Spatial distribution of 17O-excess in surface snow along a traverse from Zhongshan station to Dome A, East Antarctica

Influence of Summer Sublimation on δD, δ18O, and δ17O in Precipitation, East Antarctica, and Implications for Climate Reconstruction From Ice Cores

“…As a result, the deposition or adding of the blowing snow from the annual snow layer at Dome A (with lower δ 18 O values and higher d‐excess values) into our samples could explain the observed lower δ 18 O values and higher d‐excess values in summer precipitation at Dome A. However, the 17 O‐excess values of the blowing snow should be lower due to the influence of kinetic fractionation at very low temperature (Angert et al, ; Pang et al, ; Risi et al, ), which cannot account for the observed high values of 17 O‐excess in summer precipitation at Dome A. Moreover, the wind speed at Dome A during summer is usually <3 m/s (Ding et al, ), which limits the blowing snow process.…”

“…(a) A comparison of the 17 O‐excess/δ 18 O relationship between summer precipitation (December and January) in central Antarctica (Dome A, Vostok, and Dome C, colored dots) and the surface snow along the traverses from Zhongshan station to Dome A (light gray triangles and the light gray line), Syowa station to Dome F (black triangles and the black line), and Terra Nova Bay to Dome C (purple triangles). It is noted that the shallow surface snow sampling depth (10 cm) of the traverse from Zhongshan station to Dome A may bias the seasonality of precipitation (Pang et al, ). (b) The 17 O‐excess/δ 18 O relationship in precipitation at Dome A, Vostok, and Dome C (colored dots for summer precipitation and open dots for nonsummer precipitation).…”

Seasonal and spatial variations of 17Oexcess and dexcess in Antarctic precipitation: Insights from an intermediate complexity isotope model

“…The coefficients of cloud supersaturation (c = 1.04 and F = 0.003) determined by KC03 were based on tuning to match Antarctic isotopic data using the older fractionation factors and therefore are no longer [Landais et al, 2008] and Zhongshan to Dome F [Pang et al, 2015] traverse, respectively and are shown only for reference. The triangles (d ln ) and squares (d excess ) represent field measurements compiled by Dahe et al [1994] and Masson- for the respective longitudinal sectors defined for the East and West Paths.…”

“…Closer The d excess and d ln of water vapor over the ocean are sensitive to sea surface temperature and relative humidity (and RH n ), with colder SSTs producing lower d excess (or d ln ) and lower relative humidity resulting in higher d excess (or d ln ) as discussed in Merlivat and Jouzel [1979], Risi et al [2010b], Lewis et al [2013], Risi et al [2013], and Pfahl and Sodemann [2014]. Field measurements show that at small spatial and temporal scales, humidity dominates and the direct effect of SST is small [Pfahl and Wernli, 2008;Kurita, 2011;Steen-Larsen et al, 2014b, 2015. However, humidity is itself a function of SST, and on larger temporal and spatial scales SST is also clearly important [e.g., Petit et al, 1991;Cuffey and Vimeux, 2001;Uemura et al, 2008].…”

“…complement the existing suite of isotopic indicators, permitting a more comprehensive investigation of the global hydrological cycle. Although the use of 17 O excess has become common, the factors that control its spatial and temporal variability are not fully understood, as evidenced by the evolving interpretation of 17 O excess in polar climates [Landais et al, 2008;Risi et al, 2010a;Winkler et al, 2012;Risi et al, 2013;Winkler et al, 2013;Schoenemann et al, 2014;Pang et al, 2015]. • Supporting Information S1 • Table S1 Correspondence to: S. W. Schoenemann, schoes@uw.edu Risi et al, 2010a;Winkler et al, 2012;Schoenemann et al, 2014].…”