lack of diagenetic alteration.

Banding thickness measured in an other coheval stalagmite from the same and another nearby cave

LCB (29/03/2019): No isotopic analyses => shouldn't it be removed?

Resolving the climate history for the southwestern United States using stalagmite proxies: to explain evidence of dwelling abandonment and population redistribution.

Because Bat Cave relative humidity today varies between 70% and 95%, dry conditions are interpreted, in part, to reflect greater kinetic fractionation, resulting in higher δ13C and δ18O values in the stalagmite calcite. Another influence on stalagmite δ18O values are variations in moisture sources, with lower δD and δ18O values derived from Pacific-dominated moisture and higher values from Gulf of Mexico and Gulf of California-dominated moisture. Southwestern North America receives both winter (dominantlyPacific) and summer (dominantly North American monsoon) precipitation.

Asmerom, Y., Polyak, V. J., Rasmussen, J. B. T., Burns, S. J. and Lachniet, M.: Multidecadal to multicentury scale collapses of Northern Hemisphere monsoons over the past millennium, Proceedings of the National Academy of Sciences, 110(24), 9651–9656, doi:10.1073/pnas.1214870110, 2013.

Australian National University on a Finnigan MAT-251 mass spectrometer equipped with an automated Kiel carbonate reaction device.

Poor correlation among d13C and d18O and good overlapping of several stalagmites

LCB (29/03/2019): only tab 1 and 2 in lipdverse cover the last 2k. Cannot pick one over the other but the others should all be FALSE

Analysis of modern rainfall d18O at Liang Luar shows that summer monsoon rainwater is depleted in 18O by 6?7% compared with rain water for the remainder of the year.This large isotopic contrast means that changes in the amount of summer rainfall, or the fraction of the year dominated by the northwest monsoon, produce a significant shift in the d18O of Flores rainfall. Today, the position of the ITCZ governs the balance between summer monsoon rain and winter trade wind induced orographic rainfall, and hence d18O at Flores. Water isotope-enabled climate models show that similar relationships between ITCZ positioning and rainfall d18O also prevailed at Flores during the last glacial. Millennial-scale changes in warm pool temperatures (and surface air temperature) were small over the last 23 kyr, thus changes in the d18O of rainfall, rather than temperature, dominate the record

MF (31/12/19), LCB (29/03/2019): only tab 1 and 2 in lipdverse cover the last 2k. Cannot pick one over the other but the others should all be FALSE,

MF (31/12/19), LCB (29/03/2019): only tab 1 and 2 in lipdverse cover the last 2k. Cannot pick one over the other but the others should all be FALSE

Ayliffe, L. K., Gagan, M. K., Zhao, J., Drysdale, R. N., Hellstrom, J. C., Hantoro, W. S., Griffiths, M. L., Scott-Gagan, H., Pierre, E. S., Cowley, J. A. and Suwargadi, B. W.: Rapid interhemispheric climate links via the Australasian monsoon during the last deglaciation, Nature Communications, 4(1), doi:10.1038/ncomms3908, 2013.

An online automated carbonate preparation system linked to a VG Prism II isotope ratio mass spectrometer at the University of Southern California and an online automated carbonate preparation system linked to a Finnigan Delta Plus Advantage at the University of Sao Paulo

Moreover, the d18O of precipitation has been shown to be inversely correlated with the amount of rainfall, a relationship dubbed as the amount effect, with a slope between 0.4 and 0.8% per 100 mm increase in the mean annual precipitation

Cheng, H., Sinha, A., Cruz, F. W., Wang, X., Edwards, R. L., d’ Horta, F. M., Ribas, C. C., Vuille, M., Stott, L. D. and Auler, A. S.: Climate change patterns in Amazonia and biodiversity, Nature Communications, 4(1), doi:10.1038/ncomms2415, 2013.

TP: added site elevation, LCB(29/03/2019): one of the two is at higher resolution and should therefore be the primary

Thus, the isotopic composition of rainfall in the Andes integrates the effects of rainout of the heavy isotope along the moisture transport pathway.

Kanner, L. C., Burns, S. J., Cheng, H., Edwards, R. L. and Vuille, M.: High-resolution variability of the South American summer monsoon over the last seven millennia: insights from a speleothem record from the central Peruvian Andes, Quaternary Science Reviews, 75, 1–10, doi:10.1016/j.quascirev.2013.05.008, 2013.

d18O analyses conducted at the Las Vegas Isotope Science Laboratory at the University of Nevada, Las Vegas (LVIS: samples JX-2, -6, and -10) were performed with a Kiel IV automated carbonate preparation device  d18O and d13C analyses conducted at Universidad Aut�noma de Mexico (CBD-2) (?) ?18O values were corrected with an internal standard (USC-1) whose value was determined by comparison with the international standards NBS-18 and NBS-19.

The stalagmite ?18O values for the Mexican samples replicate very well over the common time intervals (Fig. S2), suggesting the values have not been significantly affected by kinetic effects, a conclusion that is further supported by an observation of apparent equilibrium isotopic relationships between drip-water samples and modern aragonite precipitating in the cave.

The study area receives moisture from Caribbean easterly waves guided by the trade winds, tropical cyclones from the eastern Pacific and Gulf of Mexico, and Caribbean moisture that traverses the isthmus of Tehuantepec to reach southwestern Mexico via recurved trade winds over the eastern tropical Pacific. The NAM extends from southern Mexico into the southwestern United States, and is an important contributor to annual rainfall  totals due to abundant summertime convection. Our study area is dominated by a summer moisture source (supplying ?97% of annual rainfall) from the surrounding tropical oceans.

The stalagmite ?18O values also contain a temperature imprint: a decrease in LST of ?3?4 i¿½C is responsible for making the stalagmite ?18O values higher by ?0.6?0.8% due to the water?carbonate precipitation temperature

A 0.5-or 1.0-mm sampling interval corresponds to a temporal resolution of ?2 y for the last 2 ka, 10?12 y for the LGM, HS1, and YD, and ?60 y for the Holocene.

Lachniet, M. S., Asmerom, Y., Burns, S. J., Patterson, W. P., Polyak, V. J. and Seltzer, G. O.: Tropical response to the 8200 yr B.P. cold event? Speleothem isotopes indicate a weakened early Holocene monsoon in Costa Rica, Geology, 32(11), 957, doi:10.1130/g20797.1, 2004.

Thermofinnigan Delta V Plus Isotope Ratio Mass Spectrometer coupled with a Kiel IV carbonate device

The standard deviation of repeated NBS19 measurements is ~0.06 parts per mille for d18O.

Temp and humidity measured from 2007 till 2013 show constant temp of 8 +/- 0.5 C and humidity close to 100%. Average d18O of 8 drip water samples collected between June, 2007 till July, 2008 is -9.74 +/- 0.48 parts per mille. Glass plate calcite collected over the same period shoed a d18O value of -8.15 parts per mille. So calculated equilibrium temp is 7.6 C which is close to measure cave temp of 7.87 C. Fractionation equation used has not been specified. Supplementary Information.

1. Baker, Andy, and Chris Bradley. "Modern stalagmite ? 18 O: Instrumental calibration and forward modelling." Global and Planetary Change 71.3 (2010): 201-206. 2. Oster, Jessica L., Isabel P. Monta�ez, and Neil P. Kelley. "Response of a modern cave system to large seasonal precipitation variability." Geochimica et Cosmochimica Acta 91 (2012): 92-108. 3. Tooth, Anna F., and Ian J. Fairchild. "Soil and karst aquifer hydrological controls on the geochemical evolution of speleothem-forming drip waters, Crag Cave, southwest Ireland." Journal of Hydrology 273.1 (2003): 51-68. Supplementary information.

Isotopic composition of precipitation in Southern California is largely determined by the storm track delivering precipitation to the region (Friedman, Irving, et al. "Stable isotope composition of waters in southeastern California 1. Modern precipitation." Journal of Geophysical Research: Atmospheres 97.D5 (1992): 5795-5812.). Analysis shows three primary clusters of storms entering the region with the lowest d18O precipitation arriving from North Pacific and highest from tropical Pacific. The trajectory of storms arriving in Southwest North America is strongly dependant on Pacific SST patterns (Ren, Xuejuan, Yaocun Zhang, and Yang Xiang. "Connections between wintertime jet stream variability, oceanic surface heating, and transient eddy activity in the North Pacific." Journal of Geophysical Research: Atmospheres 113.D21 (2008).), which influence the position of high and low pressure centres in the North Pacific and over the North American continent.

McCabe-Glynn, S., Johnson, K. R., Strong, C., Berkelhammer, M., Sinha, A., Cheng, H. and Edwards, R. L.: Variable North Pacific influence on drought in southwestern North America since AD 854, Nature Geoscience, 6(8), 617–621, doi:10.1038/ngeo1862, 2013.

Thermo-Finnigan MAT253 Isotope Ratio Mass Spectrometer (IRMS) or a Thermo-Finnigan Delta V Plus IRMS, with a Kiel IV Carbonate Device both at the Analytical Laboratory for Paleoclimate Studies (ALPS) at the Jackson School of Geosciences, University of Texas at Austin

repeat measurements of a carbonate standard has a long-term analytical precision of 0.12?, 2?

Samples pass the Hendy Test. Low correlation between d18O and d13C across a layer. Also d18O replicates between stalagmites, but d13C doesnt. Top of stalagmite is similar to predicted value using dripwater d18O and cave temp

AX: check if age model exists. Note: Speleo age model? It should, as it has ages!

Regression between rainfall amount and stalagmite d18O. "We choose to use 10- year decadal means to compare mean stalagmite ?18O and rainfall amount between wet and dry periods (i.e. different PDV phases) (Figure S8). Dating errors preclude us from using a regression between stalagmite ?18O and rainfall amount yearly data during the instrumental era. The slope of the regression yields a conversion of 1? stalagmite ?18O per 1.4 m/wet season (R2 = 0.74); an inverse correlation known as the ?Amount Effect? (Dansgaard, 1964; Rozanski et al., 1993)."

Partin, J. W., Quinn, T. M., Shen, C.-C., Emile-Geay, J., Taylor, F. W., Maupin, C. R., Lin, K., Jackson, C. S., Banner, J. L., Sinclair, D. J. and Huh, C.-A.: Multidecadal rainfall variability in South Pacific Convergence Zone as revealed by stalagmite geochemistry, Geology, 41(11), 1143–1146, doi:10.1130/g34718.1, 2013.

Three different labs and instruments: (1) Finnegan MAT 252 isotope ratio mass spectrometer equipped with a Kiel carbonate device; (2) Finnegan Delta E gas source ratio mass spectrometer; (3) GasBench-IRMS system

more positive values of d18O are interpreted to reflect less rainfall throughout the "amount effect" and the fact that during dry years, the water in the soil (due to evapotranspiration) has more positive d18O values. More positive d13C indicates decreased biological activity in the overlying soil during drier conditions

both d18O and d13C are recording changes between wetter and drier conditions in the external environment, with more soil activity during wet years

Sletten, H. R., Railsback, L. B., Liang, F., Brook, G. A., Marais, E., Hardt, B. F., Cheng, H. and Edwards, R. L.: A petrographic and geochemical record of climate change over the last 4600years from a northern Namibia stalagmite, with evidence of abruptly wetter climate at the beginning of southern Africa’s Iron Age, Palaeogeography, Palaeoclimatology, Palaeoecology, 376, 149–162, doi:10.1016/j.palaeo.2013.02.030, 2013.

An online, automated carbonate preparation system linked to a triple collector gas source mass spectrometer at the University of Innsbruck

equilibrium is evidenced by the lack of correlation among d18O and d13C

TP: added site elevation; TP (30/12/19): In fact, the age information is not missing, but the depth and age columns in the dataset were mislabelled (age column was labelled 'depth', and depth column was labelled 'age'). LCB: Missing age/year. See plot. ZK (14/01/2019) the time span should be 1635 - 1995 AD; BM (14/03/2019) info sent using GitHub

this interpretation is based on the correlation with instrumental temperatures (last 100 years) and in the good correlation with other nearby temperature record (SST inferred from Ifaty-4 coral d18O)

more positive values of d18O are found with greater annual temperatures (specially when averaging previous 5 years)

Mean annual air temperatures influence the annual precipitation isotope composition.

Sundqvist, H. S., Holmgren, K., Fohlmeister, J., Zhang, Q., Matthews, M. B., Spoetl, C. and Koernich, H.: Evidence of a large cooling between 1690 and 1740 AD in southern Africa, Scientific Reports, 3(1), doi:10.1038/srep01767, 2013.

TP: added site elevation; ZK 07/01/2019: The problem is that decimal separators have been lost from the isotope values.

Finnigan Delta Plus Advantage and a Kiel IV carbonate device coupled to a Finnigan MAT 253 MS both at the University of Brasilia

Still, the amount effect does not explain the total variance in the iso- topic composition of precipitation (R2 = 0.3, p < 0.01)

Intensity of the South American Summer Monsoon (SASM) excerts the strongest control on precipitation isotopes

TP: added site elevation; ZK 07/01/2019: The first problem is that decimal separators have been lost from the isotope values. The second problem is that SP14APPE00A and SP14APPE02A duplicates the same record. One of them should be removed.

Apaestegui, J., Cruz, F. W., Sifeddine, A., Vuille, M., Espinoza, J. C., Guyot, J. L., Khodri, M., Strikis, N., Santos, R. V., Cheng, H., Edwards, L., Carvalho, E. and Santini, W.: Hydroclimate variability of the northwestern Amazon Basin near the Andean foothills of Peru related to the South American Monsoon System during the last 1600 years, Climate of the Past, 10(6), 1967–1981, doi:10.5194/cp-10-1967-2014, 2014.

LCB: Missing age/year. See plot; BM (14/03/2019) info sent using GitHub; TP: broken DOI; Time-scale missing; elevation estimated from Google Earth

The amount of rainfall can be viewed as an indicator of the monsoon strength since the active period of the summer monsoon closely coincides with the rainy season in China. d18O in the speleothem reflects the amount of rainfall at short time scales (less than 10 years) but temperature trends (at larger time scales)

Ku, T. L., and Li, H. C.: Speleothems as high-resolution paleoenvironment archives: Records from northeastern China, Proceedings of the Indian Academy of Sciences - Earth and Planetary Sciences, 107, 321-330, 10.1007/BF02841598, 1998.

LCB(29/03/2019): one record covers the entire last 2k. should be the primary; TP: broken DOI; site elevation estimated from Google Earth

present day CO2 partial pressure is constant year-round and active steam flow in the cave maintains 100% humidity

Changes in the vegetation related to changes in rainfall amount lead to variation of d13C

Cool weather precipiation is depleted in d18O compared to warm weather precipitation.

Denniston, R. F., Gonzalez, L. A., Asmerom, Y., Baker, R. G., Reagan, M. K. and Bettis, E. A.: Evidence for increased cool season moisture during the middle Holocene, Geology, 27(9), 815, doi:10.1130/0091-7613(1999)027<0815:eficsm>2.3.co;2, 1999.

; climateInterpretation_seasonality changed - was originally -12 -11 -10 -9 -8 1 2 3 4 5 6 7; archiveType changed - was originally Sclerosponge (SS)

For U-Th analysis, 0.3 to 1g of sponge material was drilled along visible growth layers. The sample size was chosen so that the width and depth of the sampling groove was equivalent to a period of about 20 years, given a growth rate on the order of 0.2 mm/a. 11 samples were anayzed for U-Th. The external reproducibility of the U/Th dating results was determined as about i¿½20 years (2sem) by five replicate analyses of sample Ce96-40 and confirmed by analysis of three closely spaced sample pairs (Ce96-45/51, Ce96-170/172, Ce96-123/40). For one sample pair (Ce96-184/186) U/Th ages could not be confirmed within external reproducibility. As the age data of this specimen deviate significantly from a linear growth curve, we fitted a third order polynomial to the U/Th ages.

The observation that sponges precipitate aragonite in chemical and isotopic equilibrium indicates that the composition of the precipitating fluid is hardly influenced by the sponge metabolism. Thus pH changes in the ambient seawater may be directly monitored by the d18O record of the sponge aragonite. This hypothesis is supported by the boron isotopic composition of sponge skeletons, which indicates mineralization under seawater pH conditions [Bohm et al., 2000b].

Archive team- in inferred material, need to differentiate between surface and subsurface water.

We conclude that, together with variations in seawater d18O, the pH effect on d18O of carbonates can obscure the temperature signal in the sponge d18O record sufficiently to explain the divergent trends of the Sr/Ca and the oxygen isotope records. These results indicate that for temperature reconstructions using C. nicholsoni skeletons, Sr/Ca is a more robust proxy than d18O.

The d18Owater salinity relation in the Caribbean is on the order of 0.2 to 0.3%/psu [Ruhlemann et al., 1999; Watanabe et al., 2001]. Oxygen isotope records of these sponges do notreveal reproducible temperature signals. Variations in thed18O of the ambient water and the pH effect on the oxygenisotopic composition of carbonates [Zeebe, 1999] mayobscure temperature signals in thed18O records.

The observation that sponges precipitate aragonite in chemical and isotopic equilibrium indicates that the composition of the precipitating fluid is hardly influenced by the sponge metabolism. Thus pH changes in the ambient seawater may be directly monitored by the d18O record of the sponge aragonite. This hypothesis is supported by the boron isotopic composition of sponge skeletons, which indicates mineralization under seawater pH conditions [Bo�hm et al., 2000b].

For U-Th analysis, 0.3 to 1g of sponge material was drilled along visible growth layers. The sample size was chosen so that the width and depth of the sampling groove was equivalent to a period of about 20 years, given a growth rate on the order of 0.2 mm/a. 11 samples were anayzed for U-Th. The external reproducibility of the U/Th dating results was determined as about �20 years (2sem) by five replicate analyses of sample Ce96-40 and confirmed by analysis of three closely spaced sample pairs (Ce96-45/51, Ce96-170/172, Ce96-123/40). For one sample pair (Ce96-184/186) U/Th ages could not be confirmed within external reproducibility. As the age data of this specimen deviate significantly from a linear growth curve, we fitted a third order polynomial to the U/Th ages.

Temperature equation of Bohm et al. [2000]. Oxygen isotope records of these sponges do notreveal reproducible temperature signals. Variations in thed18O of the ambient water and the pH effect on the oxygenisotopic composition of carbonates [Zeebe, 1999] mayobscure temperature signals in thed18O records.

combines new sclerosponge data with Grossman and Ku, 1986 (10.1016/0168-9622(86)90057-6)

Three transects were sampled as a test for reproducibility (Figures 5 and 10b). Correlation between the transects was carried out by following the growth bands of the skeleton. The trends and larger features are well-reproduced in the three transects. However, transect 1 is offset from the other two transects by about 0.1%.

For U-Th analysis, 0.3 to 1g of sponge material was drilled along visible growth layers. The sample size was chosen so that the width and depth of the sampling groove was equivalent to a period of about 20 years, given a growth rate on the order of 0.2 mm/a. 4 samples were anayzed for U-Th. 10 samples for radiocarbon analysis were removed. They compared D14C data with a D14C curve measured on a Florida surface water coral [Druffel, 1989]. The fit was constrained by assuming that the growth rate was constant in the relevant part of the sponge skeleton. They further assume that the timing of the radiocarbon increase at 125 mbsl was similar to surface waters in that region because the amplitude of change in D14C is similar to the surface water change. For specimen Pb19 a mean growth rate of 0.19 mm/a was calculated from the slope of a linear fit to the dated tie points. A lifespan from about 1400 A.D. to 1996 A.D. was determined by extrapolating the mean growth rate to the base of the skeleton. The U/Th chronology is independently confirmed by the correct localization of the nuclear weapon test radiocarbon increase at a depth of about 5.9 mm below the surface of the skeleton (Figure 6, Table 2). Further independent support for the reliability of our chronologies is provided from the fit of d13C data of the investigated sponge skeletons and atmospheric CO2 records [Boi¿½hm et al., 2002].

The observation that sponges precipitate aragonite in chemical and  isotopic equilibrium indicates that the composition of the precipitating  fluid is hardly influenced by the sponge metabolism. Thus pH changes in the ambient seawater may be directly monitored by the d18O record of the sponge aragonite. This hypothesis is supported by the boron isotopic composition of sponge skeletons, which indicates mineralization under seawater pH conditions [Bohm et al., 2000b].

The observation that sponges precipitate aragonite in chemical and  isotopic equilibrium indicates that the composition of the precipitating  fluid is hardly influenced by the sponge metabolism. Thus pH changes in the ambient seawater may be directly monitored by the d18O record of the sponge aragonite. This hypothesis is supported by the boron isotopic composition of sponge skeletons, which indicates mineralization under seawater pH conditions [Bo�hm et al., 2000b].

For U-Th analysis, 0.3 to 1g of sponge material was drilled along visible growth layers. The sample size was chosen so that the width and depth of the sampling groove was equivalent to a period of about 20 years, given a growth rate on the order of 0.2 mm/a. 4 samples were anayzed for U-Th. 10 samples for radiocarbon analysis were removed. They compared D14C data with a D14C curve measured on a Florida surface water coral [Druffel, 1989]. The fit was constrained by assuming that the growth rate was constant in the relevant part of the sponge skeleton. They further assume that the timing of the radiocarbon increase at 125 mbsl was similar to surface waters in that region because the amplitude of change in D14C is similar to the surface water change. For specimen Pb19 a mean growth rate of 0.19 mm/a was calculated from the slope of a linear fit to the dated tie points. A lifespan from about 1400 A.D. to 1996 A.D. was determined by extrapolating the mean growth rate to the base of the skeleton. The U/Th chronology is independently confirmed by the correct localization of the nuclear weapon test radiocarbon increase at a depth of about 5.9 mm below the surface of the skeleton (Figure 6, Table 2). Further independent support for the reliability of our chronologies is provided from the fit of d13C data of the investigated sponge skeletons and atmospheric CO2 records [Bo�hm et al., 2002].

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally -12 -11 -10 -9 -8 1 2 3 4 5 6 7; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Sclerosponge (SS)

lower limit of 95% ci of difference in Sr/Ca between -20 and -125m, divided by difference in observed T at those depths.

Haase-Schramm 2005, they sample the time interval from 1620 to 1745 A.D. with almost monthly resolution. Bohm 2002 also looks at this sponge but reports d13C.

Haase-Schramm, Alexandra , Bohm, Florian , Eisenhauer, Anton , Dullo, Wolf-Christian , Joachimski, Michael M. , Hansen, Bent , Reitner, Joachim

Haase-Schramm, A., Boehm, F., Eisenhauer, A., Dullo, W.-C., Joachimski, M. M., Hansen, B. and Reitner, J.: Sr/Ca ratios and oxygen isotopes from sclerosponges: Temperature history of the Caribbean mixed layer and thermocline during the Little Ice Age, Paleoceanography, 18(3), n/a–n/a, doi:10.1029/2002pa000830, 2003.

Sr/Ca ratios and oxygen isotopes from sclerosponges: Temperature history of the Caribbean mixed layer and thermocline during the Little Ice Age

JLC: The site name is Exuma Sound, which is different than TOTO (Tongue of the Ocean), based on map in Rosenheim paper (but labeled this way in NOAA Paleo). The lat and lon provided for site on NOAA paleo are different than what is here, and match paper more accurately. correct Lat: 23.67N correct Lon: 75.75W;    (additional notes) This record appears in th same paper as the Tongue of the Ocean sclerosponge record of Swart et al., 2002 and Rosenheim, 2005. The Sr/Ca data and calibration of that data appears in Rosenheim et al., 2004. The data from Swart 2002 had the chronology adjusted by Rosenheim 2005, do not Swart 2002 data in final version.

Kiel III automated carbonate device attached to a Delta Plus isotope ratio mass spectrometer (IRMS)

; climateInterpretation_seasonality changed - was originally annual; archiveType changed - was originally Sclerosponge (SS)

sclerosponges were dated using U/Th radiometric techniques and then analyzed using high resolution micromilling for oxygen isotope analysis via isotope ratio mass spectrometry and laser ablation sampling for Sr/Ca analysis via ICP-MS. Constant-growth age models constructed from U/Th dating indicate growth rates of 145 mmy1 for the Exuma sclerosponge and 172 mmy1 for the TOTO sclerosponge (auxiliary material1). The radiometric age model of the TOTO sclerosponge was tuned to annual Sr/ Ca variations after Swart et al. [2002], however because tuned age models and constant growth models are within 5% [Swart et al., 2002], the U/Th constant growth model was used for the Exuma sclerosponge.

mode of skeleton formation of Ceratoporella nicholsoni suggest that these sponges precipitate aragonite close to isotopic equilibrium (bohm, 2000).

we find secular salinity increases of 0.35 A± 0.34 psu in Exuma Sound and 0.5 A± 0.35 psu in TOTO that must happen coevally with the secular temperature increases to explain the discrepancies between Sr/Ca and d18Oaragonite linear temperature trends. It is evident from (4) that our reconstruction is sensitive to the gradient d18Osw/S (0.54 %psu1). Despite the significant cumulative residual error from equations (1)a€“(3) (auxiliary material), our data clearly identify salinity variation in the subsurface waters of both Exuma Sound and TOTO during the last 100 years.

Oxygen isotope values (d18O) are measured in %VPDB for aragonite and % SMOW for water. Ratios of Sr/Ca are measured in mmolmol1, temperature (T) is in C, and salinity (S) is in psu. Equation (3) is constructed from surface waters (<50 m) of the return flow of the N. Atlantic Gyre between 45N and 31N. During transport between these latitudes, this water mass begins adopting the properties of the SMW [Krauss, 1986; Ottens, 1991]. By combining and rearranging these equations to reconstruct the salinity record preserved in Bahamas sclerosponges,

; paleoData_variableName changed - was originally Sr_Ca; climateInterpretation_seasonality changed - was originally annual; paleoData_variableName changed - was originally Sr_Ca; archiveType changed - was originally Sclerosponge (SS)

unitless ratio, two standard deviations of the mean 230Th/234U activity ratio

unitless ratio, two standard deviations of the mean 234U/238U activity ratio

Rosenheim, B. E.: Salinity change in the subtropical Atlantic: Secular increase and teleconnections to the North Atlantic Oscillation, Geophysical Research Letters, 32(2), doi:10.1029/2004gl021499, 2005.

Salinity change in the subtropical Atlantic: Secular increase and teleconnections to the North Atlantic Oscillation

JLC: The Sr/Ca data are missing for this record, added to github;   (additional notes) This record appears in th same paper as the Tongue of the Ocean sclerosponge record of Swart et al., 2002 and Rosenheim, 2005. The Sr/Ca data and calibration of that data appears in Rosenheim, et al., 2004. The data from Swart 2002 had the chronology adjusted by Rosenheim 2005, do not Swart 2002 data in final

Automated common acid bath attached to a Finnigan-MAT 251 at the University of Miami. Data have been corrected for drift of the standard during the analysis and the usual isobaric interferences

High-resolution Sr/Ca records in sclerosponges calibrated to temperature in situ

Rosenheim, B. E., Swart, P. K., Thorrold, S. R., Willenz, P., Berry, L. and Latkoczy, C.: High-resolution Sr/Ca records in sclerosponges calibrated to temperature in situ, Geology, 32(2), 145, doi:10.1130/g20117.1, 2004.

Intra-annual variation in the stable oxygen and carbon and trace element composition of sclerosponges

Needs isotopeInterpretation1_direction (GF), chronology uncertainty type is missing

OCh-S: added; SM: Isotope interpretation direction shoule be positive

The range of the observed 18O cyclicity, 3a€“5a€°, is approximately equal to the annual range of observed rainfall d18O values (IAEA/WMO, 2003) for stations from Honduras, Costa Rica and Panama.

Sub-annual cyclic isotopic signatures of several permil represent the annual cycle of local rainfall and relative humidity. Additional data from a plantation tree of known age from ENSO-sensitive northwestern coastal Peru suggests that the 1997–8 ENSO warm phase event was recorded as an 8‰ anomaly in the δ18O of α-cellulose.

Evans, M. N. and Schrag, D. P.: A stable isotope-based approach to tropical dendroclimatology, Geochimica et Cosmochimica Acta, 68(16), 3295–3305, doi:10.1016/j.gca.2004.01.006, 2004.

The negative relationship between precipitation totoals and tree-ring d18O is strengthened through complex effects of varying humidity on plant physiology. Simplified, moist atmospheric conditions will reduce transpiration and therefore reduce 18O water enrichment in needles.

Winter precipitation at this high altitude (2900m and > 3700m) sites fall as snow (contribute >80% to annual total).

Treydte, K. S., Schleser, G. H., Helle, G., Frank, D. C., Winiger, M., Haug, G. H. and Esper, J.: The twentieth century was the wettest period in northern Pakistan over the past millennium, Nature, 440(7088), 1179–1182, doi:10.1038/nature04743, 2006.

Please check isotopeInterpretation1 fields (requires isotopeInterpretation1_name, isotopeInterpretation1_direction should be positive or negative) (GF)

Correlations with 18O of precipitation (GNIP data) showed that source water signals are preserved in d18O tree rings. A possible explanation for the common decadal-to century scale trends, not directly related to mean monthly air temperature or precipitation amount, is variations in moisture source determined by the dominant atmospheric circulation pattern. The NAO index, determinates diminant wind pattern and temperature, and precipitation systems over Europe and influences d18O precipitation in Switzerland.

Reynolds-Henne, C. E., Siegwolf, R. T. W., Treydte, K. S., Esper, J., Henne, S. and Saurer, M.: Temporal stability of climate-isotope relationships in tree rings of oak and pine (Ticino, Switzerland), Global Biogeochemical Cycles, 21(4), n/a–n/a, doi:10.1029/2007gb002945, 2007.

TP (03/01/20): corrected the broken DOI (was missing a few dashes)

After evaluating the relationship between d18O and observed temperature and precipitation it can be concluded that there is some correlation of oxygen isotope values with late winter to early summer temperatures and a clear negative correlation with winter precipitation (November-February).

The meteorological stations of Khoseda Khard, Varandei,Khorei-Ver and Vorkuta.

Holzkaemper, S., Kuhry, P., Kultti, S., Gunnarson, B. and Sonninen, E.: Stable Isotopes in Tree Rings as Proxies for Winter Precipitation Changes in the Russian Arctic over the Past 150 Years, Geochronometria, 32(-1), 37–46, doi:10.2478/v10003-008-0025-6, 2008.

Needs isotopeInterpretation1_name & isotopeInterpretation1_direction (GF)

Early-millennium climate was marked by relatively warm winters and high growth season relative humidity, especially ~AD 1100a€“1250, followed by the onset of cooler and drier conditions in the early 1500s. Winter temperatures apparently attained 20th century levels by about AD 1800, while relatively low growth season humidity persisted until
about AD 1900.

precipitation d18O is positively correlated with temperature, and tree source water and tree-ring cellulose record precip d18O

Edwards, T. W. D., Birks, S. J., Luckman, B. H. and MacDonald, G. M.: Climatic and hydrologic variability during the past millennium in the eastern Rocky Mountains and northern Great Plains of western Canada, Quaternary Research, 70(2), 188–197, doi:10.1016/j.yqres.2008.04.013, 2008.

Tartakovsky, V. A., Voronin, V. I. and Markelova, A. N.: External forcing factor reflected in the common signals of δ18O-tree-ring series of Larix sibirica Ledeb. in the Lake Baikal region, Dendrochronologia, 30(3), 199–208, doi:10.1016/j.dendro.2011.08.004, 2012.

ThermoFinnigan Delta XP continuous flow isotope ratio mass spectrometer

The I´18O of cellulose in cloud forest trees reflects the seasonal change in the I´18O of source water as determined by the amount of rainfall and the 18O-enrichment of cloud water.

Source water d18O is determined by P_isotopes, and secondary temperature and ET effects.

During boreal summer (May to October), cloud forests receive most of their rainfall as the northward movement of the Intertropical Convergence Zone (ITCZ) brings convective storms to the region. During the dry season (approximately January through April), moisture advection and cloud water deposition are an important component of cloud forest hydrology (4), particularly on the leeward Pacific slope that would otherwise experience the effects of a pronounced dry season.

Anchukaitis, K. J. and Evans, M. N.: Tropical cloud forest climate variability and the demise of the Monteverde golden toad, Proceedings of the National Academy of Sciences, 107(11), 5036–5040, doi:10.1073/pnas.0908572107, 2010.

; archiveType changed - was originally Tree ring cellulose (TR); archiveType changed - was originally Tree ring cellulose

TP (31/12/19): climate interpretation (P-negative) was removed from isotopeInterpretation2; OCh-S: added

A multi-proxy record spanning 180 years from Cedrela spp. showed a significant negative relationship between d18O in tree-ring cellulose and January precipitation.

Source water d18O is determined by P_isotopes, which is strongly influenced by precipitation amount (negative relation).

TP (31/12/19): climate interpretation (P-negative) was removed from isotopeInterpretation2

A multi-proxy record spanning 180 years from Cedrela spp. showed a significant negative relationship between cellulose d18O and January precipitation.

Ballantyne, A. P., Baker, P. A., Chambers, J. Q., Villalba, R. and Argollo, J.: Regional Differences in South American Monsoon Precipitation Inferred from the Growth and Isotopic Composition of Tropical Trees, Earth Interactions, 15(5), 1–35, doi:10.1175/2010ei277.1, 2011.

A 150-year record obtained from Polylepis spp. showed a significant negative relationship between d18O and March precipitation

Source water d18O is determined by P_isotopes, which is strongly influenced by precipitation amount.

A 150-year record obtained from Polylepis spp. also showed a significant negative relationship between d18O and March precipitation

A composite d18O time-series representing pooled tree-ring samples (4-6 trees) of Tibetan juniper (Juniperus tibetica)

Late Holocene Asian summer monsoon variability reflected by δ18O in tree-rings from Tibetan junipers

GrieSSinger, J., Braeuning, A., Helle, G., Thomas, A. and Schleser, G.: Late Holocene Asian summer monsoon variability reflected byδ18O in tree-rings from Tibetan junipers, Geophysical Research Letters, 38(3), n/a–n/a, doi:10.1029/2010gl045988, 2011.

; archiveType changed - was originally Tree ring cellulose (TR); archiveType changed - was originally Tree ring cellulose (TR)

TP (31/12/19): climate interpretation (RH-negative) was removed from isotopeInterpretation2

When the total rainfall is more, ..., trees continue to grow until a period of lower relative humidity (65%) leading to higher teak 18O.

We propose that this correlation is caused by longer duration of the growing season in years of higher rainfall.

Managave, S. R., Sheshshayee, M. S., Ramesh, R., Borgaonkar, H. P., Shah, S. K. and Bhattacharyya, A.: Response of cellulose oxygen isotope values of teak trees in differing monsoon environments to monsoon rainfall, Dendrochronologia, 29(2), 89–97, doi:10.1016/j.dendro.2010.05.002, 2011.

(i) the presence of relatively stronger amount effect in rainfall over a longer time scale, (ii) higher contribution of rainfall during the north-east (NE) monsoon, depleted in 18O, and (iii) relatively lesser   effect of the relative humidity in deciding tree 18O.

by an isotope ratio mass spectrometer (ThermoQuest Delta Plus) interfaced with a pyrolysis-type elemental analyzer (ThermoQuest TC/EA).

Please check inferred material, should this be soil or leaf water? Check isotopeInterpretation1_name - can this be changed to one of the standardized nameds?

OCh-S:WEB3638db18 please replace to TR11SAHU00; OCh-S: Leaf water is correct

Instrumental calibration. A negative correlation between I´18O of precipitation and the amount of precipitation is observed in tropical regions including the Himalaya, which is termed as the a€˜amount effecta€™ (AraguA¡s-AraguA¡s et al., 1998; Dansgaard, 1964; Yadava and Ramesh, 2005).

Our interpretation of the temperature signal in the δ18O chronology is that higher temperatures stimulate evaporation of soil water, resulting in a preferential loss of lighter isotopes in soil water, which in turn is taken up by trees.

More specifically, lower atmospheric humidity causes higher vapor pressure gradient between leaf interstitial space and the atmosphere, resulting in a preferential loss of lighter isotopes and consequent enrichment in δ18O of leaf water.

Since all the responses of tree-ring δ18O to the climatic factors (precipitation, relative humidity, and temperature) are related to dry–wet conditions, the PDSI is considered to be the most useful single variable to explain the variance of our δ18O chronology.

d18O of the leaf water takes part in synthesis of photosynthates.

Increasing aridity over the past 223 years in the Nepal Himalaya inferred from a tree-ring δ18O chronology

Sano, M., Ramesh, R., Sheshshayee, M. and Sukumar, R.: Increasing aridity over the past 223 years in the Nepal Himalaya inferred from a tree-ring δ18O chronology, The Holocene, 22(7), 809–817, doi:10.1177/0959683611430338, 2011.

TP (31/12/19): climate interpretation (T_air-positive) was removed from isotopeInterpretation2

while δ18O in cellulose represents a mixed summer and winter temperature and precipitation signal.

Sidorova, O. V., Saurer, M., Myglan, V. S., Eichler, A., Schwikowski, M., Kirdyanov, A. V., Bryukhanova, M. V., Gerasimova, O. V., Kalugin, I. A., Daryin, A. V. and Siegwolf, R. T. W.: A multi-proxy approach for revealing recent climatic changes in the Russian Altai, Climate Dynamics, 38(1-2), 175–188, doi:10.1007/s00382-010-0989-6, 2011.

; archiveType changed  was originally Tree ring cellulose (TR); archiveType changed  was originally Tree ring cellulose

Changed isotopeInterpretation1_name from 'Palmer Drought Severity Index(combined effect o f temperature and precipitation amount)' to standardized equivalent P_E - check direction (GF)

TP (31/12/19): climate interpretations (P-negative, T_air-positive) were removed from isotopeInterpretation2 and 3; OCh-S: changed to P_E

In the monsoon season, high temperature usually indicates less rainfall and low relative humidity, which can make the tree-ring cellulose d18O heavier. Low PDSI indicates a dry condition.

In the monsoon season, high temperature usually indicates less rainfall and low relative humidity, which can make the tree ring cellulose d18O heavier. Low PDSI indicates a dry condition.

Please add isotopeInterpretation1_name and isotopeInterpretation1_direction (GF)

TP (31/12/19): climate interpretations (P-negative, T_air-positive) were removed from isotopeInterpretation2 and 3; OCh-S: added

OCh_S: Missing data are  desplayed in the graph 2 as continous line, while should be a gap (empty space)

all tree average, normalised d18O of tree cellulose (w.r.t., 1951-2002 average)

TP: this is a derived average of all other trees from the site, with d18O values normalised to zero.

Grid of 19.75 deg N, 103.25degE; 19.75 deg N, 103.75 deg E; 20.25 deg N, 103.25 deg E; and 20.25 deg N, 103.75 deg E

Xu, C., Sano, M. and Nakatsuka, T.: A 400-year record of hydroclimate variability and local ENSO history in northern Southeast Asia inferred from tree-ring δ18O, Palaeogeography, Palaeoclimatology, Palaeoecology, 386, 588–598, doi:10.1016/j.palaeo.2013.06.025, 2013.

Positive correlation between cellulose d18O and precipitation d18O; the later is positively influenced by air temperature.

Composite tree-ring d18O record representing the average of up to 8 Rocky Mountain Bristlecone Pine (Pinus aristata) trees in any given year of the composite record.

Secular temperature trends for the southern Rocky Mountains over the last five centuries

Berkelhammer, M. and Stott, L. D.: Secular temperature trends for the southern Rocky Mountains over the last five centuries, Geophysical Research Letters, 39(17), n/a–n/a, doi:10.1029/2012gl052447, 2012.

Positive correlation between cellulose d18O and precipitation d18O; precipitation amount influences d18O of precipitation

Oxygen isotopes in tree rings are a good proxy for Amazon precipitation and El Nino-Southern Oscillation variability

Brienen, R. J. W., Helle, G., Pons, T. L., Guyot, J.-L. and Gloor, M.: Oxygen isotopes in tree rings are a good proxy for Amazon precipitation and El Nino-Southern Oscillation variability, Proceedings of the National Academy of Sciences, 109(42), 16957–16962, doi:10.1073/pnas.1205977109, 2012.

Changed isotopeInterpretation1_name from 'Palmer Draought Severity Index(combined effect o f temperature and precipitation amount)' to standardized equivalent P_E - check direction (GF)

OCh-S: In 1 file has been presented 6 graphs, which were presented later on again. Either leave 1 file with 6 graphs, or present only 1 graph with own link. Label is desapeer 06, 01, 02, 03, 04, 05. Same graphs repeated 5 times with different links.

As recorded in the meteorological data from the monsoon season, higher temperatures usually correlate with lower precipitation, and relative humidity levels, both of which lead to enriched d18O in tree rings?..moreover, as climate parameters are significantly correlated with one another, it is difficult to identify a dominant factor...Although the mechanisms underlying variations in tree ring d18O can generally be attributed to d18O of source water and evaporative enrichment of leaf water d18O, in pluvial monsoon regions these effects seem to be well represented by the PDSI,

As recorded in the meteorological data from the monsoon season, higher temperatures usually correlate with lower precipitation, and relative humidity levels, both of which lead to enriched 18O in tree rings. Moreover, as climate parameters are significantly correlated with one another, it is difficult to identify a dominant factor. Although the mechanisms underlying variations in tree- ring d18O can generally be attributed to d18O of source water and evaporative enrichment of 18O leaf water, in pluvial monsoon regions these effects seem to be well represented by the PDSI.

Generally, lower precipitation levels correlate with higher d18O values of the precipitation (amount effect); at the same time, higher temperatures (usually associated with lower precipitation levels) also lead to d18O enrichment of soil water; acting together, these factors cause d18O enrichment of source water.

Sano, M., Xu, C. and Nakatsuka, T.: A 300-year Vietnam hydroclimate and ENSO variability record reconstructed from tree ringδ18O, Journal of Geophysical Research: Atmospheres, 117(D12), n/a–n/a, doi:10.1029/2012jd017749, 2012.

tree-ring cellulose d18O record representing 5 Mimosa acantholoba trees

Composite tree-ring d18O record representing up to 5 trees (Mimosa acantholoba) in any given year; mean inter-tree correlation = 0.83 (p < 0.01).

Oxygen isotopes in tree rings record variation in precipitation δ18O and amount effects in the south of Mexico

Brienen, R. J. W., Hietz, P., Wanek, W. and Gloor, M.: Oxygen isotopes in tree rings record variation in precipitationδ18O and amount effects in the south of Mexico, Journal of Geophysical Research: Biogeosciences, 118(4), 1604–1615, doi:10.1002/2013jg002304, 2013.

plant waters determined by fog and precipitaiton isotope composition, which is influenced by synoptic conditions. strong correlation with 500 mb pressure anomalies with middle-wood d18O

plant water isotope composition determined by fog (July, positive correlation) and precipitaiton (Aug-Sep, negative correlation).

Middle-wood and Late-wood d18O records from 3 Coast Redwood (Sequoia sempervirens) trees at the Arcata site, NW California.

Oxygen and carbon stable isotopes in coast redwood tree rings respond to spring and summer climate signals

Johnstone, J. A., Roden, J. S. and Dawson, T. E.: Oxygen and carbon stable isotopes in coast redwood tree rings respond to spring and summer climate signals, Journal of Geophysical Research: Biogeosciences, 118(4), 1438–1450, doi:10.1002/jgrg.20111, 2013.

Middle-wood and Late-wood d18O records from 3 Coast Redwood (Sequoia sempervirens) trees at Jedediah Smith State Park site, NW California.

Middle-wood and Late-wood d18O records from 4 Coast Redwood (Sequoia sempervirens) trees at Prairie Creek State Park site, NW California.

plant waters are influenced by spring-summer precipitation d18O, which is strongly influenced by minimum spring-summer temperatures

Spring-summer temperatures since AD 1780 reconstructed from stable oxygen isotope ratios in white spruce tree-rings from the Mackenzie Delta, northwestern Canada

Porter, T. J., Pisaric, M. F. J., Field, R. D., Kokelj, S. V., Edwards, T. W. D., deMontigny, P., Healy, R. and LeGrande, A. N.: Spring-summer temperatures since AD 1780 reconstructed from stable oxygen isotope ratios in white spruce tree-rings from the Mackenzie Delta, northwestern Canada, Climate Dynamics, 42(3-4), 771–785, doi:10.1007/s00382-013-1674-3, 2013.

Climatic Signals in δ13C and δ18O of Tree-rings from White Spruce in the Mackenzie Delta Region, Northern Canada

Porter, T. J., Pisaric, M. F. J., Kokelj, S. V. and Edwards, T. W. D.: Climatic Signals in δ13C and δ18O of Tree-rings from White Spruce in the Mackenzie Delta Region, Northern Canada, Arctic, Antarctic, and Alpine Research, 41(4), 497–505, doi:10.1657/1938-4246-41.4.497, 2009.

A modified method, which is based on standard protocols [Green, 1963; Loader et al., 1997], was used to extract cellulose component from whole wood. 18O/16O ratios using a continuous flow isotope ratio mass spectrometer (Thermo Fisher Scientific Delta V Advantage) coupled to an elemental analyzer (Thermo Fisher Scientific Thermal Conversion/Elemental Analyzer) via a Conflo III interface.

Please check isotopeInterpretation1_name: can this be changed to a standardized term? eg. P_isotope (GF)

TP (31/12/19): climate interpretations (P-negative, T_air-positive) were removed from isotopeInterpretation2 and 3, ; OCh-S: changed; OCh-S:WEBa8749551 needs to be renamed to TR13SAWA00

plant water is linked to precipitation, and the isotope composition of precipitation is negatively correlated with P amount

Sano, M.; Tshering, P.; Komori, J.; Fujita, K.; Xu, C.; Nakatsuka, T.

May-September precipitation in the Bhutan Himalaya since 1743 as reconstructed from tree ring cellulose δ18O

Sano, M., Tshering, P., Komori, J., Fujita, K., Xu, C. and Nakatsuka, T.: May-September precipitation in the Bhutan Himalaya since 1743 as reconstructed from tree ring cellulose δ18O, Journal of Geophysical Research: Atmospheres, 118(15), 8399–8410, doi:10.1002/jgrd.50664, 2013.

TP (31/12/19): climate interpretation (T_air-positive) removed from isotopeInterpretation2

Sidorova, O. V., Siegwolf, R. T. W., Myglan, V. S., Ovchinnikov, D. V., Shishov, V. V., Helle, G., Loader, N. J. and Saurer, M.: The application of tree-rings and stable isotopes for reconstructions of climate conditions in the Russian Altai, Climatic Change, 120(1-2), 153–167, doi:10.1007/s10584-013-0805-5, 2013.

March and July air temperature (r = 0.29; p < 0.01) are positively and significantly correlated to the oxygen isotopes for the period from 1929 to 2008. Oxygen isotopic values, which reflect the condensation temperature of the precipitation water showed increasing trends during 4111 to 3806 BC, indicating warm and dry period.

March and July air temperature (r = 0.29; p < 0.01) are positively and significantly correlated to the oxygen isotopes for the period from 1929 to 2008. Assuming that the same relation might haver persisted earlier as well.

Sidorova, O. V., Saurer, M., Andreev, A., Fritzsche, D., Opel, T., Naurzbaev, M. M. and Siegwolf, R.: Is the 20th century warming unprecedented in the Siberian north?, Quaternary Science Reviews, 73, 93–102, doi:10.1016/j.quascirev.2013.05.015, 2013.

Warmer spring temperatures result in leaf and soil water enrichment

Composite tree-ring d18O record representing five Pinus uncinata trees

Climate sensitivity and parameter coherency in annually resolved δ13C and δ18O from Pinus uncinata tree-ring data in the Spanish Pyrenees

Konter, O., Holzkaemper, S., Helle, G., Buentgen, U., Saurer, M. and Esper, J.: Climate sensitivity and parameter coherency in annually resolved δ13C and δ18O from Pinus uncinata tree-ring data in the Spanish Pyrenees, Chemical Geology, 377, 12–19, doi:10.1016/j.chemgeo.2014.03.021, 2014.

tree-ring cellulose d18O record representing nine Cedrela odorata trees

Comparison with other P_isotope records indicates this tree-ring d18O record is influenced by regional P_isotope trends. However, no climate influence is clearly identified.

Oxygen isotopes in tree rings show good coherence between species and sites in Bolivia

Baker, J. C. A., Hunt, S. F. P., Clerici, S. J., Newton, R. J., Bottrell, S. H., Leng, M. J., Heaton, T. H. E., Helle, G., Argollo, J., Gloor, M. and Brienen, R. J. W.: Oxygen isotopes in tree rings show good coherence between species and sites in Bolivia, Global and Planetary Change, 133, 298–308, doi:10.1016/j.gloplacha.2015.09.008, 2015.

What drives interannual variation in tree ring oxygen isotopes in the Amazon?

Baker, J. C. A., Gloor, M., Spracklen, D. V., Arnold, S. R., Tindall, J. C., Clerici, S. J., Leng, M. J. and Brienen, R. J. W.: What drives interannual variation in tree ring oxygen isotopes in the Amazon?, Geophysical Research Letters, 43(22), 11,831–11,840, doi:10.1002/2016gl071507, 2016.

Significant Correlation with maximum June July Aaugust air temperature (r=0.54; p<0.001)

Naulier, M., Savard, M. M., Begin, C., Gennaretti, F., Arseneault, D., Marion, J., Nicault, A. and Begin, Y.: A millennial summer temperature reconstruction for northeastern Canada using oxygen isotopes in subfossil trees, Climate of the Past, 11(9), 1153–1164, doi:10.5194/cp-11-1153-2015, 2015.

TP: added elevations; OCh-S: replaced soil water to soil, precipitation water; Changed Pub_1 DOI

Significant Correlation with summer months of the England Wales Precipiation series (r = -0.58, n = 161, p < 0.001)

Each of the individual I´18O series has a significant negative correlation (p < 0.001) with the summer (Junea€“August) EWP

Young, G.H.F., Loader, N.j., McCarroll, D., Bale, R.J., Demmler, J.C., Miles, D., Nayling, N.T., Rinne, K. T., Robertson, I., Watts, C., Whitney, M.

Young, G. H. F., Loader, N. J., McCarroll, D., Bale, R. J., Demmler, J. C., Miles, D., Nayling, N. T., Rinne, K. T., Robertson, I., Watts, C. and Whitney, M.: Oxygen stable isotope ratios from British oak tree-rings provide a strong and consistent record of past changes in summer rainfall, Climate Dynamics, 45(11-12), 3609–3622, doi:10.1007/s00382-015-2559-4, 2015.

TP: added elevations; OCh_S: replaced soil water to soil, precipitation water

Significant Correlation with summer months of the England Wales Precipiation series (r= -0.39, n = 163, p<0.001)

Each of the individual I´18O series has a significant negative correlation (p < 0.001) with the summer (Junea€“August) P_E

The oldest part of the reconstruction is characterized by a prolonged period of relatively wet conditions
(1360a€“1450), followed by a period of drier conditions until 1600. Another wet period until 1760 follows, with
a short increase to relatively drier conditions around 1720. The most marked trend in the reconstruction is the shift to
dry conditions from 1760 to 1850. The late 20th century is characterized by increasingly dry summers, but these SPEI
values are not unprecedented in the record.

Labuhn, I., Daux, V., Girardclos, O., Stievenard, M., Pierre, M. and Masson-Delmotte, V.: French summer droughts since 1326 CE: a reconstruction based on tree ring cellulose δ18O, Climate of the Past, 12(5), 1101–1117, doi:10.5194/cp-12-1101-2016, 2016.

Wet conditions for large parts of the record prior to 1800, except two drier intervals in the 14th century and in the earlier half of the 16th century, and the late 20th century is characterized by increasing drought.

tree-ring cellulose mean d18O record representing five picea balfouriana trees

Positive correlation between cellulose d18O and precipitation d18O; the later is negatively influenced by precipitation amount.

Multi-century humidity reconstructions from the southeastern Tibetan Plateau inferred from tree-ring δ 18 O

Wernicke, J., Hochreuther, P., GrieSSinger, J., Zhu, H., Wang, L. and Braeuning, A.: Multi-century humidity reconstructions from the southeastern Tibetan Plateau inferred from tree-ring δ18O, Global and Planetary Change, 149, 26–35, doi:10.1016/j.gloplacha.2016.12.013, 2017.

tree-ring cellulose mean d18O record representing five Abies georgii trees

Cellulose d18O is strongly influenced by isotopically enriched leaf waters, which is negatively correlated with RH.

tree-ring cellulose d18O representing primarily Scots pine from multiple sites in SE Sweden

This record represents a regional composite tree-ring d18O record, developed from sub-fossil and living trees from 20 sites in SE Sweden with a spatial range of 57.04-58.59°N and 14.08-16.44°E. The set of coordinates and elevation given for this record correspond to the middle of the total spatial range.

Seasonal variability in Northern Hemisphere atmospheric circulation during the Medieval Climate Anomaly and the Little Ice Age

Edwards, T. W. D., Hammarlund, D., Newton, B. W., Sjolte, J., Linderson, H., Sturm, C., St. Amour, N. A., Bailey, J. N.-L. and Nilsson, A. L.: Seasonal variability in Northern Hemisphere atmospheric circulation during the Medieval Climate Anomaly and the Little Ice Age, Quaternary Science Reviews, 165, 102–110, doi:10.1016/j.quascirev.2017.04.018, 2017.

tree-ring cellulose mean d18O record representing up to eight (depending on year) Juniperus tibetica trees

A composite d18O time-series representing pooled tree-ring samples (up to 8 trees) of Tibetan juniper (Juniperus tibetica)

Late Holocene relative humidity history on the southeastern Tibetan plateau inferred from a tree-ring δ 18 O record: Recent decrease and conditions during the last 1500 years

GrieSSinger, J., Braeuning, A., Helle, G., Hochreuther, P. and Schleser, G.: Late Holocene relative humidity history on the southeastern Tibetan plateau inferred from a tree-ring δ 18 O record: Recent decrease and conditions during the last 1500 years, Quaternary International, 430, 52–59, doi:10.1016/j.quaint.2016.02.011, 2017.

A Dual Stable Isotope Approach Unravels Common Climate Signals and Species-Specific Responses to Environmental Change Stored in Multi-Century Tree-Ring Series from the Tibetan Plateau

<jats:p>Tree-rings are recorders of environmental signals and are therefore often used to reconstruct past environmental conditions. In this paper, we present four annually resolved, multi-centennial tree-ring isotope series from the southeastern Tibetan plateau. The investigation site, where juniper and spruce trees jointly occur, is one of the highest known tree-stands in the world. Tree ring cellulose oxygen (δ18O) and carbon (δ13C) isotopes were analyzed for a common period of 1685–2007 AD to investigate climate–isotope relationships. Therefore, various climate parameters from a local meteorological station and from the CRU 4.02 dataset were used. Tree-ring δ18O of both species revealed highly significant sensitivities with a high degree of coherence to hydroclimate variables during the growing season. The obtained δ18O–climate relationships can even be retained using a species mean. In contrast, the individual δ13C series indicated a weaker and non-uniform response to the tested variables. Underlying species-specific responses and adaptations to the long-term trend in atmospheric CO2 bias even after a trend correction identified dominant environmental factors triggering the tree-ring δ13C at our site. However, analysis of individual intrinsic water-use efficiency in juniper and spruce trees indicated a species-specific adaptation strategy to climate change.</jats:p>

GrieSSinger, J., Braeuning, A., Helle, G., Schleser, G., Hochreuther, P., Meier, W. and Zhu, H.: A Dual Stable Isotope Approach Unravels Common Climate Signals and Species-Specific Responses to Environmental Change Stored in Multi-Century Tree-Ring Series from the Tibetan Plateau, Geosciences, 9(4), 151, doi:10.3390/geosciences9040151, 2019.

Please check inferred material, should this be soil or leaf water? Please check isotopeInterpretation1_name: can this be changed to a standardized term? eg. P_isotope (GF)

TP (31/12/19): climate interpretation (T_air-positive) removed from isotopeInterpretation3; isotopeInterp2 was incomplete and removed; OCh: replaced to P_E (precipitation_Evaporation, PDSI), Soil water replaced to Leaf water

Calibration with instrumental rainfall record; More specifically, inverse correlations between the I´18O of precipitation and the amount of precipitation are observed at low latitudes, known as the a€˜amount effecta€™ (AraguA¡s-AraguA¡s et al., 1998; Dansgaard, 1964). Therefore, smaller amounts of precipitation are associated with higher I´18O values for precipitation, representing the enrichment of 18O in the source water that is taken up by the trees.

Warmer conditions enhance the evaporation of the soil water, which increases δ18O in the source water.

The isotopic composition of the leaf water originating from soil moisture is subsequently modulated by its transpiration through the stomata, leading to the preferential loss of the lighter isotope (16O) and the consequent enrichment of the leaf water 18O. During the transpiration process, lower relative humidity increases the δ18O of the leaf water.

Because tree-ring δ18O correlates negatively with precipitation and relative humidity and positively with temperature, moisture-related climatic indices are expected to be suitable parameters to explain the variations in tree-ring oxygen isotopes.

Masaki Sano, A.P. Dimri, R. Ramesh, Chenxi Xu, Zhen Li, Takeshi Nakatsuka

Moisture source signals preserved in a 242-year tree-ring δ 18 O chronology in the western Himalaya

Sano, M., Dimri, A. P., Ramesh, R., Xu, C., Li, Z. and Nakatsuka, T.: Moisture source signals preserved in a 242-year tree-ring δ18O chronology in the western Himalaya, Global and Planetary Change, 157, 73–82, doi:10.1016/j.gloplacha.2017.08.009, 2017.

Average tree-ring cellulose d18O representing 7 individual Nothofagus pumilio trees

Temperature (positive) and precipitation amount (negative) have a significant influence on the isotopic composition of precipitation, which influences the isotopic composition of cellulose. The southern annular mode is correlated with both climate variables.

The is a composite d18O record representing seven individual Nothofagus pumilio trees

Imprints of Climate Signals in a 204 Year δ18O Tree-Ring Record of Nothofagus pumilio From Perito Moreno Glacier, Southern Patagonia (50°S)

GrieSSinger, J., Langhamer, L., Schneider, C., SaSS, B.-L., Steger, D., Skvarca, P., Braun, M. H., Meier, W. J.-H., Srur, A. M. and Hochreuther, P.: Imprints of Climate Signals in a 204 Year δ18O Tree-Ring Record of Nothofagus pumilio From Perito Moreno Glacier, Southern Patagonia (50°S), Frontiers in Earth Science, 6, doi:10.3389/feart.2018.00027, 2018.

tree-ring cellulose oxygen isotope ratios were measured using an isotope ratio mass spectrometer (Delta V Advantage, Thermo Scientific) interfaced with a pyrolysis-type high-temperature conversion elemental analyzer (TC/EA, Thermo Scientific) at the Research Institute for Humanity and Nature, Japan.

OCh: replaced to P_E (precipitation_Evaporation, PDSI), Soil water replaced to Leaf water

PDSI gives soil moisture status which in turn is related to precipitation and temperature

Xu, C.; Sano, M.; Dimri, A.P.; Ramesh, R.; Nakatsuka, T.; Shi, F.; Guo, Z.

<jats:p>We have constructed a regional tree ring cellulose oxygen isotope (δ&lt;sup&gt;18&lt;/sup&gt;O) record for the northern Indian sub-continent based on two new records from north India and central Nepal and three published records from Northwest India, western Nepal and Bhutan. The record spans the interval from 1743&amp;amp;ndash;2008 CE. Correlation analysis reveals that the record is significantly negatively correlated with the three regional climatic indices: All India Rainfall (&lt;i&gt;r&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;&amp;amp;minus;0.5, &lt;i&gt;p&lt;/i&gt;&amp;amp;thinsp;&lt;&amp;amp;thinsp;0.001, &lt;i&gt;n&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;138), Indian monsoon index (&lt;i&gt;r&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;&amp;amp;minus;0.45, &lt;i&gt;p&lt;/i&gt;&amp;amp;thinsp;&lt;&amp;amp;thinsp;0.001, &lt;i&gt;n&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;51) and the intensity of monsoonal circulation (&lt;i&gt;r&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;&amp;amp;minus;0.42, &lt;i&gt;p&lt;/i&gt;&amp;amp;thinsp;&lt;&amp;amp;thinsp;0.001, &lt;i&gt;n&lt;/i&gt;&amp;amp;thinsp;=&amp;amp;thinsp;51). The close relationship between tree ring cellulose δ&lt;sup&gt;18&lt;/sup&gt;O and the Indian summer monsoon (ISM) can be explained by oxygen isotope fractionation mechanisms. Our results indicate that the regional tree ring cellulose δ&lt;sup&gt;18&lt;/sup&gt;O record is suitable for reconstructing high-resolution changes in the ISM. The record exhibits significant inter-annual and centennial variations. Inter-annual changes are closely related to the El Niño-Southern Oscillation (ENSO), which indicates that the ISM was affected by ENSO in the past. However, the ISM-ENSO relationship was not consistent over time. Centennial changes in the regional tree ring δ&lt;sup&gt;18&lt;/sup&gt;O record indicate a trend of weakened ISM intensity since 1820. Decreasing ISM activity is also observed in various high-resolution ISM records from southwest China and Southeast Asia, and may be the result of reduced land-ocean thermal contrasts since 1820 CE.
                    </jats:p>

Decreasing Indian summer monsoon in northern Indian sub-continent during the last 180 years: evidence from five tree cellulose oxygen isotope chronologies

Xu, C., Sano, M., Dimri, A., Ramesh, R., Nakatsuka, T., Shi, F. and Guo, Z.: Decreasing Indian summer monsoon in northern Indian sub-continent during the last 180 years: evidence from five tree cellulose oxygen isotope chronologies, https://doi.org/10.5194/cp-14-653-2018

The modified plate method (Kagawa et al., 2015; Xu et al., 2011, 2013b), based on the chemical treatment procedure of the Jayme–Wise method (Green, 1963; Loader et al., 1997), was used to extract alpha-cellulose. Oxygen isotope ratios  were measured using an isotope ratio mass spectrometer (Delta V Advantage, Thermo Scientific) interfaced with a pyrolysis-type high-temperature conversion elemental analyzer (TC/EA, Thermo Scientific) at the Research Institute for Humanity and Nature, Japan.

OCh: replaced to P_E (precipitation_Evaporation, PDSI) Soil water replaced to Leaf water

PDSI reflects the soil moisture stress which is an integrated effect of the precipitation and temperature

tree-ring cellulose d18O record, average of 5 Liriodendron tulipifera trees

Higher vapor pressure deficit (lower RH) results in leaf water 18O enrichment, which results in higher tree-ring d18O values

tree-ring cellulose d18O record, average of 5 Quercus rubra trees

Site-averaged latewood d18O record representing 5 Liriodendron tulipifera trees, and site-averaged latewood d18O record representing 5 Quercus rubra trees.

Tree-ring isotopes capture interannual vegetation productivity dynamics at the biome scale

Levesque, M., Andreu-Hayles, L., Smith, W. K., Williams, A. P., Hobi, M. L., Allred, B. W. and Pederson, N.: Tree-ring isotopes capture interannual vegetation productivity dynamics at the biome scale, Nature Communications, 10(1), doi:10.1038/s41467-019-08634-y, 2019.

latewood cellulose d18O record representing 5 Liriodendron tulipifera trees

Site-averaged latewood d18O record representing 5 Liriodendron tulipifera trees.

tree-ring cellulose d18O record representing 5 Liriodendron tulifera trees

tree-ring cellulose d18O record representing 5 Quercus rubra trees

Site-averaged latewood d18O record representing 5 Quercus rubra trees.

Cahyarini, Sri Yudawati;Pfeiffer, Miriam;Nurhati, Intan Suci;Aldrian, Edvin;Dullo, Wolf-Christian;Hetzinger, Steffen

Wu, Henry C.;Felis, Thomas;Scholz, Denis;Giry, Cyril;Kölling, Martin;Jochum, Klaus P.;Scheffers, Sander R.

Porter, Trevor J.;Schoenemann, Spruce W.;Davies, Lauren J.;Steig, Eric J.;Bandara, Sasiri;Froese, Duane G.

Vinther, B.M.;Jones, P.D.;Briffa, K.R.;Clausen, H.B.;Andersen, K.K.;Dahl-Jensen, D.;Johnsen, S.J.

McGregor, Helen V.;Evans, Michael N.;Goosse, Hugues;Leduc, Guillaume;Martrat, Belen;Addison, Jason A.;Mortyn, P. Graham;Oppo, Delia W.;Seidenkrantz, Marit-Solveig;Sicre, Marie-Alexandrine;Phipps, Steven J.;Selvaraj, Kandasamy;Thirumalai, Kaustubh;Filipsson, Helena L.;Ersek, Vasile

Leduc, Guillaume;Sachs, Julian P.;Kawka, Orest E.;Schneider, Ralph R.

van Breukelen, M.R.;Vonhof, H.B.;Hellstrom, J.C.;Wester, W.C.G.;Kroon, D.

Rosenheim, Brad E.;Swart, Peter K.;Thorrold, Simon R.;Willenz, Philippe;Berry, Lorraine;Latkoczy, Christopher

Swart, P. K.;Thorrold, S.;Rosenheim, B.;Eisenhauer, A.;Harrison, C. G. A.;Grammer, M.;Latkoczy, C.

GrieSSinger, Jussi;Braeuning, Achim;Helle, Gerd;Thomas, Axel;Schleser, Gerhard

Edwards, Thomas W.D.;Hammarlund, Dan;Newton, Brandi W.;Sjolte, Jesper;Linderson, Hans;Sturm, Christophe;St. Amour, Natalie A.;Bailey, Joscelyn N.-L.;Nilsson, Anders L.

GrieSSinger, Jussi;Braeuning, Achim;Helle, Gerhard;Hochreuther, Philipp;Schleser, Gerhard

GrieSSinger, Jussi;Braeuning, Achim;Helle, Gerhard;Schleser, Gerhard;Hochreuther, Philipp;Meier, Wolfgang;Zhu, Haifeng

GrieSSinger, Jussi;Langhamer, Lukas;Schneider, Christoph;SaSS, Bjoern-Lukas;Steger, David;Skvarca, Pedro;Braun, Matthias H.;Meier, Wolfgang J.-H.;Srur, Ana M.;Hochreuther, Philipp