Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
Precipitation weighted signal subject to post-depositional processes
regions plot close to the global meteoric water line of Craig 1961;d2H= 8 d18O + 10)
regions plot close to the global meteoric water line of Craig 1961;d2H= 8 d18O + 10)
regions plot close to the global meteoric water line of Craig 1961;d2H= 8 d18O + 10)
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)'
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)'
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)'
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.
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.
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.
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
GNIP data for Hall Beach and Pond Inlet, near the study site
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)
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)
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)
GNIP data for Groennedal and Prins Christians Sund, near the study site
GNIP data for Groennedal and Prins Christians Sund, near the study site
GNIP data for Groennedal and Prins Christians Sund, near the study site
GNIP data for Groennedal and Prins Christians Sund, near the study site
GNIP data for Groennedal and Prins Christians Sund, near the study site
GNIP data for Groennedal and Prins Christians Sund, near the study site
Daily precipitation amount and dD were measured during 2003–2006 as part of campaign by JAMSTEC.
Daily precipitation amount and dD were measured during 2003–2006 as part of campaign by JAMSTEC.
Daily precipitation amount and dD were measured during 2003–2006 as part of campaign by JAMSTEC.
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).
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).
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).
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
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
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
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
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
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
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
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
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
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.
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.
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.
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.
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.
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.
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.
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.
Rainfall amount and d18O of rainfall depend on the position of the ITCZ and frequency of ENSO
Rainfall amount and d18O of rainfall depend on the position of the ITCZ and frequency of ENSO
Rainfall amount and d18O of rainfall depend on the position of the ITCZ and frequency of ENSO
Rainfall amount and d18O of rainfall depend on the position of the ITCZ and frequency of ENSO
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.
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.
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.
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.
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.
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.
Winter precipitation at this high altitude (2900m and > 3700m) sites fall as snow (contribute >80% to annual total).
Winter precipitation at this high altitude (2900m and > 3700m) sites fall as snow (contribute >80% to annual total).
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.
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.
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.
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.
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.
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.
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.
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.
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.
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.
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.