Kiel automated device for isotope ratio mass spectrometry on a Finnigan Delta XL mass ratio spectrometer.
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"
; archiveType changed - was originally Lake sediment (LS)
"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.
ENSO; Pacific ocean?atmosphere dynamics.
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.
"using equations from Leng and Marshall (2004), measured calcite-?18O values predict lake water temperatures during calcite formation of 14.7 �C, which compareswell with measured growing season temperatures (14 to 16 �C). Similar studies were carried out for Bison Lake that also indicates isotopic equilibrium between calcite and lake water shown in Supplementary Fig. 6 from Anderson (2011)."
fraction of modern 14C activity uncertainty
210Pb, 239+240Pu or 137Cs activity uncertainty
Y if supported 210Pb activity, N if unsupported 210Pb activity
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)
year (MAT3277152d67): interpretation4_scope: '' has been replaced by 'climate'
depth (MAT5e1d4452c1): interpretation4_scope: '' has been replaced by 'climate'
d18O (LS12ANYE): paleoData_isPrimary: '' has been replaced by 'FALSE'
d18O (LS12ANYE): paleoData_primaryAgeColumn: '' has been replaced by 'FALSE'
year (MAT3277152d67): paleoData_isPrimary: '' has been replaced by 'TRUE'
year (MAT3277152d67): paleoData_primaryAgeColumn: '' has been replaced by 'TRUE'
depth (MAT5e1d4452c1): paleoData_isPrimary: '' has been replaced by 'FALSE'
depth (MAT5e1d4452c1): paleoData_primaryAgeColumn: '' has been replaced by 'FALSE'
d18O (LS12ANYE): interpretation2_basis: '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).' has been replaced by ''
d18O (LS12ANYE): interpretation2_direction: 'negative' has been replaced by ''
d18O (LS12ANYE): interpretation2_inferredMaterial: 'lake water' has been replaced by ''
d18O (LS12ANYE): interpretation2_integrationTime: '5-100' has been replaced by ''
d18O (LS12ANYE): interpretation2_integrationTimeUncertaintyType: 'chronological' has been replaced by ''
d18O (LS12ANYE): interpretation2_integrationTimeUnits: 'years' has been replaced by ''
d18O (LS12ANYE): interpretation2_rank: '1' has been replaced by ''
d18O (LS12ANYE): interpretation2_scope: 'isotope' has been replaced by 'climate'
d18O (LS12ANYE): interpretation2_variable: 'effectivePrecipitation' has been replaced by ''
d18O (LS12ANYE): interpretation2_variableGroup: 'EffectiveMoisture' has been replaced by ''
d18O (LS12ANYE): interpretation2_variableGroupDirection: 'negative' has been replaced by ''
d18O (LS12ANYE): interpretation2_variableGroupOriginal: 'P_E' has been replaced by ''
d18O (LS12ANYE): interpretation3_basis: '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.' has been replaced by ''
d18O (LS12ANYE): interpretation3_inferredMaterial: 'lake water' has been replaced by ''
d18O (LS12ANYE): interpretation3_integrationTime: '5-100' has been replaced by ''
d18O (LS12ANYE): interpretation3_integrationTimeUncertaintyType: 'chronological' has been replaced by ''
d18O (LS12ANYE): interpretation3_integrationTimeUnits: 'years' has been replaced by ''
d18O (LS12ANYE): interpretation3_mathematicalRelation: 'increase' has been replaced by ''
d18O (LS12ANYE): interpretation3_rank: '2' has been replaced by ''
d18O (LS12ANYE): interpretation3_scope: 'isotope' has been replaced by 'climate'
d18O (LS12ANYE): interpretation3_seasonality: 'Summer' has been replaced by ''
d18O (LS12ANYE): interpretation3_variable: 'effectivePrecipitation' has been replaced by ''
d18O (LS12ANYE): interpretation3_variableGroup: 'EffectiveMoisture' has been replaced by ''
d18O (LS12ANYE): interpretation3_variableGroupDirection: 'negative' has been replaced by ''
d18O (LS12ANYE): interpretation3_variableGroupOriginal: 'P_E' has been replaced by ''
d18O (LS12ANYE): interpretation4_basis: '' has been replaced by '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).'
d18O (LS12ANYE): interpretation4_direction: '' has been replaced by 'negative'
d18O (LS12ANYE): interpretation4_inferredMaterial: '' has been replaced by 'lake water'
d18O (LS12ANYE): interpretation4_integrationTime: '' has been replaced by '5-100'
d18O (LS12ANYE): interpretation4_integrationTimeUncertaintyType: '' has been replaced by 'chronological'
d18O (LS12ANYE): interpretation4_integrationTimeUnits: '' has been replaced by 'years'
d18O (LS12ANYE): interpretation4_rank: '' has been replaced by '1'
d18O (LS12ANYE): interpretation4_scope: '' has been replaced by 'isotope'
d18O (LS12ANYE): interpretation4_variable: '' has been replaced by 'effectivePrecipitation'
d18O (LS12ANYE): interpretation4_variableGroup: '' has been replaced by 'EffectiveMoisture'
d18O (LS12ANYE): interpretation4_variableGroupDirection: '' has been replaced by 'negative'
d18O (LS12ANYE): interpretation4_variableGroupOriginal: '' has been replaced by 'P_E'
d18O (LS12ANYE): interpretation5_basis: '' has been replaced by '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.'
d18O (LS12ANYE): interpretation5_inferredMaterial: '' has been replaced by 'lake water'
d18O (LS12ANYE): interpretation5_integrationTime: '' has been replaced by '5-100'
d18O (LS12ANYE): interpretation5_integrationTimeUncertaintyType: '' has been replaced by 'chronological'
d18O (LS12ANYE): interpretation5_integrationTimeUnits: '' has been replaced by 'years'
d18O (LS12ANYE): interpretation5_mathematicalRelation: '' has been replaced by 'increase'
d18O (LS12ANYE): interpretation5_rank: '' has been replaced by '2'
d18O (LS12ANYE): interpretation5_scope: '' has been replaced by 'isotope'
d18O (LS12ANYE): interpretation5_seasonality: '' has been replaced by 'Summer'
d18O (LS12ANYE): interpretation5_variable: '' has been replaced by 'effectivePrecipitation'
d18O (LS12ANYE): interpretation5_variableGroup: '' has been replaced by 'EffectiveMoisture'
d18O (LS12ANYE): interpretation5_variableGroupDirection: '' has been replaced by 'negative'
d18O (LS12ANYE): interpretation5_variableGroupOriginal: '' has been replaced by 'P_E'
d18O (LS12ANYE): interpretation6_scope: '' has been replaced by 'isotope'
year (MAT3277152d67): interpretation1_scope: '' has been replaced by 'climate'
year (MAT3277152d67): interpretation2_scope: '' has been replaced by 'climate'
year (MAT3277152d67): interpretation3_scope: '' has been replaced by 'climate'
depth (MAT5e1d4452c1): interpretation1_scope: '' has been replaced by 'climate'
depth (MAT5e1d4452c1): interpretation2_scope: '' has been replaced by 'climate'
depth (MAT5e1d4452c1): interpretation3_scope: '' has been replaced by 'climate'
Updated lipdverse database entry with a changed file.
d18O (LS12ANYE): interpretation1_seasonality: 'winter' has been replaced by 'Winter'
d18O (LS12ANYE): interpretation1_variable: 'P' has been replaced by 'precipitation'
d18O (LS12ANYE): interpretation2_variable: 'P_E' has been replaced by 'effectivePrecipitation'
d18O (LS12ANYE): interpretation3_variable: 'P_E' has been replaced by 'effectivePrecipitation'
Changes made as part of LiPDverse vocabulary standardization process
d18O (LS12ANYE): paleoData_longName: '' has been replaced by 'AD'
year (MAT3277152d67): paleoData_units: 'AD' has been replaced by 'yr AD'
year (MAT3277152d67): paleoData_longName: '' has been replaced by 'AD'
depth (MAT5e1d4452c1): paleoData_longName: '' has been replaced by 'AD'
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.
Rocky Mountain hydroclimate: Holocene variability and the role of insolation, ENSO, and the North American Monsoon