Triple isotopic composition of oxygen in surface snow and water vapor at NEEM (Greenland)

Landais, A.; Steen‐Larsen, Hans Christian; Guillevic, Mathieu; Masson‐Delmotte, Valérie; Vinther, Bo M.; Winkler, R.

doi:10.1016/j.gca.2011.11.022

Cited by 99 publications

(115 citation statements)

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“…The reason for this is the isotopic composition of source moisture being controlled by kinetic effects at evaporation related to wind speed, sea surface temperature and relative humidity (for d-excess) or relative humidity (for 17 O-excess) (Merlivat and Jouzel, 1979;Landais et al, 2012;Johnsen et al, 1989). Measurements of d-excess in Greenland ice cores have therefore been used to infer present and past evaporation conditions and locate the main moisture sources (Johnsen et al, 1989;MassonDelmotte et al, 2005b;Steen-Larsen et al, 2011).…”

Section: Introductionmentioning

confidence: 99%

“…Measurements of d-excess in Greenland ice cores have therefore been used to infer present and past evaporation conditions and locate the main moisture sources (Johnsen et al, 1989;MassonDelmotte et al, 2005b;Steen-Larsen et al, 2011). A few measurements of 17 O-excess conducted at the seasonal scale show a seasonal cycle in anti-correlation with respect to Greenland temperature and δ 18 O (Landais et al, 2012). On stadial-interstadial timescales, existing ice core records have revealed an anti-correlation of d-excess with δ 18 O, reflecting the impact of changes in cloud condensation temperature on (i) the ratio of equilibrium fractionation for δD and δ 18 O (Merlivat and Nief, 1967;Ellehoj et al, 2013) and (ii) kinetic fractionation on ice crystals (Jouzel and Merlivat, 1984).…”

Section: Introductionmentioning

confidence: 99%

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What controls the isotopic composition of Greenland surface snow?

et al. 2014

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Abstract. Water stable isotopes in Greenland ice core data provide key paleoclimatic information, and have been compared with precipitation isotopic composition simulated by isotopically enabled atmospheric models. However, postdepositional processes linked with snow metamorphism remain poorly documented. For this purpose, monitoring of the isotopic composition (δ 18 O, δD) of near-surface water vapor, precipitation and samples of the top (0.5 cm) snow surface has been conducted during two summers (2011)(2012) at NEEM, NW Greenland. The samples also include a subset of 17 O-excess measurements over 4 days, and the measurements span the 2012 Greenland heat wave. Our observations are consistent with calculations assuming isotopic equilibrium between surface snow and water vapor. We observe a strong correlation between near-surface vapor δ 18 O and air temperature (0.85 ± 0.11 ‰ • C −1 (R = 0.76) for 2012). The correlation with air temperature is not observed in precipitation data or surface snow data. Deuterium excess (d-excess) is strongly anti-correlated with δ 18 O with a stronger slope for vapor than for precipitation and snow surface data. During nine 1-5-day periods between precipitation events, our data demonstrate parallel changes of δ 18 O and d-excess in surface snow and near-surface vapor. The changes in δ 18 O of the vapor are similar or larger than those of the snow δ 18 O. It is estimated using the CROCUS snow model that 6 to 20 % of the surface snow mass is exchanged with the atmosphere. In our data, the sign of surface snow isotopic changes is not related to the sign or magnitude of sublimation or deposition. Comparisons with atmospheric models show that day-to-day variations in near-surface vapor isotopic composition are driven by synoptic variations and changes in air mass trajectories and distillation histories. We suggest that, in between precipitation events, changes in the surface snow isotopic composition are driven by these changes in near-surface vapor isotopic composition. This is consistent with an estimated 60 % mass turnover of surface snow per day driven by snow recrystallization processes under NEEM summer surface snow temperature gradients. Our findings have implications for ice core data interpretation and model-data comparisons, and call for further process studies.

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Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

What controls the isotopic composition of Greenland surface snow?

et al. 2014

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“…17 O-excess is therefore not only a tracer for the relative humidity over oceanic source regions, but also can be used to make corrections for the influence of non-moisture source conditions on d-excess in precipitation. At the NEEM (North Greenland Eemian Ice Drilling) of Greenland, simultaneous measurements of  17 O and  18 O in atmospheric vapor vs. precipitation validated firstly the theoretical coefficient of meteoric water line for  17 O and  18 O, and showed that seasonal variation of 17 O-excess is in phase with relative humility over oceanic source regions [80]. 17 O-excess is therefore regarded as a potential tool for reconstructing relative humidity over moisture source.…”

Section: O-excess Recordmentioning

confidence: 66%

“…It provides the possibility to distinguish the influences of relative humidity as well as SST over moisture source, vapor transport processes and local temperature from the ice core stable isotopes when combining both 17 O-excess and d-excess data. However, only limited 17 O-excess measurements were performed up to now, including the surface snow samples collected along a transect from Terra Nova Bay to Dome C [16] and at NEEM [80], as well as the ice core samples from Vostok, EPICA Dome C and Talos Dome [81]. Thus, it is necessary to obtain more 17 O-excess measurements from the other locations (especially the West Antarctica) to explore the spatial and temporal variations of 17 O-excess.…”

Section: Discussionmentioning

confidence: 99%

Climatology of stable isotopes in Antarctic snow and ice: Current status and prospects

2012

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Stable isotopic composition in Antarctic snow and ice is commonly regarded as one of invaluable palaeoclimate proxies and plays a critically important role in reconstructing past climate change. In this paper we summarized the spatial distribution and the controlling factors of D,  18 O, d-excess and 17 O-excess in Antarctic snow and ice, and discussed their reliability and applicability as palaeoclimate proxies. Recent progress in the stable isotopic records from Antarctic deep ice cores was reviewed, and perspectives on bridging the current understanding gaps were suggested. Antarctic Ice Sheet is a highly important part of the Earth system. Thanks to its extraordinary environment of very low temperature, extremely low snow accumulation rate and thick ice layer, a wealth of high resolution and long chronology paleoclimatic information is stored, and hence Antarctic Ice Sheet is honored as archives of the Earth's climate. Because the reliability of future climate prediction is, to a great degree, dependent on our knowledge of the past climatic evolution, Antarctic ice core records play an important role in the current global change studies. O in the Vostok and the EPICA Dome C ice cores have documented temperatures over the past 400 ka and 800 ka BP (before present), respectively [1-4], which well reflects the glacial-interglacial change. A drilling has successfully reached the bedrock at the Dome F site providing an ice core which covers more than 700 ka [5]. The robust couplings of dust-climate and CO 2 -climate over the glacial-interglacial timescales are also revealed by a comparison between   D (  18 O) and the corresponding dust and CO 2 records from the same ice cores, taking account of the ice core ice-age and gas-age difference [6][7][8]. These results contribute significantly to our understanding of the Earth's climatic and environmental evolution during Antarctic

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“…The second-order parameter deuterium excess (d = δD-8 × δ 18 O), which combines the information from δ 18 O and deuterium, has been used to derive information about both condensation temperature and moisture source conditions, namely wind speed, sea surface temperature, and relative humidity (e.g., Stenni et al, 2001;Uemura et al, 2012). Most recently, due to the development of new measuring techniques, the rare isotope 17 O and the corresponding 17 O excess have been introduced into ice core studies (e.g., Landais et al, 2008Landais et al, , 2012Schoenemann et al, 2014). The 17 O excess is supposed to be insensitive to evaporation temperature and less sensitive than d excess to equilibrium fractionation processes during formation of precipitation.…”

Section: Stable Isotopesmentioning

confidence: 99%

The influence of the synoptic regime on stable water isotopes in precipitation at Dome C, East Antarctica

Schlosser¹,

Dittmann²,

Stenni³

et al. 2017

The Cryosphere

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Abstract. The correct derivation of paleotemperatures from ice cores requires exact knowledge of all processes involved before and after the deposition of snow and the subsequent formation of ice. At the Antarctic deep ice core drilling site Dome C, a unique data set of daily precipitation amount, type, and stable water isotope ratios is available that enables us to study in detail atmospheric processes that influence the stable water isotope ratio of precipitation. Meteorological data from both automatic weather station and a mesoscale atmospheric model were used to investigate how different atmospheric flow patterns determine the precipitation parameters. A classification of synoptic situations that cause precipitation at Dome C was established and, together with back-trajectory calculations, was utilized to estimate moisture source areas. With the resulting source area conditions (wind speed, sea surface temperature, and relative humidity) as input, the precipitation stable isotopic composition was modeled using the so-called Mixed Cloud Isotope Model (MCIM). The model generally underestimates the depletion of 18 O in precipitation, which was not improved by using condensation temperature rather than inversion temperature. Contrary to the assumption widely used in ice core studies, a more northern moisture source does not necessarily mean stronger isotopic fractionation. This is due to the fact that snowfall events at Dome C are often associated with warm air advection due to amplification of planetary waves, which considerably increases the site temperature and thus reduces the temperature difference between source area and deposition site. In addition, no correlation was found between relative humidity at the moisture source and the deuterium excess in precipitation. The significant difference in the isotopic signal of hoarfrost and diamond dust was shown to disappear after removal of seasonality. This study confirms the results of an earlier study carried out at Dome Fuji with a shorter data set using the same methods.

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Triple isotopic composition of oxygen in surface snow and water vapor at NEEM (Greenland)

Cited by 99 publications

References 52 publications

What controls the isotopic composition of Greenland surface snow?

What controls the isotopic composition of Greenland surface snow?

Climatology of stable isotopes in Antarctic snow and ice: Current status and prospects

The influence of the synoptic regime on stable water isotopes in precipitation at Dome C, East Antarctica

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