Kriosfera Zemli, 2015, vol. XIX, No. 2, pp. 86–94 http://www.izdatgeo.ru RECONSTRUCTION OF PALEOCLIMATE OF RUSSIAN ARCTIC IN THE LATE –HOLOCENE ON THE BASIS OF ISOTOPE STUDY OF ICE WEDGES I.D. Streletskaya1, A.A. Vasiliev2,3, G.E. Oblogov2, I.V. Tokarev4 1 Lomonosov Moscow State University, Department of Geography, 1 Leninskie Gory, Moscow, 119991, ; [email protected] 2 Earth Cryosphere Institute, SB RAS, 86 Malygina str., Tyumen, 625000, Russia; [email protected], [email protected] 3 Tyumen State Oil and Gas University, 38 Volodarskogo str., Tyumen, 625000, Russia 4 Resources Center “Geomodel” of Saint-Petersburg State University, 1 Ulyanovskaya str., St. Petersburg, 198504, Russia The results of paleoclimate reconstructions for the Russian Arctic on the basis of the isotope composition (δ18O) of ice wedges have been presented with the attendant analysis of all available data on isotope composition of syngenetic ice wedges with determined geologic age. Spatial distributions of δ18O values in ice wedges and elementary ice veins have been plotted for the present time and for MIS 1, MIS 2, MIS 3, and MIS 4. Trend lines of spatial distribution of δ18O for different time periods are almost parallel. Based on the data on isotope composition of ice wedges of different age, winter paleotemperatures have been reconstructed for the Russian Arctic and their spatial distribution characterized. Paleoclimate, ice wedges, isotope composition, atmospheric transfer

INTRODUCTION Over the last decades numerous papers on iso- region [Derevyagin et al., 2010]. These tope composition of ice wedges and its relation to pa- data allow to expand this range and to adjust Vasil- leo-geographic conditions have been published chuk’s equations for the whole Russian Arctic. [Mackay, 1983; Vasil’chuk, 1992; Nikolayev and The problem of formation and alteration of the Mikhalev, 1995; Meyer et al., 2002a,b, 2010a,b; Popp isotope composition of snow in snow cover and ice et al., 2006; Vasil’chuk and Vasil’chuk, 2014]. Recon- has been understudied. Most of the studies are related structions of paleo-geographic conditions are based to glaciers [Fisher et al., 1983; Petit et al., 1999; Opel et on correlation between the values of isotope composi- al., 2009]. It is obvious that fractionation of oxygen tion of atmospheric precipitations (snow and rain) isotopes occurs during the snow accumulation as a and the air temperature [Dansgaard, 1964; Rozanski result of snow sublimation accompanied by loss of et al., 1993]. Ice wedges develop as a result of frost light isotopes [Friedman et al., 1991; Johnsen et al., cracks infilling with snowmelt water and snow, whose 2000; Sokratov and Golubev, 2009; Lacelle, 2011]. An- original isotope composition reflects temperature of other process leading to alteration of the isotope com- snow formation and thus the “isotope signal” sub- position of ice wedges is mixing of snow with snow- sumed into the ice allows reconstructing the winter melt water in the spring, when this mixture fills to air temperature. cryogenic cracks. Estimations of winter air temperatures based on No data on possible alteration of the values of the isotope composition of ice wedges were first per- isotope composition of ice in already existing ice formed by Vasil’chuk [1992]. He suggested simple wedges have been reported. During the time of their equations for estimation of average air temperatures existence, ice wedges are affected by differing tem- for January and for the whole winter [Vasil’chuk, peratures and pressure, which should result in chang- 2006]. In some cases, use of these equations may lead es in the original isotope composition of snow. The to controversial results, because the author did not main question, how large is the influence of these and specify what climate characteristics had been used to other processes on original isotope composition. In establish correlations. For example, it was not ex- other words, we should figure out, whether the cor- plained for what time period the mean winter tem- relation between the isotope composition of snow and perature had been calculated. Besides, Vasilchuk’s air temperature during the formation of ice wedges equations can be applied for relatively narrow range still exists, or fractionation processes alter the isotope of 18O values: –14 to –29 ‰. New isotope data are composition of ice wedges so significantly, that it is available now for Svalbard, Western Yamal, and West- impossible to reconstruct air temperatures. In the lit- ern Taimyr. On the base of the oxygen isotope analy- erature on the isotope composition of glaciers, the sis (δ18O) of about 1600 ice wedge cores, the winter possibility of changes in values of glacier ice isotope air paleotemperatures were reconstructed for the composition with time has been discussed. But recon- Copyright © 2015 I.D. Streletskaya, A.A. Vasiliev, G.E. Oblogov, I.V. Tokarev, All rights reserved.

86 RECONSTRUCTION OF PALEOCLIMATE OF RUSSIAN ARCTIC IN LATE PLEISTOCENE–HOLOCENE structions of paleoclimate are based on the assump- Besides our own, we used all available literature tion that the isotopic values for glacier ice are con- data on isotope composition of ice wedges. For our stant. In this study, we also consider negligible pro- analysis, only the data on syngenetic ice wedges with cesses of isotope separation and presume that the known age of adjacent were used. The original isotope composition of ice wedges is constant available data on epigenetic ice wedges were not used during the whole period of their existence. because the age of their formation can not be deter- mined reliably, and thus it was impossible to find a RESEARCH METHODS AND ORIGINAL DATA relation between the atmospheric temperature and a A study of permafrost sections and isotope com- certain geological time interval. The data base on the position of ice wedges was performed on seven coast- isotope composition of ice wedges, which have been al bluffs of the Kara Sea (Yenisey Gulf, Gydan Gulf, compiled from the literature sources, is very large. and Western Yamal) formed by the late Pleistocene Not all these data are representative: in some cases, and Holocene deposits. Cryostratigraphy of these only sporadic samples were collected, and in most sections and the data on isotope composition of ice cases authors have not reported a total amount of wedges are reported in [Streletskaya et al., 2007, 2009, samples. 2011, 2012; Streletskaya and Vasiliev, 2009, 2012; Ob- Because stratigraphic schemes for Late Pleisto- logov et al., 2012]. Usually, 15–20 samples of each ice cene deposits differ for different regions, and their wedge were examined to determine the isotopic val- geological age determinations do not always agree ues and 2–3 samples of recent elementary veins. All of well, we used ranging the Pleistocene–Holocene age available ice wedges have been sampled. in relation to marine isotope stages (MIS) with their Stable isotopes δ18O and δD values were deter- boundaries accurately determined [Bassinot et al., mined in the isotope laboratory of the Alfred Wagen- 1994]. er Institute for Polar and Marine Research (AWI, Fig. 1 and Table 1 jointly present the data on Potsdam, Germany). The error of estimates for δ18O sampling points, geographical location and δ18O val- is 0.1 ‰, and for δD is 0.8 ‰ [Boereboom et al., ues in the cores of ice wedges of various ages. Num- 2013]. bering in Fig. 1 correspond to the numbers indicated We highly relied on the on the isotope data of in the first column of Table 1. As can be seen, the sam- syngenetic ice wedges coeval with the surrounding pling sites network covers a vast area of the Russian sediments that were conclusively corroborated by Arctic in the latitude/longitude range of 66–78° N fairly accurate determinations of the geological age, and 15–171° E. All of the sampling points tend to be used as proper materials for the analyses. The age of concentrated on the seacoast. Given that the content syngenetic ice wedges proved close to that of the host of Table 1 is varied, the detailed data are provided sediments. In our studies, either radiocarbon dating only for MIS 1 (<11 kyr), MIS 2 (11–24 kyr), and or optically stimulated luminescence method was ap- for MIS 3 (24–57 kyr), while reliable data on the iso- plied to determine the sediments age. topic composition of ice wedges related to MIS 4

Fig. 1. Location of sites, where isotope composition of syngenetic ice-wedges was studied and their sedi- ments age determined. Sites are numbered as indicated in the first column of Table 1.

87 I.D. STRELETSKAYA ET AL.

Table 1. Mean stable oxygen isotope (δ18O) values for ice wedges in the Russian Arctic

Geogra- Mean values (δ18O), ‰ Num- phic Modern ber, cf. Sampling site Holocene Late Neo-Pleistocene Source coordi- (elementa- Fig. 1 (MIS 1) nates ry veins) MIS 2 MIS 3 MIS 4 12 345 6 78 9 1 Adventalen Val- 78°12′ N, –10.5(1)* –15.6 (65) – – – [Budantseva et al., 2012] ley, Svalbard 15°50′ E 2 Pechora Rv. estu- 68°00′ N, –12.4 (1) – – – – [Konyakhin et al., 1996] ary 54°30′ E 3 Amderma Settle- 70°00′ N, –16.5 (4) –20.9 (4) – – – [Vasil’chuk and Kotlyakov, ment 62°00′ E 2000; Leibman et al., 2001] 4 Vorkuta 67°30′ N, –16.0 (12) – – – – [Vasil’chuk et al., 2005] 64°00′ E 5 Marre-Sale Cape, 69°41′ N, –14.0 (2) –16.7 (40) –23.9 (126) –23.6 (1) – [Streletskaya et al., 2013] Western Yamal 66°48′ E 6 Yerkuta Rv., 68°11′ N, –12.3 (1) –20.6 (25) – – – [Budantseva et al., 2012] Western Yamal 68°51′ E 7 Shchuchya Rv., 66°30′ N, –18.2 (1) –19.4 (7) – – – [Vasil’chuk, 1992] Southern Yamal 69°00′ E 8 Seyakha Vostoch- 70°00′ N, –17.3 (2) –19.7 (3) –22.9 (15) –23.9 (17) – [Vasil’chuk, 1992, 2006] naya Rv. 72°30′ E 9 Gydan Peninsula 71°48′ N, – –19.5 (15) –24.1 (5) – – [Oblogov et al., 2012] 75°12′ E Gydan Peninsula 71°50′ N, –18.8 (3) –21.9 (40) – – – [Vasil’chuk, 1992] 75°12′ E 10 Sverdrup Island 75°15′ N, – –19.9 (1) –24.9 (1) – – [Tarasov et al., 1995] 79°00′ E 11 Sibiryakov Island 72°43′ N, – –19.9 (22) – – [Streletskaya et al., 2012] 79°06′ E 12 Dikson Settle- 73°30′ N, –20.7 (1) –20.6 (33) –24.9 (17) – – [Streletskaya et al., 2011, ment 80°33′ E 2013] 13 Sopochnaya 71°53′ N, –16.6 (1) –19.8 (3) –23.7 (42) – – [Streletskaya et al., 2011, Karga Cape 82°40′ E 2013] 14 Ust’-Port Settle- 69°37′ N, –16.4 (1) – – – – [Konyakhin et al., 1996] ment 84°25′ E 15 Labaz Lake 72°20′ N, – –23.0 (138) –30.2 (138) – – [Chizhov et al., 1997] 99°00′ E 16 Cape Sabler 74°33′ N, –20.4(5) –23.1 (8) –26.3 (23) –29.5 (24) – [Derevyagin et al., 1999] 100°32′ E 17 Cape Momotov 74°00′ N, –20.5 (1) –24.9 (>200) –31.0 (>200) – –30.6 (1) [Magens, 2005; Boereboom Klyk 116°00′ E et al., 2013] 18 Western parts of 73°00′ N, –26.0 (1) –22.7 (5) – –29.3 (12) – [Magens, 2005; Schirrmeis- the Rv. delta 124°00′ E ter et al., 2002, 2003] 19 Bykovsky Pen- 71°40′ N, –25.4 (15) –28.2 (239) –30.8 (72) –30.1 (112) –32.0 (1) [Schirrmeister et al., 2002; insula 129°00′ E Meyer et al., 2002b] 20 74°30′ N, –18.1 (1) – –28.5 (5) – – [Vasil’chuk, 2006; Meyer et 139°00′ E al., 2002a] 21 Yana- 72°42′ N, –22.0 (38) –25.0 (>400) – – – [Opel et al., 2011] rivers Valley coast 143°30′ E (Oyagossky Yar) 22 Bolshoy Lyak- 73°11′ N, –20.4 (1) –27.0 (1) – –31.2 (40) – [Meyer et al., 2002a] hovsky Island 143°56′ E 23 75°00′ N, –18.3 (3) – –29.0 (1) – – [Konyakhin et al., 1996; Island 150°00′ E Ivanova, 2012] 24 Rv. basin 69°00′ N, –25.3 (7) –27.0 (6) – –32.4 (61) –33.0 (1) [Konyakhin et al., 1996; area (Bizon) 158°00′ E Vasil’chuk, 2006]

88 RECONSTRUCTION OF PALEOCLIMATE OF RUSSIAN ARCTIC IN LATE PLEISTOCENE–HOLOCENE

Сontinued Table 1 12 345 6 78 9 25 Kolyma Rv. basin 68°40′ N, –25.5 (15) –20.8 (4) –32.5 (19) – – [Vasil’chuk, 1992; Fukuda area (Plakhtinsky 160°17′ E et al., 1997] Yar) 26 Chetyrekhstol- 70°47′ N, –19.2 (14) –20.0 (3) – – – [Konyakhin et al., 1996] bovy Island 161°36′ E 27 Ambarchik Polar 70°00′ N, –2.9 (7) – –29.2 (5) – – [Romanenko et al., 2011] Station 162°00′ E 28 Rauchua Rv. 69°30′ N, – –23.0 (3) –31,2 (10) – – [Kotov, 1998] 167°00′ E 29 70°00′ N, –19.2 (1) –21.6 (8) –30.4 (160) – – [Vasil’chuk, 1992; 168°00′ E Konyakhin et al., 1996] 30 Apapelkhin Valley 70°00′ N, –23.0 (1) – –33.6 (2) – – [Romanenko et al., 2011] 171°00′ E

* The numbers inside parentheses show the quantity of samples used for mean oxygen isotope δ18O values.

(57–71 kyr) are available only for some separate re- However, accurate dating of the elementary veins age gions. is often impossible. Therefore, taking the cue from In order to determine the relationships between Vasil’chuk [1992], we use the approximation method. the isotopic values of ice wedges and air temperature, Elementary veins were sampled at 22 sites, and the and to plot calibration diagram we collected data on data from 20 sites were used for calibration, except the isotopic measurements in elementary ice veins, for the two sites, with the weather stations located at currently forming in various Arctic regions, from a distance of more than 100 km from the sampling Spitsbergen (Svalbard) to Chukotka. sites. The most precise calibration method would con- Climatic characteristics of the areas where ele- sist in direct comparison of the isotopic composition mentary veins formed were derived from the data of elementary veins with their formation accurately provided by the closest weather stations, as their own dated, and the climatic characteristics of that time. annual temperature records for the Russian Arctic.

Table 2. Mean monthly air temperatures in the cold period during 1961–1990 (Climate Normals) According to the data from weather stations in proximity to elementary vein sampling sites De- Weather stations Octo- Novem- Janu- Febru- Sampling site cem- March April May in proximity ber ber ary ary ber Adventalen Valley, Svalbard Barentsburg –4.8 –9.4 –12.3 –14.6 –14.7 –14.5 –11.4 –4.1 Amderma Settlement Amderma –3.7 –11.0 –15.2 –19.9 –19.8 –15.8 –12.2 –5.1 Vorkuta Vorkuta –5.2 –13.4 –17.0 –21.2 –20.1 –14.6 –10.3 –3.1 Marre-Sale Cape, Yamal Peninsula Marre-Sale –5.1 –13.4 –18.2 –22.6 –22.4 –18.3 –13.9 –5.8 Yerkuta Rv., Yamal Peninsula Marre-Sale –5.1 –13.4 –18.2 –22.6 –22.4 –18.3 –13.9 –5.8 Shchuchya Rv., Yamal Peninsula Salekhard –4.9 –15.6 –20.7 –24.8 –23.6 –16.2 –9.9 –1.8 Seyakha Vostochnaya Rv. Seyakha –6.1 –16.2 –21.6 –26.0 –25.9 –21.8 –16.4 –7.1 Settlement of Dixon Dikson –8.6 –19.0 –22.9 –26.8 –26.4 –23.4 –17.9 –9.0 Sopochnaya Karga Cape Sopochnaya Karga –8.2 –20.0 –24.9 –29.2 –28.6 –25.0 –18.7 –9.1 Sabler Cap Taimyr Lake –12.5 –24.6 –29.1 –32.9 –32.4 –29.8 –20.8 –10.4 Mamontov Klyk Cape Terpiay Tumsa –11.7 –25.1 –30.4 –33.6 –32.1 –29.1 –20.8 –9.6 Western part of the Lena Rv. delta Dunai –11.1 –23.7 –29.2 –32.6 –32.3 –29.1 –20.6 –9.2 Bykovsky Peninsula Tiksi –11.4 –24.6 –28.5 –31.8 –30.1 –26.2 –18.7 –6.8 Kotelny Island Kotelny –12.5 –23.2 –27.7 –30.4 –30.8 –28.2 –21.4 –9.6 Bolshoy Lyakhovsky Island Shalaurov Cape –11.4 –23.5 –28.7 –31.2 –31.5 –28.6 –20.9 –8.9 New Siberia Island –13.2 –22.3 –26.3 –28.4 –28.3 –27.1 –19.4 –8.2 Kolyma Rv. basin area (Bizon) Kolymskaya –11.5 –26.4 –32.7 –34.0 –33.5 –28.9 –18.7 –3.7 Kolyma Rv. basin area (Plakhtinsky Yar) Chersky –10.7 –25.2 –31.3 –32.8 –31.5 –25.4 –15.0 –6.2 Chetyrekhstolbovy Island Chetyrekhstolbovy –9.9 –21.2 –26.9 –28.7 –29.6 –26.7 –19.5 –7.0 Ayon Island Ayon Island –10.1 –20.7 –26.3 –28.1 –29.3 –26.9 –19.3 –6.2

89 I.D. STRELETSKAYA ET AL.

When revealing correlations between the elementary –37.0 ‰ strongly deviates from the trend line, and ice veins isotope values and the area’s climatic char- thus far such deviation has remained unexplainable. acteristics, the period over which the climatic param- As follows from Fig. 2, the trend slopes have proven eters have been averaged should be specified. close to each other, although to some extent greater Vasil’chuk [1992] conducted the comparison relying contrasting changes were observed in δ18O from west on elementary veins with estimated age less than to east during the cold phase of MIS 1 and MIS 3. 100 years. Given that the observation time interval at This allows us to make an essential inference most weather stations in northern areas is much about quite stable atmospheric transfer, covering the shorter, it appears not feasible to perform the averag- period beginning 60 kya to the present time. Earlier it ing of climatic parameters for different time intervals, was thought, however, that the direction of atmo- in order to use them for correlations afterwards. In spheric transfer remained unaltered thus far since its our opinion, it appears more practical to opt for the inception 18–20 kya [Vasil’chuk and Vasil’chuk, 2014]. 1961–1990 period accepted as climate standard in Our data have expanded this time span to be 50–60 climatology that can serve as a basis for climatic pa- thousand years. rameters correlation. The elementary ice veins sam- The formation of the Kara Sea ice sheet during pling sites, complemented by a list of the nearby the last glaciation (MIS 2) [Svendsen et al., 2004] had weather stations and climate standard for them are no significant influence on the parameters of atmo- given in Table 2. spheric transfer. Probably, dimensions of the ice sheet Spatial distribution of δ18O in ice wedges were so small that it could not change directions of of various age, as an indicator of climate change atmospheric transfer. The insights into the lesser ex- in the Arctic region tent of the last glaciation in the Kara Sea have been The spatial distribution of δ18O values in elemen- corroborated by the recent studies of submerged ter- tary ice veins, as well as in syngenetic ice wedges of minal moraines [Gusev et al., 2012]. From Fig. 2 it different age (grouped in the age ranges related to the also follows that polygonal ice-wedges developed in marine isotope stages) depending on the longitude, as the Holocene in much severe climatic conditions than shown in Fig. 2. The trend lines for δ18O values for they are today. different age groups were drawn for illustration (vi- The available extensive database on isotope com- sualization) purposes. position of elementary ice veins, geographically, cov- These lines are shown for a better representation ers a large area and holds representative climatic data of WE trends in the spatial variability of δ18O. All allowing to confidently establish correlations be- points are located in the vicinity of the trend lines. tween δ18O and climatic parameters, and to construct The only exception is the δ18O value for the MIS 2 calibration diagram. Given that, technically, ice near Cape Mamontov Klyk, where δ18O constitute wedges form from snow, which is largely affected by –30.5 ‰ according to [Magens, 2005], and –37.0 ‰ natural conditions, correlations only with winter cli- according to [Boereboom et al., 2013]. The value of matic characteristics can be searched.

Fig. 2. Spatial distributions of oxygen stable iso- Fig. 3. Correlations between δ18O values for modern topes and their trend lines in ice-wedges-formed at elementary ice veins and air temperatures: different times in the Russian Arctic. 1 – January; 2 – winter (December–February); 3 – cold period 1 – modern elementary ice veins; 2 – MIS 1; 3 – MIS 2; 4 – (October–May). MIS 3; 5 – MIS 4.

90 RECONSTRUCTION OF PALEOCLIMATE OF RUSSIAN ARCTIC IN LATE PLEISTOCENE–HOLOCENE

The highest correlation range of δ18O (R2 > 0.73) The lowest temperatures of the cold period are accounts for the November, December, January tem- attributed to Cryochron MIS 4 (Zyryanka time). On peratures and the mean winter temperature (Decem- the present-day Laptev Sea coast, the mean tempera- ber through February). Normally, the coldest month ture of the cold period averaged at about –31 °C in (January) temperature, and the coldest season (from the observation period, with the mean January tem- October through May) mean temperature are used perature going down to –42 °C, which dropped even for reconstructions of paleotemperatures. The corre- lower, down to –32 and –43 °C, respectively, on the lation radius (R2) in the δ18O/average temperature coast. With regard to the western- ratio of the cold period adds up only to 0.673, but we most Russian Arctic regions, the data on the isotopic none the less decided to use this correlation, to com- composition of ice wedges are not available for MIS 4, pare our estimates of paleotemperatures for the cold which makes reconstructing the paleotemperatures period with the published data. for the Zyryanka cryochron exceedingly challenging. Fig. 3 illustrates the relations of δ18O to mean Across the transition from MIS 4 to MIS 3 January temperature, to mean winter temperature (Karginsky Interglacial time), the average tempera- and to mean temperatures during the cold period. As ture in the cold period increased by 3–5 °C, and was a first approximation, we used linear trends. The fol- –27…–29 °C in eastern Arctic, with the temperature lowing regression equations describing the relations warmed up to –38…–40 °C in January. At the same between δ18O and corresponding temperatures have time, the average temperature in the cold period rose thus been obtained: to –23…–25 °C in western Arctic. Mean January tem- peratures proved also higher than in the eastern sec- t = 1.12δ18O – 6.43, R2 = 0.745, σ = 2.6, mean Jan tor, not exceeding –32…–35 °C. Thus, the recon- structed paleotemperatures have failed to support the t = 1.15δ18O – 4.6, R2 = 0.754, σ = 2.7, mean win assumption that Karginsky Interglacial time was re- sponsible fore substantially warmer periods [Arkhan- t = 0.885δ18O – 2.55, R2 = 0.674, σ = 2.7. mean col gelov et al., 1988; Meyer et al., 2002a; Schirrmeister et The difference between our estimations of paleo- al., 2002]. Low winter temperatures are also charac- temperatures and those performed by Vasil’chuk teristic of this time, which was earlier marked by [1992, 2006] does not exceed 2 °C. With probabili- Vasil’chuk [1992]. The analysis of the data presented ty of 0.85, the range of temperature variations would in Fig. 4, a, b suggests that the annual winter tem- be ±3.8 °С. peratures decrease during the last Cryochron MIS 2 On the basis of the regression equations obtained (Sartan time) in the European North and in eastern using the isotopic composition values (Table 1) the Arctic was inconspicuous, versus MIS 3. The average mean paleotemperatures were calculated for January temperature of the cold period decreased only by and the cold period accounted for MIS 1, MIS 2, 2 °C, while mean January temperature by <1 °C com- MIS 3 and MIS 4 time intervals. The modern tem- pared to the MIS 3 temperatures. At the same time, perature records (climate standard) were borrowed the mean temperature of the cold period in western from the climate database. Fig. 4 shows the mean sector of the Russian Arctic varied from 3–4 °С on temperatures longitudinal distributions for the cold the Taimyr Peninsula to 0–1 °С in Western Siberia. period (Fig. 4, a) and January (Fig. 4, b). The minimum temperatures during the cold period

Fig. 4. Spatial distributions of the reconstructions yielded modern and paleotemperatures of air in the Russian Arctic: а – cold period temperatures; b – January temperatures; 1 – modern temperatures; 2 – MIS 1; 3 – MIS 2; 4 – MIS 3; 5 – MIS 4.

91 I.D. STRELETSKAYA ET AL. and in January were incidental to the Chukotka ar- State support of the leading scientific schools of eas, reaching –32 и –44 °С, respectively. The transi- the Russian Federation (SciS-335.2014.5). Part of tion from the last glacial Late Pleistocene (MIS 2) to the original data was obtained using equipment of the Holocene (MIS 1) is characterized by a temperature “Geomodel” Resource Center (the Research Park of rise both in the cold period, and in January. The mean St. Petersburg State University). temperature of the cold period and in January had risen by 7–8 °С in the areas of Chukotka, Taimyr, and References by about 4 °C in western sector of the Russian Arctic. Arkhangelov, A.A., Konyakhin, M.A., Mikhalev, D.V., Soloma- The spatial distribution of the winter paleotempera- tin, V.I., Vaikmyae, R.A., 1988. Oxygen isotope composition tures and the ice wedges isotopic composition values of ground ice. In: Problems of Geocryology. Nauka, Moscow, distributions prove the atmospheric transfer to have pp. 152–158. (in Russian) been stable in the Russian Arctic, at least since Bassinot, F.C., Labeyrie, L.L., Vincent, E., Quidelleur, X., Sha- MIS 3. ckleton, N.J., Lancelot, Y., 1994. The astronomical theory of climate and the age of the Brunhes-Matuyama magnetic CONCLUSIONS reversal. Earth and Planet. Sci. Lett., No. 126, 91–108. Boereboom, T., Samyn, D., Meyer, H., Tison, J.-L., 2013. Stable A new database of isotope values for various ma- isotope and gas properties of two climatically contrasting rine isotope stages, from modern to MIS 4, has been (Pleistocene and Holocene) ice wedges from cape Mamontov generated with regard to syngenetic ice wedges of dif- Klyk, Laptev Sea, Northern Siberia. The Cryosphere, No. 7, ferent age in the Russian Arctic. pp. 31–46, doi:10.5194/tc-7-31-2013. It has been established that the direction of at- Budantseva, N.A., Vasil’chuk, A.K., Zemskova, A.M., et al., 2012. δ18 mospheric transfer in winter, basically, has not О variations in Late Holocene ice-wedges and winter Air temperature variability in the Yamal Peninsula, Russia, and changed in the Russian Arctic since about 50–60 kya in Adventdalen, Svalbard. In: Proceedings of the Tenth In- until the present time. The formation of the Kara Sea ternational Conference on Permafrost (TICOP): Resources ice sheets in the Late Pleistocene and their degrada- and Risks of Permafrost Areas in a Changing World. Pechat- tion made no significant impact on the direction of nik, Tyumen, vol. 3, pp. 41–45. (in Russian) the winter atmospheric circulation. That being the Chizhov, A.B., Dereviagin, A.Yu., Simonov, E.F., Hubber- case, the glaciers were likely to be essentially limited ten, H.-W., Siegert, C., 1997. Isotope composition of ground in area and size. ice in the area of Labaz Lake (Taimyr). Kriosfera Zemli I (3), 79–84. On the base of the isotope composition values for modern ice wedges (elementary veins) compared Dansgaard, W., 1964. Stable isotopes in precipitation. Tel- lus 19 (4), 425–463. to climatic characteristics (the mean air temperature Derevyagin, A.Yu., Chizhov, A.B., Brezgunov, V.S., Hub ber- for 1961–1990 time span), correlation dependences ten, H.-W., Siegert, C., 1999. Isotopic composition of ice δ18 between O and winter temperatures have been wedges on Cape Sabler (Taimyr Lake). Kriosfera Zemli specified. The selected regression equations allow to III (3), 41–49. reconstruct temperature of formation of ice wedges Derevyagin, A.Yu., Chizhov, A.B., Meyer, H., 2010. Winter using the isotopic composition data. temperature conditions in the Laptev sea region during the The reconstructions of temperatures have been last 50 thousand years in ice-wedges isotope records. Krio- done for January and the cold period of the Russian sfera Zemli XIV (1), 32–40. Arctic, covering the period from 60 kya to the present Fisher, D.A., Koerner, R.M., Paterson, W.S.B., Dansgaard, W., time. It has been ascertained that MIS 3 was charac- Gundestrup, N., Reeh, N., 1983. Effect of wind scouring on climatic records from ice-core oxygen-isotope profiles. terized by relatively low winter temperatures Nature, No. 301, 205–209. [Vasil’chuk, 1992]. Last ice episode in the Late Pleis- Friedman, I., Benson, C., Gleason, J., 1991. Isotopic changes tocene developed in the conditions of winter tempe- during snow metamorphism, in: Taylor Jr., H.P., O’Neil, J.R., ratures decrease not greater than by 1–2 °С during Kaplan, I.R. (Eds). Stable Isotope Geochemistry: A Tribute MIS 2/MIS 3 transition, in the background. to Samuel Epstein. Spec. Publ., 3. The Geochemical Society, pp. 211–221. The authors would like to thank Hanno Meyer Fukuda, M., Nagaoka, D., Saijyo, K., 1997. Radiocarbon dating (Alfred Wegener Institute for Polar and Marine Re- results of organic materials obtained from Siberia permafrost search, Research Unit Potsdam, Potsdam, Germany) are, in: Report of Institute of Low Temperature Science. for stable isotope analyses of ice wedges. We are also Hokkaido Univ., Sapporo, Japan, pp. 17–28. grateful to Hanno Meyer and Thomas Opel for useful Gusev, E.A., Kostin, D.A., Markina, N.V., et al., 2012. Mapping and genetic interpretation aspects of Quaternary deposits on discussions and constant support of our studies. We the Russian Arctic shelf (results of State Geological Map- thank all participants of field works in West Taimyr, ping-41000/3). Region. Geologia i Metallogenia, No. 50, Gydan and Yamal peninsulas. 5–14. This research work was carried out within the Ivanova, V.V., 2012. Geochemistry of massive ice beds on the framework of RAS Presidium 23 Programs and under New Siberia island (the , Russian Arc-

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