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A variation of stable isotope composition of snow with altitude on the Elbrus mountain, Central Caucasus

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This study aims to analyze the stable isotope composition of the snow cover of the Elbrus Mountain – the highest mountain in Europe. Snow sampled in the middle accumulation period in January 2017, February 2016, January 2001 and during snowmelt in July 1998 and August 2009. Snow sampled at the south slope of Mt. Elbrus at different elevations, and the total altitude range is approximately 1700 m. A significant altitude effect in fresh snow precipitation was determined in February 2001 with gradient –1.3‰ δ18O/100 m (–11.1‰ δ2 H /100 m) at 3100-3900 m a.s.l. and inverse altitude effect in February 2016 with gradient +1.04‰ δ18O /100 m (+8.7‰ δ2 H /100 m) at 3064-3836 m a.s.l. There is no obvious altitude effect of the δ2 H and δ18O values in snow at the Elbrus slope in 2017, except for the height range 2256-3716 m a.s.l., where altitudinal effect of δ18O values was roughly -0.32‰/100m. The δ18O values in the winter snowpack in some cases decrease with increasing altitude, but sometimes are not indicating a temperaturealtitude effect. Post-depositional processes cause isotopic changes, which can result from drifting, evaporation, sublimation, and ablation. The study of altitude effect in snow is important for understanding the processes of snow-ice and snow-meltwater transformation and the snow/ice potential to provide paleo-environmental data.

For citation:

Vasil’chuk Yu., Chizhova J., Frolova N., Budantseva N., Kireeva M., Oleynikov A., Tokarev I., Rets E., Vasil’chuk A. A variation of stable isotope composition of snow with altitude on the Elbrus mountain, Central Caucasus. GEOGRAPHY, ENVIRONMENT, SUSTAINABILITY. 2020;13(1):172-182.


For all studies that require information about the isotopic composition of the snowpack in a catchment, detailed infor­mation on the spatial and temporal variability of the isotopic content of snow is valuable. The water input in snow-dom­inated watershed for residence time analysis, end member mixing analysis or the detection of source water contribution requires a detailed understanding of the effects of factors that modify the isotopic composition of snow cover.

During orographic lift of air mass, the heavier water mol­ecules condense at first, i.e. the precipitation is isotopically enriched, and the cloud moisture is subsequently depleted due to continuous precipitation under equilibrium fraction­ation.

Depletion of the isotopic composition of precipitation with elevation is the”altitude isotope effect”- the altitude iso­tope effect in precipitation well-known since the Dansgaard (1964) research. The altitude effect is temperature-related be­cause the condensation is caused by the temperature drop due to the increasing altitude. Due to the decreasing pres­sure with increasing altitude, a larger temperature decrease is required to reach the saturated water vapor pressure than for isobaric condensation. Moser and Stichler (1970) observed altitudinal isotope effect in fresh snow at the Kitzsteinhorn in Austrian Alps. An elevation gradient for δ180 values between is -0.6 and -1.0% per 100 in high mountains in the snow was determined (Niewodniczanski et al. 1981). However, there was in a wide range of isotope values with small-scale inverse gradient and thus only partly attributable to a linear elevation gradient. These variations explained by conditions during snowfall and after snow deposition, such as wind drift and fractionation by melting processes, as well as orographic and climatic features of the studied areas (Niewodniczanski et al. 1981). For the fresh snow in the Canadian Rocky Moun­tains, elevation gradients range from -0.3 to +1.8% per 100 m, depending on snowfall and accumulation conditions (Moran et al. 2007).

In contrast to the altitude isotope effect in fresh snow, the isotopic composition of an entire snowpack is more complex (Moser and Stichler 1974). The snowpack is altered by sublimation, evaporation, metamorphism of snow crys­tals, percolating of meltwater and isotopically enriched pre­cipitation, especially in temperate climatic conditions (Judy et al. 1970; Ambach et al. 1972; Stichler et al. 2001; Sokratov and Golubev 2009). These processes may conceal the alti­tudinal effect in fresh snow and result in inverse gradients (Moser and Stichler 1970). In some cases, there was no sig­nificant relation between the isotopic signature of the entire snowpack and elevation (Raben and Theakstone 1994; Kang et al. 2002; Koniger et al. 2008).

Dietermann and Weiler (2013) observed only a limited altitude isotope effect in Swiss Alps. The altitudinal effect for δ2Η values at the south-facing slopes ranged from -6.2 to +2.6%/100 m with a wide variability for the individu­al samples. These results confirm the influence of melting processes altering the mean isotopic composition of snow cover. The north-facing slope of this catchment is a steep av­alanche-prone slope popular for mountain skiing. These fac­tors likely lead to snow mixing and disturbance of the altitude isotopic effect (Dietermann and Weiler 2013).

We have found the altitudinal effect on δ180 and δ2Η val­ues of fresh snow on the southern slope of Elbrus in Janu­ary 2001, decreasing with increasing altitude (Vasil'chuk and Chizhova 2010). The of snow becomes more and more deplet­ed in 180 and 2Η content at higher elevations. In the range of 3100-3400 m a.s.l., the gradients are -2.4 % / 100 m for Δδ180 and -20 % for Δδ2Η values, and at altitudes of 3400-3900 m they are -0.6 / 100 m for Δδ180 and -6 % for Δδ2Η values. We found a decreasing d-excess values in snow at 3100 to 3400 m a.s.l. We associated high gradients at altitudes from 3100 to 3400 m with intensive washing out of the air mass and iso­topic depletion during precipitation. However, if we assume, based on the isotope data, the decrease of δ180 values from -17 to -29% in snow with increasing altitude from 3100 to 3400 m due to progressive precipitation, the decreasing of d-excess in this snow could not be explained.

The progressive rainout process based on the Rayleigh fractionation/condensation model predicts increasing d-ex- cess values in the latest stages of precipitation. Also, the equi­librium Reyleigh condensation model including the isotopic kinetic effect (Jouzel and Merlivat 1984) as well as isotopic model including mixed cloud processes (Ciais and Jouzel 1994) predict relatively high values of d-excess.

In many cases, the d-excess is found to increase with alti­tude on the mountain slopes, possibly for a variety of reasons. This issue has not been finally resolved. Hereby, a decreasing d-excess with decreasing δ180 values in fresh snow in Jan­uary 2001 may indicate a very ambiguous formation of the isotopic composition of snow cover on the southern slope of Elbrus.

Recent studies of glaciers of Elbrus are focused on obtain­ing information about the environmental conditions of ice accumulation, including sources of air masses, atmospheric conditions, and the transformation of snow to ice. The stable isotopes and chemical composition are indicators of the pro­cesses involved in atmospheric precipitation.

0bservations of recent retreat of the Elbrus glacier system (Vasil'chuk et al. 2006, 2010; Zolotarev and Kharkovets 2010; Holobaca 2016; Tielidze and Wheate 2017) show significant changes of the glaciers volume and their 'tongues' retreats during the past 100 years, however, there appears to be no signature in the isotopic composition of the glacier ice (Va­sil'chuk et al. 2006).

Although most of the incoming moisture to the Elbrus is of Atlantic origin, some air masses drift from the south­ern deserts. The dust that originates from the foothills of the Djebel Akhdar in eastern Libya and transported to the Cauca­sus along the eastern Mediterranean coast, Syria and Turkey (Shahgedanova et al. 2013) was found in snowpack of Gara- baschi glacier.

Elbrus glacier's ice is paleo-archive, especially at altitudes above 4900 m, where isotope record is undisturbed by the meltwaters due to the absence of melting at this elevation. The isotope records of low-latitude and high-mountain gla­ciers cores have the potential to provide detailed paleo-en- vironmental proxy record and to prove extremely valuable in producing continuous records of atmospheric chemistry and climate (Thompson et al. 1998, 2006a, 2006b; Tian et al. 2003; Yao et al. 2006). The low-latitude Tibetan cores records, espe­cially Dunde and Dasuopu, are consistent with the local tem­perature records (Yao et al. 2006), the more northern sites, similar to Dunde, are thought to be more temperature-dom­inated (e.g., Tian et al. 2003).

In recent years, deep drilling of Elbrus glaciers allowed to obtain δ180 and δ2Η records (Mikhalenko et al. 2015; Kozach- ek et al. 2017). There was no significant correlation between ice core δ180 records from the western Elbrus plateau (height 5115 m a.s.l) with regional temperature, neither with the re­analysis data nor with the data of meteostation (Mikhalen­ko et al. 2015; Kozachek et al., 2017). At the western Elbrus plateau, the snow accumulation rate is high and moreover, pronounced seasonal variations of δ180 and δ2Η values were noted in the core. In spite of the presence of δ180 amplitude in ice core, which could indicate the existence of a δ180-tem- perature relationship, conditions of individual snowfall play an important role. Such conditions include snow mixing by wind and different air masses with different source character­istics affect the precipitation at the base and crest of a moun­tain.

In this case, the study of the formation of an isotope al­titude effect in snow is important for understanding this ex­clusion of temperature effect in ice. Here, the results of iso­tope analysis of the snow samples are presented to provide a better understanding of the spatial and temporal features of snow accumulation on Elbrus.


The Caucasus Mountains are located between the Black and the Caspian Seas and generally oriented from east to southeast, with the Greater Caucasus range often considered as the divide between Europe and Asia. The total area of gla­ciers in the Caucasus is about 1121±30 km2 (Mikhalenko et al. 2015). Glaciers on the Elbrus Mountain are located in the altitudinal range 2800-5642 m.

The coldest conditions occur above 5200 m a.s.l., where the mean summer air temperature does not exceed 0oC, while the Elbrus glaciers between 4700 and 4900 m a.s.l. are prone to surface melting. Snow accumulation measurements from 1985 to 1988 showed total snow accumulation of 400­600 mm w.e. a-1 with considerable wind-driven snow erosion at the col of Elbrus (5300 m a.s.l.).

The summer atmospheric circulation pattern in the Cau­casus is dominated by the subtropical high pressure to the west and the Asian depression to the east. In winter, circula­tion is affected by the western extension of the Siberian High (Volodicheva 2002). The Caucasus is located in the southern part of the vast Russian Plain and therefore buffeted by the unobstructed passage of cold air masses from the north. High mountain ridges in the southern Caucasus deflect air flowing from the west and southwest. The influence of the free atmosphere on the Elbrus glacier regime is greater than local orographic effects as the glacier accumulation area lies above main ridges.

Most part of the annual precipitation falls in the western and southern parts of the Caucasus. For the southern slope of the Caucasus, the amount of precipitation ranges from 3000-3200 mm a-1 in the west to 1000 mm a-1 in the east. The proportion of winter precipitation (0ctober-April) also decreases eastward from more than 50 to 35-40% for the northern Greater Caucasus and from 60-70 to 50-55% for the southern slope (Rototaeva et al. 2006). The proportion of solid precipitation increases with altitude and reaches 100% above 4000-4200 m.

0ur research is focused on the southern slope of Elbrus, from the Azau station (2330 m a.s.l.), along the Garabashi Glacier (43°20' N, 42°26' E) to the summit (Fig. 1). The paper discusses data obtained in 2017, 2016, and, also the data we have obtained in previous years (Vasil'chuk et al., 2006, 2010; Vasil'chuk and Chizhova 2010).


Fig. 1. Space image of Elbrus from SPOT 7 satellite, August 20, 2016


In terms of temperature, the 2015/16 season continued a unique series of warm winters, which began in 2009/10. The temperature anomaly was formed due to warm months at the beginning (November) and the end of winter (February, March). While the traditionally cold months (December, Janu­ary) were slightly different from the long-year norm.

According to the amount of precipitation, the 2015/16 season was 18% below normal, and the winter maximum precipitation was recorded in January. During the January snowfall, 101.9 mm of precipitation fell, which was 36% of the precipitation of the entire cold period (XI-III). The thickness of the snow at the bottom of the valley during the second decade of January increased from 30 cm to 72 cm (weather station Terskol, 2141 m a.s.l.) and from 59 cm to 103 cm (Azau weather station).

Winter 2016/17 was characterized by extremely low pre­cipitation and long periods without precipitation, for exam­ple, until January 26, 2017, snow fell only on 26 November. The level of temperature drop with altitude (lapse rate) for the southern slope of Elbrus is concerned to be 0.6 °C / 100 m. This lapse rate was determined by comparison of automatic weather station (installed on the western Elbrus plateau at 5115 m a.s.l.) record with measurements from the nearest meteorological station (Mikhalenko et al. 2015).


Snow was sampled on the south slope of Mt. Elbrus in the middle of the snow accumulation period in January 2017, February 2016, January 2001 and during snowmelt season in July 1998 and August 2009. In 2017, fresh snow was sampled. In 2016, the surface snow (1 Feb) and fresh snow (3 Feb) were sampled, in 2001 and 2009 fresh snow was sampled. During the ablation season of 1998, surface snow was sampled. The sampling was performed at an altitude of about 1700 m (Fig. 2).


Fig. 2. Sampling profile on the southern slope of Elbrus


Samples of surface snow (from a depth of 0-15 cm) were collected on 1 February 2016 (according to the Terskol weather station, precipitation events were on 28 and 29 Jan­uary). Samples of fresh snow collected on 3 February 2016 (from a depth of 0-15 cm) represent snow fell on 2 February from morning till evening. According to the Terskol weather station on 2 February, 9 mm of precipitation fell.

In January 2001 and August 2009, samples of just depos­ited snow also have been collected within three hours after snowfall at 0-10 cm depth of snow cover. Samples of melted snow were collected at the Garabaschi glacier in July 1998.

In January 2017, samples of fresh snow were collected within the range of 2300-3800 m a.s.l. On January 27 and 28, in the valley and on the slope of Elbrus, the snow fallen on 26 January was sampled. On January 29, snow fell in the af­ternoon and newly deposited snow was sampled on 30 Jan­uary. All snow samples were taken from 0-10 cm depth of snow cover. In the valley (2332 m a.s.l.) and at the slope (3345 m a.s.l.) snow pits had been excavated at 10 cm intervals.

Isotope ratios in snow of 2016, 2017 and 2009 were measured by a Finnigan Delta-V continuous flow mass spec­trometer in Stable Isotope Laboratory of Geographical De­partment of Lomonosov Moscow State University. Concur­rently, isotope composition of snow sampled in 2016, was determined in Saint Petersburg State University Resource center for Geo-Environmental Research and Modeling (GEO­MODEL) by Picarro L-2120i. The differences in measured δ18O values for the same samples in two laboratories does not ex­ceed ±0.3%o. Isotope composition of snow sampled in 2001 and 1998 was measured by W.Papesch in Research center "Arsenal” in Seibersdorf, Austria.

Isotope data are expressed conventionally as δ-notion (%), representing a deviation in parts per thousand, relating to the isotopic composition of V-SMOW (Vienna Standard Mean Ocean Water). International standards V-SMOW2, GISP, SLAP2 were used for the calibration. The measurement pre­cision for δ18O values is ±0.1%.


The δ18O - δ2H ratios for all snow samples (accumulation and melt) are shown in Fig. 3. Most of them are very close to the global meteoric water line.


Fig. 3. The δ18O - δ2H plot for all snow samples: 1998, 2001, 2009, 2016, 2017

Altitude isotope effect in fresh winter snow is clearly vis­ible in 2016 at elevation up to 3000 m a.s.l and in 2001 at elevation from 3000 to 4000 m a.s.l (Fig. 4, a). Inverse altitude effect was observed in fresh snow sampled in 2016 above 3000 m a.s.l and in August 2009 (Fig. 4, b).


Fig. 4. The δ18O values in snow cover of Elbrus Mountain in winter (a) and summer season (b)


The values of d-excess (d ) in fresh snow have season­' exc' al variations increasing in summer (Table 1). The dexc values depend on the relative humidity of the air masses at their oceanic origin (Merlivat and Jouzel 1979). The lower dexc val­ues of precipitation in the northern hemisphere during the summer months correspond with the higher relative air hu­midity which relates to the SST in the oceanic source regions of the air masses concerned. In the Chinese Tien Shan, high dexc values were noted during the winter months when pre­cipitation fell at low temperatures and low relative humidi­ty (Pang et al. 2011). 0n the contrary, the higher dexc values during the winter months are caused by the lower relative humidity at the oceanic source regions. The inverse trend for dexc values in summer precipitation may occur in regions where the atmospheric water vapor dominates due to mois­ture evaporation from continental basins (Schotterer et al. 1993; Schotterer et al. 1997).


Table 1. Deuterium excess of snow cover of Elbrus Mountain 


Type of snow

dexc, %





Summer melted





Winter fresh





Summer fresh





Winter fresh





Winter fresh




We consider separately the surface snow (which lay af­ter falling out for some time and was subjected to various processes: re-deposition, sublimation, melting, drifting, etc.) and fresh newly deposited snow, which was sampled either immediately after snowfall or the next day after.

Newly deposited (fresh) snow

In fresh snow sampled on 27 and 28 January 2017, the δ18O values vary from -24.84 to -34.46%, the δ2Η from -173.2 to -247.9% (Table 2). Regardless of the date of selection, all samples are in the altitude range of 2256-3850 m a.s.l. Prac­tically, there is no clear relationship between the δ18O and δ2Η values and altitude (Fig. 5). However, some weak trend to decreasing δ18O values with altitude can be identified by calculating the difference between isotope content at 2256 m a.s.l. and 3850 m a.s.l. It gives the gradient to be -0.32% δ18O/100 m.


Table 2. The altitudinal distribution of δ18O and δ2H values in fresh snow on Elbrus in 2016 and 2017

Sample ID

Height, m

δ18O, %

Δ δ18O, %/100 m

δ2Η, %

dexc , %



E19 c






E20 c






E21 c






E22 c






E23 c






E24 c






E26 c



+ 1.04



E27 c






E28 c






E29 c



























Not pronounced















E36 с






E37 с






E38 с






E39 с



Not pronounced



E40 с





E41 с






E42 с






E43 с
















Not pronounced





























































































Fig. 5. The altitudinal effect on δ18O and δ2H and d for fresh snow in 27 January 2017


0n 3 February 2016, the δ18O values increased from -34.5% to -25.5% in fresh snow between 2287 and 3836 m a.s.l., the lowest δ180 values were obtained near 3000 m a.s.l. (Fig. 6). It was found that there is a clear inverse altitudi­nal isotope effect between 4000 and 3000 a.s.l. with a gradi­ent of δ18O = +1.04%/100 m (Table 2). Below 3000 m a.s.l., the δ18O and δ2Η values distributed randomly which could be attributed to the lower boundary of air mass or turbulent mixing inside of it.


Fig. 6. The altitudinal effect on δ18O and δ2H and dexc for fresh snow in 8 February 2001 and 3 February 2016


In August 2009, fresh snow showed weak positive iso­tope trend with altitude with a low statistical significance (Fig. 7).


Fig. 7. The altitudinal effect on δ18O and δ2H and dexc for fresh snow in August, 2009 and for surface snow 1 February, 2016


In 2001, the altitudinal isotope effect has been observed above 3000 m in fresh snow with gradient of δ18O -1.3%/100 m and δ2Η -11.1%/100 m (at 3100 m δ18O = -17.81%, δ2Η = -128.1%, at 3900 m δ18O = -28.24%, δ2Η = -217.1%, see Fig. 6).

Simultaneous temperature measurements on the southern slope of Elbrus in the altitude range of 2355-3853 m showed temperature drop with altitude for different types of weather in the 2016/17 season (Table 3).


Table 3. Measured air temperature on the southern slope of Elbrus in 2017

Date and type of the weather Height a.s.l.

30/01/2017 Cloudy with clearings, overhead fog

31/01/20017 Clear, little cloudy

4/02/2017 Clear, in the morning cloudy

5/02/2017 Cloudy with clearings, the bottom of the sun, above the fog





















calculated lapse rate °C/100 m





These values mean that for the snow samples of 2001, in which the altitude isotope effect is pronounced (from 2900 to 3900 m a.s.l.), the relationship coefficient δ18O with T is in the range from 0.55 %o/°C to 0.76 %o/°C (based on Table 3 data for different types of weather). This corresponds to the Rayleigh model of equilibrium isotope fractionation.

The decrease of dexc values with altitude was revealed (see Fig 6). Such decreasing dexc values during snowfall con­tradicts other model calculations (Jouzel and Merlivat 1984; Ciais and Jouzel 1991) and field observations (Vasil'chuk et al. 2005).

Surface snow

Snow sampled on February 1, 2016, in the range of 1900 m - 4100 m a.s.l. is characterized by insignificant isotope vari­ations (see Fig. 7). The possible reasons are: 1) the formation of isotope composition of snow at single condensation level from extensive cloud; 2) the initial isotope signal of the snow may be modified by processes of drifting or wind erosion. In the ab­lation season of 1998, the residual surface melted snow had the highest δ18O values from -6.82 to -8.79% and δ2Η from -41.9 to -57.0% (see Fig. 4, b). That probably was a result of spring-summer snow accumulation modified by sublimation and partial melting. The lower value at 3780 m a.s.l. indicates partial melting of surface snow and exposure of winter snow.

The absence of altitudinal isotope effect can be explained by the fact that snow-bearing air masses undergo no small- scale orographic uplift and secondly that the source and the trajectory of air masses are essential to the average isotopic content (Moran et al. 2007).

Snow pits

The mean values of δ18O for two snow pits in January 2017 at 2332 m and 3345 m a.s.l. were -26.4 %, -24.8 % and the values for δ2Η were -189.7 %, -174.8 %, respectively. While the mean δ18O and δ2Η values in snow pit at a lower altitude are more negative than the values at a higher altitude (Fig. 8). In the pit at 2332 m, the upper horizon is formed by snow with low values of δ18O (-29.4 %) and δ2Η (-215.4 %), this is clear­ly freshly fallen January snow, in other snow horizons the δ18O and δ2Η values are close to a uniform.

Similar values of δ18O and δ2Η were obtained in the mid­dle snow horizons at 3345 m a.s.l., while the lower horizon here is characterized by relatively high values (see Fig. 8), in­dicating the accumulation and preservation of snow, which was fallen most probably in autumn.


Fig. 8. The values of δ18O, δ2H and d in snow pits at 2332 and 3345 m a.s.l.



In fresh snow in February 2016, the most negative val­ues of δ18O from -31.3 to -34.4% in the range of 3064­3457 m a.s.l. (Table 2) are extreme for Elbrus, especially for elevation below 4000 m a.s.l. Snow pit and firn core isotope records obtained at 5115 m a.s.l. (Kutuzov et al. 2013) show a clear season variation from -27 % to -5.5 % for δ18O val­ues. Extremely negative isotope values in fresh snow of 2016 may be explained by drying of the air mass. The evolution of the isotope composition of water vapor during conden­sation and rainout from an idealized air mass is commonly modeled as a Rayleigh distillation process. The late stages of rainout are associated with rapid decreases of δ18O values in precipitation and in vapor. The rate of decrease of δ18O values also increases exponentially as the air mass dries out, and is greater at lower temperatures (Moran et al. 2007).

In any case, we can not ignore the empirical data obtained for snow on 3 February, even if the isotope values distribu­tion was not described by any model.

The formation of an altitude isotopic effect is not always associated with local conditions like a windward / leeward slope, temperature, etc. The absence of altitude effect is often explained by the fact that air masses do not follow the oro­graphic uplift and, secondly, the source and trajectories of air masses, that could change pretty fast, are both important for the formation of isotope composition.

Moore et al. (2016) investigated the importance of non­local processes through the analysis of the synoptic scale circulation during a snowfall event at the summit of Mount Wrangell in south-central Alaska. During this event, there was over a 1-day period in which the local temperature was ap­proximately constant, a change in δ18O values that exceeded half that normally seen to occur between summer and winter in the region. It may be suggested that a change in the source region for the snow that fell on Mount Wrangell during the event from the subtropical eastern Pacific to northeastern Asia.

In order to explain isotope signal in the sow collected on the 3rd of February, we suppose a simultaneous coming of one air mass to the mountain slope, but by two ways. Back­ward air masses trajectories to Mt. Elbrus are provided by NOAA using the HYSPLIT model (Draxler and Rolph 2011), cal­culated for the 3rd of February at 3000 and 5000 m showed one source and one path of moisture from the north. The most negative δ18O and δ2Η values corresponded to 3064-3457 m a.s.l. range. One of the reasons for this distribution of δ18O and δ2Η values in snow is the removal of a part of the snow from the summit zone to a height of 3000 m. In this case, snow with low δ18O and δ2Η values, deposited on summit is blown downward, forming a reverse altitude isotope effect. Another reason is that the altitude of 3000 m corresponds to the zone of maximum accumulation. Progressive precipitation leads to strong isotopic depletion of the remaining vapor and the last precipitation. It is obvious that the inverse high-altitude iso­tope effect is associated with these very negative values at an altitude of about 3000 m.

In fresh snow sampled in 2017 with a weakly decreasing of δ180 and δ2Η values with altitude, there is also a very slight increase of dexc. The main feature of the isotope signature of snow in 2017 is high dexc values reaching 33% (see Table 1, Table 2). Backward HYSPLIT trajectories to Mt. Elbrus for the 26th of January 2017 at 3000 and 5000 m showed the source of moisture was the Mediterranean area. It is known that this region during the winter months due to low relative humidity over the sea is a source of precipitation with high deuterium excess (Gat and Carmi 1970).

In fresh snow sampled in 2001, there was a "classical” alti- tudinal isotope effect in precipitation due to orographic uplift of air masses and the related decrease in the condensation temperature (see Fig. 6).

When precipitation falls from air masses as they traverse topographic barriers, continued Rayleigh distillation on the lee slope should indeed produce an inverse relationship with altitude-lighter isotopic ratios with decreasing altitude. This would suggest a systematic altitudinal relationship that is the opposite of that which is observed on windward slopes, but an inverse relationship of this type is not well established or widely reported.

Poage and Chamberlain (2001) provide a compilation of observed δ18O-elevation gradients from 68 different studies worldwide, with only two of these studies reporting δ18O depletion of precipitation with altitude. Ambiguous or in­verse δ18O-elevation relationships have been reported from eastern (lee) slopes in Sierra Nevada (Friedman and Smith 1970) and the Canadian Rockies (Grasby and Lepitski 2002). Complex altitudinal relationships are also evident in high al­pine snow samples (Niewodnizanski et al. 1981). This study indicates the necessity to further study the isotope variabil­ity of the snow cover to predict the isotopic composition of snowmelt water and to better understand the accumulation processes and the sources of snow in high mountains.


The results suggest that δ18O-elevation gradients in fresh snow on south slope of Elbrus Mountain have similar values but opposite trends in different years and seasons. Above 3000 m in 2001, the δ180 values decreased with altitude by -1.3 %o/100 m (-11,1%o δ2Η /100 m), in 2016, the δ18O values increased with altitude by +1.04 % /100 m (+8.76 % δ2Η /100 m).

In 2017, the relationship between the values of δ18O and δ2Η with the altitude of the terrain is not clearly pronounced with a weakly decreasing δ18O values in an altitude range of 2256-3716 m a.s.l., there is also a very slight increase of dexc. Such an uneven distribution of the isotope composition of snow with altitude in different seasons most likely is ex­plained by various mechanisms of snow deposition - oro­graphic uplift of the air mass along the slope or over-climb­ing through the main Caucasian ridge and considerable drift of dry snow on the slope.

Below 3000 m, the disruption of δ18O-elevation gradi­ents has been attributed to post-depositional altering, wind movement, turbulent mixing of air masses or simultaneous coming of an air mass to the slope.


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About the Authors

Yurij Vasil’chuk
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Julia Chizhova
Institute of Geology of Ore Deposits, Petrography, Mineralogy, and Geochemistry (IGEM RAS)
Russian Federation

Natalia Frolova
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Nadine Budantseva
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Maria Kireeva
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Alexander Oleynikov
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Igor Tokarev
Centre for Geo-Environmental Research and Modelling (GEOMODEL) at St. Petersburg University
Russian Federation
St. Petersburg

Ekaterina Rets
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


Alla Vasil’chuk
Lomonosov Moscow State University
Russian Federation

Faculty of Geography,


For citation:

Vasil’chuk Yu., Chizhova J., Frolova N., Budantseva N., Kireeva M., Oleynikov A., Tokarev I., Rets E., Vasil’chuk A. A variation of stable isotope composition of snow with altitude on the Elbrus mountain, Central Caucasus. GEOGRAPHY, ENVIRONMENT, SUSTAINABILITY. 2020;13(1):172-182.

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