Palaeoclimate Evolution in Siberia and the Russian Far East from the Oligocene to Pliocene – Evidence from Fruit and Seed Floras

Home , Western Siberia

SVETLANA POPOVA1,2, TORSTEN UTESCHER3, DMITRIY GROMYKO1, ANGELA A. BRUCH4 & VOLKER MOSBRUGGER2,4

1 Komarov Botanical Institute / Laboratory of Palaeobotany, 2 Prof. Popova Street, 197376 Saint Petersburg, Russia (E-mail: [email protected]) 2 Biodiversity and Climate Research Centre (LOEWE BiK-F), Senckenberganlage 25, D-60325 Frankfurt, Germany 3 Steinmann Institute, Bonn University, Nußallee 8, D-53115 Bonn, Germany 4 Senckenberg Research Institute and Natural History Museum, Senckenberganlage 25, D-60325 Frankfurt, Germany

Received 11 May 2010; revised typescripts received 10 August 2010 & 15 November 2010; accepted 16 December 2011

Abstract: Th e Cenozoic continental deposits of Western Siberia, Eastern Siberia and the Russian Far East are best described on the basis of carpological records. Th e palaeoclimate evolution has been reconstructed quantitatively (Coexistence Approach) providing inferred data on temperature, precipitation and the mean annual range of these parameters. Climate curves document the transition from very warm and humid conditions in the Late Oligocene via the Middle Miocene Climatic Optimum to a cool temperate climate during the Pliocene. Compared with other time intervals the Miocene climate is the most comprehensively reconstructed. For the Middle Miocene the Siberian and Far Eastern data are combined with the ‘NECLIME data set’ available for the same time slice, thus allowing a synthesis and discussion of temperature and precipitation patterns on a Eurasia-wide scale. Th e MAT pattern on a Eurasia-wide scale shows a strong latitudinal temperature increase from the Russian Far East to China, and a well expressed longitudinal gradient from Western Siberia to warmer conditions in Europe, the Black Sea area and the Eastern Mediterranean. Th e reconstructed MAP of Western Siberia is around 1000 mm, which is close to the data obtained for the continental interior of Northern China but lower than most of the data in the Eurasian data set.

Key Words: Siberia, Russian Far East, Oligocene, Miocene, Pliocene, fruit and seed fl oras, palaeoclimate

Sibirya ve Rusya Uzak Doğu’sunda Oligosen’den Pliyosen’e Paleoiklim Evrimi – Meyve ve Tohum Floralarından Veriler

Özet: Batı, Doğu Sibirya ve Rusya Uzak Doğu’sunun Senozoyik karasal tortulları karpolojik (tohum-meyve) kayıtları temel alınarak en iyi şekilde tanımlanmıştır. Paleoiklim evrimi, sıcaklık, yağış ve bu parametrelerin yıllık ortalama uzanımlarından elde edilmiş verilere dayanarak sayısal olarak (Birarada Olma Yaklaşımı) yeniden düzenlenmiştir. İklim eğrileri, Geç Oligosen’den Orta Miyosen İklimsel Maksimum’a çok sıcak ve nemli koşullardan, Pliyosen süresince serin ılıman koşullara geçişi belgelemektedir. Diğer zaman aralıkları ile karşılaştırıldığında, Miyosen iklimi en kapsamlı olarak yeniden şekillendirilmiştir. Sibirya ve Uzak Doğu’su Orta Miyosen’i için veriler, Avrasya geniş ölçeğinde sıcaklık ve yağış modellemelerinin sentezi ve tartışmasını sağlayacak şekilde, benzer zaman dilimi için elde edilmiş ‘NECLIME veri seti’ ile biraraya getirilmiştir. Avrasya geniş ölçeğinde yıllık ortalama sıcaklık (YOS) modeli, Rusya Uzak Doğu’sundan Çin’e kuvvetli enlemsel sıcaklık artışı ve Batı Sibirya’dan Avrupa, Karadeniz alanı ve Doğu Akdeniz’deki daha ılık koşullara iyi ifade edilmiş boylamsal değişimi göstermektedir. Batı Sibirya’dan elde edilmiş yıllık yağış miktarı (YYM), Avrasya veri setindeki verilerin çoğundan daha düşük fakat Kuzey Çin’in kıta içinden elde edilmiş veriye yakın olup, 1000 mm civarındadır.

Anahtar Sözcükler: Sibirya, Rusya Uzak Doğusu, Oligosen, Miyosen, Pliyosen, meyve ve tohum fl oraları, paleoiklim

Introduction the Kazakh highlands to the south, and the East Th e Western Siberian Basin is located between Siberian platform and the Taymyr fold belt to the Novaya Zemlya and the Ural Mountains to the west, east and the northeast, respectively. Th e basin covers

315 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

over 3.5 million km2 and represents a depocentre V. Nikitin (1999) and P. Dorofeev (1963) who worked with important hydrocarbon resources, with a on this subject throughout the 20th century. Owing basin fi ll of several thousand metres of Mesozoic to their common eff orts the main composition of the to Cenozoic strata resting on a folded Palaeozoic Cenozoic fl oras of Western Siberia and northeastern basement (Vyssotsky et al. 2006). Th e Cenozoic Russia (including the Far East) was revealed and succession of Western Siberia comprises shallow evolution stages of the fl ora were defi ned. According marine platform sediments and, from the Oligocene to this there are four main evolution stages in the on, predominantly fl uviatile to lacustrine continental Cenozoic fl oras of Siberia (Nikitin 2006). In the fi rst deposits (Arkhipov et al. 2005). While for the marine phase, the pre-Turgayan, a subtropical fl ora existed Palaeogene deposits dinocyst stratigraphy can be (Late Cretaceous–Eocene). Th e second, Turgayan, used for correlation (e.g., Kuz´mina & Volgova phase is characterized by the expansion of a boreal, 2008), younger continental deposits are mainly warm temperate fl ora. Th is fl ora evolved during the dated by palaeobotanical means (e.g., Gnibidenko Early Oligocene and, during the Late Oligocene to 2007). Th us, 17 fl oral complexes were established Early Miocene, was replaced by diverse mesophilous by Nikitin (2006), subdividing the time-span from mixed coniferous-broad-leaved forests. Th e next the Rupelian to the earliest Pleistocene. From the phase, Post-Turgayan (Middle and Late Miocene Serravallian on, these fl ora complexes can partly be to Early Pliocene), mainly shows the dominance of connected to mammal zones (Babushkin et al. 2001). forest-steppe and steppe landscape later on. Th e last Th e stratigraphic concept based on palaeocarpology phase is the modern stage which started at the end of is completed by palynological data (Babushkin et the Pliocene. al. 2001) and magnetostratigraphic studies carried Palaeocarpological studies of the Cenozoic out in the Taganskaja (Kireevskoe locality) and the deposits in Northeastern Siberia and the Far East Besheulskaja Series, approximately corresponding to began in the 1960s. Th ey were complicated by the Burdigalian to Serravalian time-span. As a result, uncertainties in the stratigraphical position of the fl ora a regional stratigraphical scheme was established bearing horizons, by the mostly poor preservation of allowing for correlations with the international the fruits and seeds (Nikitin 2007). Also, sediments standard (Babushkin et al. 2001). are oft en diagenetically altered making preparation of Th e Russian Far East is located between Lake the fossils diffi cult (Nikitin 1969). As a consequence Baikal in Eastern Siberia and the Pacifi c Ocean. Our the knowledge about composition and evolutionary knowledge of the Cenozoic strata in Northeastern history of the Cenozoic fl ora of Northeastern and Siberia including the Far East is still limited. While the Far East is limited (Nikitin 2007). Filling gaps in Western Siberia Cenozoic horizons can be on the map of Siberia and northeastern Russia by traced over long distances, Cenozoic exposures in discovering new localities and identifying fossil Northeastern Siberia and the Far East occur in isolated taxa were one of the main objectives of Russian intramontane and marginal basins, hampering a palaeobotanical research during the middle of the correlation of the strata (Nikitin 2007). Stratigraphic 20th century. subdivision and dating of the continental deposits in Th e Cenozoic palaeoclimate evolution of Europe this area is mainly based on palaeobotanical means is relatively well investigated. Recent studies unravel (Nikitin 2007). continental climate change during the Neogene of At the beginning of the 20th century China. However, only little information is available palaeobotanical research on the Cenozoic fl oras for the high latitudes of northern Eurasia. of Western Siberia began. Leaf fl oras primarily Th e climate evolution of the Neogene of Western originate from Tomsk, Omsk, and Novosibirsk Siberia has been outlined by Nikitin (1988) but was Oblasts and were studied by various researchers based only on qualitative interpretations of the fl oral such as Kryshtofovich (1928), Chahlov (1948), record. A qualitative palaeoclimate record for the Gorbunov (1955), and Yakubovskaya (1957). Th e Cenozoic of the Arctic coastal areas of northeastern most extensive studies were carried out by P. Nikitin, Siberia (Kolyma River Basin) based on pollen fl ora was

316 S. POPOVA ET AL.

published by Laukhin et al. (1992). Th e Nikitin (1988) the Cenozoic continental deposits of Western Siberia climate curve displays a long-term cooling trend is better known. So far, mainly palaeobotanical data from warmest conditions at the Oligocene/Miocene have been used to subdivide the succession. A system transition to a colder climate in the Late Pliocene. of fl ora complexes serves as a basis for the regional During the Miocene this cooling is connected to stratigraphical chart recently developed (Figure 1). drying while for the Pliocene several fl uctuations Th is stratigraphical scheme can be correlated with from humid to dry are displayed. However, the data the palynological and palaeomagnetic zonation given by Nikitin (1988) are not informative enough of Siberia (Gnibidenko et al. 1989; Nikitin 1999; to draw conclusions about climate types existing in Martynov et al. 2000). the single stages. To study the palaeoclimate evolution from the Lunt et al. (2008) suggested that the high latitudes Early Oligocene to the Late Pliocene in diff erent parts are a target region, where proxy data should be of Siberia, the Russian Far East and Tambov oblast acquired. It is relevant because anything that happens (European Russia) the Coexistence Approach (CA) with climate seems to aff ect the higher latitudes. Here was used (Mosbrugger & Utescher 1997). Th e CA we present a fi rst quantitative reconstruction of the follows the nearest living relative concept. It is based Cenozoic palaeoclimate evolution for this region. on climatic requirements of modern plant taxa that are identifi ed as Nearest Living Relatives (NLRs) of the fossil taxa recorded. Climate data for extant plants are Materials and Methods obtained by overlapping plant distribution area and In the present study a total of 91 Cenozoic fruit and modern climatology. Fossil plant taxa and climatic seed fl oras from western and northeastern Siberia requirements of their NLRs are made available in the and the Russian Far East are selected from published Palaeofl ora (www.palaeofl ora.de) data base (Utescher sources and analysed with respect to palaeoclimate & Mosbrugger 2010). Coexistence intervals for (Table 1). Th e individual fl oras comprise 14 to 198 taxa. diff erent climatic parameters can be calculated using For each of the fruit and seed fl oras studied, the fl oral the program Climstat. Th ey defi ne ranges of climate diversity, geographical position and stratigraphical variables that allowed most considered plant taxa to dating are given in Appendix 1. Th ese data were co-exist at the location studied. published by Nikitin (2006) in his monograph on the To apply the CA to the Siberian, Russian Far seed and fruit fl ora of Siberia. Th ree Middle Miocene East and Tambov fl oras, major extensions of the fl oras from the Tambov oblast, in European Russia, Palaeofl ora data base are necessary. A total of are also included in the analysis. Flora lists for these about 270 fossil taxa had to be entered including sites were published by Dorofeev (1963). information on organ type, stratigraphic range, Th e Cenozoic deposits of northeastern Siberia reference, and NLRs cited. Climate data for about have been little investigated. Th e biostratigraphy of 160 modern taxa, both species and genera, not so far available in the Palaeofl ora had to be retrieved. Th is Table 1. Mean taxa diversity of singles fl oras for each time was done by overlapping plant distribution areas and interval from Late Pliocene to Early Oligocene. climatology (M üller 1996). Th e NLR concept provided by Nikitin (2006) was Time slice Number of fl oras Mean taxa diversity checked. For fossil taxa occurring earlier than the Late Pliocene 10 56 Late Miocene, NLRs were preferably identifi ed at the generic level; for younger records a comparison Early Pliocene 2 22 with a single modern species partly makes sense, Late Miocene 7 36 e.g., for Acorus calamus L., Alnus cordata (Loisel.) Middle Miocene 15 58 Loisel., Aralia spinosa Vent., Comptonia peregrina L., Early Miocene 32 56 Hippuris vulgaris L., Sambucus racemosa L., Styrax Late Oligocene 19 83 japonica Zieb. et Zucc.. For Sciadopitys and Sequoia, Early Oligocene 24 45 known to be problematic in the applications of the

317 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

and warmest months (CMT; WMT), mean annual precipitation (MAP), and mean precipitation of the wettest and the driest month (MPwet; MPdry). Th ese 6 climate variables were calculated independently for all fl oras studied, and then the resulting set of 6 CA ranges was used to calibrate data using modern climate space. Th us refi ned, narrower intervals could be obtained, leading to a more precise reconstruction. Details of the procedure are described in Utescher et al. (2009). To illustrate climate change in Siberia, the Russian Far East and Tambov oblast during the Cenozoic, the fl oras are allocated to 7 time intervals (cf. Figures 1–4). Time intervals are defi ned according to the international standard: Early and Late Oligocene, Early, Middle, and Late Miocene, and Early and Late Pliocene. Th is allocation of the fl oras was performed using the system of fl ora complexes (Nikitin 2006). In Western Siberia Figure 1 shows how these fl ora complexes approximately correlate with the chronological standard (Babushkin et al. 2001; cf. chapter 1). As is obvious from the fi gure, there is some overlap of complex and stage boundaries, e.g., for the Late Miocene (later Serravallian to late Tortonian) and the Late Pliocene time interval (Piacenzian to earliest Pleistocene), stratigraphic uncertainties that cannot be overcome when considering the available Figure 1. Standard chronostratigraphy based on Gradstein et al. (2004) and the International Stratigraphic Chart, stratigraphic concept, but that are still acceptable, 2006 (ICS). Th e correlations with Western Siberian we think, in view of the coarse resolution chosen for regional stages (horizons) and fauna complexes the time intervals studied. More details about the follow Babushkin et al. (2001) and Nikitin (2006). stratigraphic positioning of the sites are available in Time intervals defi ned for the present study: a– Late Appendix 1 where fl ora complexes are cited for each Pliocene, b– Early Pliocene, c– Late Miocene, d– Middle Miocene, e– Early Miocene, f– Late Oligocene, fl ora, where known. g– Early Oligocene. To visualize the results, a series of maps is provided and discussed below showing the evolution of the 6 CA on Cenozoic fl oras (cf. Utescher et al. 2000), climate variables analysed in 7 stages throughout the climate data for the plant family are used. Both taxa Cenozoic. For the technical preparation of the maps are relics and had a much wider distribution in the ArcView 3.2 was used. Th e grid was generated using Cenozoic than at present. Th e genera Scindapsus and the following settings of Spatial Analyst: method Urospatha were excluded from the analysis, because IDW; power 2. these present-day tropical elements were common in the mid-latitude Cenozoic carpological record and generally formed climatic outliers in the CA analysis Results (e.g., Utescher et al. 2000). Palaeoclimate data, presently reconstructed for 6 Floras were analysed with respect to 3 temperature diff erent climate variables (mean annual temperature, and 3 precipitation variables: mean annual cold, warm month mean, mean annual precipitation, temperature (MAT), mean temperatures of the coldest annual range of temperature and precipitation) are

318 S. POPOVA ET AL.

Figure 2. Mean annual temperature (left ) and mean annual precipitation (right) in the Cenozoic of Western, Eastern Siberia and the Russian Far East: a– Late Pliocene, b– Early Pliocene, c– Late Miocene, d– Middle Miocene, e– Early Miocene, f– Late Oligocene, g– Early Oligocene.

319 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

Figure 3. Cold month mean temperature (left ) and warm month mean temperature (right) in the Cenozoic of Western, Eastern Siberia and the Russian Far East: a– Late Pliocene, b– Early Pliocene, c– Late Miocene, d– Middle Miocene, e– Early Miocene, f– Late Oligocene, g– Early Oligocene.

320 S. POPOVA ET AL.

Figure 4. Mean annual range of temperature (left ) and mean annual range of precipitation (right) in the Cenozoic of Western, Eastern Siberia and the Russian Far East: a– Late Pliocene, b– Early Pliocene, c– Late Miocene, d– Middle Miocene, e– Early Miocene, f– Late Oligocene, g– Early Oligocene.

321 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

shown in the map series for 7 time intervals. Th e indicated, while the mean for the Late Oligocene is maps allow an analysis of climate change in Siberia, about 14°C, thus indicating a temperature increase the Russian Far East and Tambov oblast during the (Table 2). When comparing the means from MAT, Cenozoic in time and space. Gradients and patterns CMT, and WMT, slightly cooler conditions during obtained for single climate variables are shown in the Oligocene/Miocene transition are indicated for Figures 2–4 and described below. Means of climate Western Siberia fl oras. variables in each time interval obtained for Western In the Early Miocene this cooling trend continued. Siberia and the Russian Far East are given in Table 2. Comparatively low temperature means are indicated For Western Siberia changing climate patterns can for the Koinatkhun fl ora (Appendix 1) in the Far continuously be studied for the time-span from the East, due to the low diversity of the fl ora with Early Oligocene to the Middle Miocene. In the latter only 9 taxa contributing to the climate data in the time interval data for Kazakhstan are also available. analysis (with 8 taxa being the limit in the CA). CA While for the Late Pliocene several data points intervals obtained are quite large, thus allowing also are present, the Late Miocene and Early Pliocene for warmer conditions (MAT: –6.2–16.1°C; CMT: situation cannot be documented. For Eastern Siberia –26.8–6.4°C; WMT: 15.9–25.6°C). Th e mean values and the Far East climate evolution is documented for of MAT reconstructed for the Western Siberian fl oras the time-span from the Early Miocene to the Late (12.9°C) are about 2°C lower than the data from the Pliocene. Far East (10.45°C). A more pronounced contrast between both regions is evident from CMT, with a mean of –5.05°C obtained for the Far East and 2.5°C Temperature for Western Siberia. In the temperature evolution of Western Siberia Th e slightly cooler Early Miocene conditions during the Oligocene, the highest values are were followed by a minor temperature rise during indicated by the Early Oligocene Trubachovo and the Middle Miocene. In the western part of Western Katyl’ga fl oras (Appendix 1), with MAT up to Siberia MAT was around 13.6°C, but the Far East fl ora almost 17.3°C, CMM at 6.6°C, and mean WMM at yield a MAT of 12.05°C. For example, MAT calculated 24.7°C. Th e Early Oligocene Kompasskiy Bor fl ora for the West Siberian Orlovka fl ora (Appendix 1) (Appendix 1), Western Siberia, in contrast, has the ranges from 13.3 to 17.5°C and CMT from –0.1 to lowest temperature results with 10.5°C for MAT, 7.7°C. For the Mamontova Gora and Rezidentsiya 0.05°C for CMM, and 23.3°C for WMM when Ca fl oras of Eastern Siberia (Appendix 1) MAT ranges interval means are regarded. When averaged across from 12.7 to 13.7°C and 3.4 to 16.1°C, respectively all Early Oligocene fl oras a MAT of 13.5°C was (CMT: –0.1–1.3°C / –12.9–6.4°C). Data obtained

Table 2. Regional climate means by time interval.

MAT CMM WMM MAP Mpwet MPdry

Stage Number of mean W mean Far mean W mean Far mean W mean mean W mean Far mean W mean Far mean W mean Far fl oras Siberia East Siberia East Siberia Far East Siberia East Siberia East Siberia East

Late Pliocene 10 8.32 6.3 -2.01 3.3 18.2 20.6 751.46 749.5 105.75 107 28.8 29.25

Early Pliocene 2 7.22 -3.35 22.05 859 113.25 30

Late Miocene 7 9.66 -1.51 21.74 864.71 117.42 115.7

Mid-Miocene 15 13.6 12.05 2.86 2.57 24.1 22.6 965 867 149.4 140.5 44.8 37

Early Miocene 32 12.9 10.45 2.5 5.25 23.9 22.7 994.06 896.83 143.15 117.16 39.86 45.8

Late Oligocene 19 14.13 2.88 24.48 1015.6 145.36 42.97

Early Oligocene 24 13.52 3.13 23.71 1029 139.79 37.5

322 S. POPOVA ET AL.

for the Middle Miocene fl oras of the Tambov oblast Late Oligocene fl oras of Western Siberia (Table 2) (European Russia) indicate the warmest conditions stayed about at the same level, with values ranging observed in our data. For example, one of the fl oral from 1015 to 1029 mm. For the Rupelian Kompasskiy MAT ranges from 15.7 to 20.8°C, CMT from 2.2 to Bor fl ora (Appendix 1), a MAP interval from 776 13.6°C, and WMT from 25.6 to 28.1°C. mm to 864 mm was obtained; for Obukhovka and Th e onset of pronounced cooling is quite evident Pavlograd (Appendix 1) 592 mm to 1146 mm and in the Late Miocene temperature data obtained 820 mm to 869 mm were obtained respectively, with from Eastern Siberia, with MAT at 10.8°C, and the latter values being the lowest registered in our from the Far East, with mean MAT at 9.36°C. Th e Oligocene record. Precipitation rates of the wettest Late Miocene Eastern Siberia Omoloy river fl ora month (MPwet) calculated for the Rupelian Achair (Appendix 1) is characterized by a MAT range from fl ora (Appendix 1) range from 150 mm to 195 mm. 7.3 to 16.1°C, with a CMT of –3.8°C, while for the Th e driest month precipitation (MPdry) of the late Temmirdekh-khaya fl ora (Appendix 1) nearby, MAT Rupelian Antropovo fl ora (Appendix 1) ranges from ranges from 9.3 to 10.8°C, CMT from –2.8 to 1.1°C 53 mm to 64 mm. During the Late Oligocene there and WMT from 21.6 to 23.8°C. Results obtained is a slight increase of observed precipitation rates. from the other Late Miocene fl oras of the Far East For the Dubovka fl ora (Appendix 1) MAP ranges show MAT ranging from 2.42 to 16°C, CMT from between 1146 and 1322 mm, MPwet from 150 to 170 –9.7 to 7°C and WMT ranging from 17.6 to 25.6°C, mm, and MPdry from 41 to 64 mm. indicate a cooling trend. Th e mean MAP determined for the Early Miocene Th e Early Pliocene MAT reconstructed for 2 fl oras of Western Siberia is 994 mm. Th e wettest data points in Eastern Siberia and the Russian Far Western Siberia site is Gorelaya (Appendix 1) with East were lower by more than 2°C than in the Late MAP ranging from 760 to 3151 mm, MPwet around Miocene, testifying to continuing cooling. Late 389 mm and MPdry from 90 to 165 mm. For Early Pliocene fl oras of the Far East are characterized by Miocene fl oras in the Far East a MAP of around MAT around 6°C and thus indicate only a slight 896 mm was obtained. Slightly drier conditions are declining trend when compared to Early Pliocene indicated by the Ulan-Kyuyugyulyur fl ora of Eastern conditions, characterized by MAT around 7°C as Siberia (MAP 592–1206 mm; MPwet 143 mm) and calculated for the Eastern Siberia Delyankir fl ora the Far Eastern Koynatkhun fl ora (MAP 406 – 1206 (appendix 1) with a MAT result 6.9–7.8°C. However, mm; MPwet 64–143 mm). In the Middle Miocene, for CMM a marked temperature decrease from the precipitation rates tend to show no signifi cant change Early to the Late Pliocene is evident from the data. when compared to the Early Miocene level, as for In Western Siberia MAT had clearly dropped below the Tambov oblast and the Western Siberian fl oras. 10°C in the Late Pliocene; for most of the fl oras MAT However, for the Mamontova Gora fl ora in Eastern means from 6°C to 8°C result, except for the fl ora Siberia a slight decreasing trend is shown, with MAP of Merkutlinskiy where a MAT around 11°C was ranging from 776 to 847 mm and MPdry being obtained. Winter temperatures reconstructed for all around 32 mm. Pliocene localities were well below freezing point, Results from the Late Miocene to Early Pliocene contrasting the Middle Miocene conditions. fl oras of the northeastern part of Eurasia show a continuing trend to drier conditions. For instance, MAP reconstructed for the Late Miocene Osinovaya Precipitation fl ora, in the Far East, ranges from 609 to 975 mm, To study precipitation patterns in Western and for the Tnekveem fl ora (Appendix 1) a MAP of at Eastern Siberia and the Russian Far East, mean annual least 373 mm is indicated. Lowest MPDry rates with precipitation (MAP) and the mean annual range of a CA range from 9 mm to 26 mm are obtained for precipitation (MARP– calculated as diff erence of Late Miocene Magadan fl ora. Annual precipitation MPwet and MPdry) were calculated by the CA for rates reconstructed for the Late Pliocene fl oras of the time intervals studied. Th e MAP of Early and West Siberia are 751 mm at a mean, for Far Eastern

323 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

fl oras comparable values are calculated (749 mm at Comparison with Neighbouring Areas a mean). Th e northern Late Pliocene fl ora of Blizkiy, Data cover allows a comparison of the Siberian data Far East, (Appendix 1) shows the driest conditions, set with spatial palaeoclimate data reconstructed for with MAP ranging from 453 to 980 mm, MPwet adjacent continental areas of Eurasia in the three from 68 to 118 mm, and MPdry from 8 to 53 mm. Miocene time intervals considered here. When our Early Miocene climate data reconstructed for Western Discussion Siberia is compared with available palaeoclimate data from Kazakhstan and Northern China, a steep Cenozoic Palaeoclimate Evolution of Siberia gradient to warmer / wetter conditions towards the Th e evolution of temperature patterns of Western South and Southeast is evident (Table 2; Bruch & and Eastern Siberia and the Russian Far East during Zhilin 2006; Liu et al. 2011). MAT means calculated the second half of the Cenozoic largely coincides from the fl oras of the Far East and Western Siberia with the major trends of global climate evolution, as range from about 10°C to 13°C while Kazakhstan refl ected in the marine oxygen isotope record (e.g., fl oras are warmer by 5–6°C; fl oras from Northern Zachos et al. 2001) and in continental climate curves China are warmer by even 7–9°C. CMT and WMT (e.g., Paratethys: Utescher et al. 2007; NW Germany: reconstructed for Western Siberian fl oras show that conditions were cooler by about 3°C in Kazakhstan Utescher et al. 2009). Mean values calculated for and by about 5°C when compared to Northern China. Western and Eastern Siberia and the Russian Far Drier conditions existed in Western and Eastern East (Table 2) show that temperatures increased from Siberia and in the Russian Far East, with mean MAP the Early to the Late Oligocene (Western Siberia) at 994 mm and 896 mm, respectively, whereas wetter followed by a slight decrease in the Early Miocene conditions were observed for Kazakhstan (1077 mm) (Western Siberia). Th e slightly higher values obtained and from the fl oras in Northern and Western China, for the Late Oligocene might be related to the Late ranging from 1173 mm to 1111 mm). Oligocene warming at around 25 Ma known from marine records (Zachos et al. 2001). As well as in In the Middle Miocene, the Siberian data are combined with the ‘NECLIME data set’ available for Western Siberia, a slight temperature decrease in the the same time interval (Bruch et al. 2007; Bruch et Early Miocene is not only documented in marine al. 2011; Liu et al. 2001; Utescher et al. 2011; Yao et records but also in continental curves of Western al. 2011). Th e Eurasia-wide MAT pattern shows a Europe (e.g., Lower Rhine Basin; Utescher et al. strong latitudinal temperature increase from Far East 2009). Russia to China, and a well expressed longitudinal Mean temperature data reconstructed for both gradient from Western Siberia to warmer conditions Western and Eastern Siberia indicate warmer in the West, the Black Sea area and the Eastern conditions for fl oras allocated to the earlier part of the Mediterranean (Figure 5). Mean annual precipitation Middle Miocene (cf. Kaskovsky fl ora complex, Table of Western Siberia, around 1,000 mm, is lower than 2). Th us the Middle Miocene Climatic Optimum other data reconstructed for most Middle Miocene (MMCO) known both from global marine records Eurasian sites. Only fl oras located in the continental and from European continental curves (e.g., Zachos interior of Northern China provide values at a et al. 2001; Mosbrugger et al. 2005) is most probably comparable level (Figure 6). refl ected by the Siberian data. For Eastern Siberia and With smaller-scale regional patterns and trends the Far East the onset of the subsequent Late Miocene of climate evolution both Far Eastern and Siberian Cooling and continuing temperature decrease during fl oras, as well as the fl oral record of Northern China the Pliocene is clearly shown by our data (Table 2; (Liu et al. 2011) show evidence of a slight temperature Far East data column). In Europe, the Late Miocene increase from Early to Middle Miocene. In Northern Cooling is connected to an increase in seasonality China this warming was connected to precipitation of temperature (Utescher et al. 2000, 2007; Bruch et increase while in our study area MAP stayed at the al. 2011). Th is is also evident from the data obtained same level. Results obtained from Middle Miocene from Eastern Siberia and the Far East (Figure 2a–e). fl oras of the Ukrainian Carpathians and Ukrainian

324 S. POPOVA ET AL.

Figure 5. Mean annual temperature reconstructed for the combined Eurasian data set of the NECLIME network for the Middle Miocene time slice.

Figure 6. Mean annual precipitation reconstructed for the combined Eurasian data set of the NECLIME network for the Middle Miocene time slice.

Plain (Syabryaj et al. 2007) are also interesting to trend is most probably connected to a signifi cant compare with fl oras of the European part of Russia northward shift of the tectonic plate (Syabryaj et in our data set (Tambov oblast). Th e mean values al. 2007). Drier conditions, with mean 974 mm are of MAT from the Ukrainian Carpathians and indicated by the fl oras of the Tambov region, when the Tambov oblast indicate similar temperature compared to those of the Ukrainian Carpathians conditions at about 16–17°C, while values from the (1179 mm) and Ukraine Plain (1202 mm). Th is result Ukraine Plain are lower by more than 4°C. Th e same coincides very well with palaeoclimate studies based observation can be made for CMT. Th is decreasing on large mammal hypsodonty, which indicate that

325 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

more arid conditions became established in the mid- 400 mm. In the seasonal distribution of rainfall, the latitudes of the continental interior of Eurasia in the climate over Siberia is dry in winter, with the wettest later Middle Miocene (Eronen et al. 2010). month commonly being August. During summer the As observed for the Middle Miocene (see above), Pacifi c coastal areas of the Far East are infl uenced by Late Miocene data reveal the same latitudinal gradient the East Asian monsoon. from drier conditions in the Far East, with mean Th e SH predominantly originates from radiative MAP at 864 mm to 1058 mm calculated for fl oras cooling of the continental area during winter, and of Northern China (Liu et al. 2011). A comparable its intensity thus correlates closely with local surface latitudinal gradient is obvious for MAT, which is over air temperature (Panagiotopoulos et al. 2005) Th e 5°C higher in Northern China. strength of the SH has a strong impact on the large- scale atmospheric circulation patterns over Eurasia. In Eastern Eurasia, it is known that both Arctic Comparison with Present-day Climate Patterns oscillation (AO) and the intensity of the SH strongly Present-day climate patterns over Siberia show aff ect the East Asian winter monsoon and the outbreak a strong imprint of the Siberian High (SH), the of cold air masses into East Asia (e.g., Gong et al. strongest semi-permanent high pressure system of 2001). However, the SH strongly infl uences winter the Northern Hemisphere. Th e high plays a critical temperatures over the mid-latitudes of Western role in the climate over Eurasia and the Northwest Eurasia because the high can extend westwards and Pacifi c through the formation of a cold and dry thus block lows coming in from the west (Rogers continental air mass in the cold season (Takaya & 1997). Nakamura 2005). Northern Siberia has the lowest Due to the data cover the climate patterns obtained winter temperatures on the globe, an extremely high for the past time intervals are fragmentary. However, seasonality of temperature and comparatively low it is clearly evident that warm and wet climate MAP, with the highest precipitation rates during conditions prevailed in the study area between the summer. Present-day climatology (e.g., New et the Early Oligocene and the Mid-Miocene, with al. 2002) shows that the coldest conditions for MAT CMTs commonly above 0°C. Th e Middle Miocene (<–20°C) and CMT –40°C) are recorded in Eastern temperature gradients have the same sense as today Siberia. Th is is also true for MART doming up in the but are shallower by ca. 80 % (Figure 2, Table 2). MART coastal areas near the Laptev Sea. Climate data show a increases from Kazakhstan (mean ca. 19°C) towards steep latitudinal gradient to warmer conditions in the Western Siberia (mean ca. 22°C) and Eastern Siberia south and shallower longitudinal gradients towards (Mamontova Gora fl ora: 23°C), decreasing again the west and somewhat more pronounced ones towards the Far East (Osinovaja fl ora: 22.5°C). CMT towards the Far East (cf. present-day climatology, shows a parallel pattern. Th is clearly indicates that New et al. 2002). up to the Middle Miocene, atmospheric circulation An imprint of the SH is also evident in MAP patterns substantially diff ered from present-day gradients over Eastern Siberia (cf. present-day conditions and no strong anticyclone existed over climatology, New et al. 2002). MAP is lowest in the Siberia during the cold season. centre of the anticyclone (<300 mm). It shows a steep During the Late Miocene no data are available latitudinal gradient towards wetter conditions from for Western Siberia, but the results obtained from the Arctic coastal areas to the coastal area of East Asia. Eastern Siberia and the Far East for the fi rst time Towards the West, MAP steadily increases, reaching show a higher CMT diff erence of ca. 7°C between 500 to 600 mm in Western Siberia and 600 to 700 mm the Far Eastern Osinovaja site (3°C) and the Omoloy in Eastern Europe. Th is simple pattern is, however, High Arctic site –4°C), attaining ca. 30% of present- complicated by a gradient to dry conditions in the days gradient (–20°C / –47°C). At the same time continental interior of Eurasia comprising most of winter temperatures clearly below freezing point are Kazakhstan, Mongolia and Western China. South of indicated. Western Siberia experienced signifi cant ca. 50 to 55°N latitude, MAP rapidly declines below drying during the Late Miocene Cooling (cf. Middle

326 S. POPOVA ET AL.

Miocene and Late Pliocene MAP data on Figure stratospheric clouds, was proposed by Sloan and 2a, d). Th us it is probable that during the Late Pollard (1998) causing up to 20°C warming of high Miocene, with an intensifying Arctic glaciation (e.g., latitude winter temperatures in the model. Modelling Th iede et al. 1998), circulation patterns in the NH studies for a Tortonian time interval point to started to shift to present-day conditions, although enhanced subtropical jets and increased storm track temperatures were still considerably higher than activity between 40°N and 60°N, as well as higher today and gradients much weaker. Th is observation fl uxes in the sensible and latent heat, leading to a is in agreement with proxies from other high latitude signifi cant warming of the high latitudes. It is shown regions such as palaeobotany-based data obtained that a complete forest cover of the high latitudes that for the Late Miocene Homerian group of Alaska replaces modern tundra vegetation in the model revealing a warmer climatic aspect than previously aff ects albedo and the hydrological cycle, thus leading thought (Reinink-Smith & Leopold 2005). to warmer and wetter conditions in the polar region Th us the above fi ndings largely coincide with (Micheels et al. 2007, 2011). the observation that the intensifi cation of the East Asian winter monsoon did not occur prior to the Summary and Conclusions Late Miocene (at ca. 8 Ma; cf. Qiang et al. 2001; Fan et al. 2006). Th e establishment of this pattern Our results show that the warmest and wettest was accompanied by the onset of drying in the conditions in Western Siberia existed during the mid-latitude continental interior of Eurasia and the Oligocene, with MAT around 14°C, and MAP at expansion of C4 plants in the Himalayan foreland 1000 mm, while Early Miocene data indicate slight from the later Late Miocene on (Fortelius et al. 2002; cooling and drier conditions. In the Middle Miocene Guo et al. 2004; Huang et al. 2007). Th is evolution temperatures increased again while the decreasing is also linked to the uplift history of the Tibetan trend of precipitation continued. In Eastern Siberia Plateau, reinforcing the climatic gradients over and the Russian Far East subsequent cooling began in Eastern Eurasia. Tibetan uplift has strong pulses the Late Miocene. For the Late Pliocene mean MAT between the Late Miocene and the Late Pliocene, as around 6°C is indicated. MAP shows a signifi cant shown by coarse-gained continental sediments and decreasing trend from the Early Miocene on. Th e sedimentary records from ODP sites in the Pacifi c most marked drying (by over 100 mm) occurred in (Zhang et al. 2007). the Late Pliocene. Our data show that drying and cooling intensifi ed Our data signifi cantly contribute to recent, in the study area during the Pliocene. However, quantitative palaeoclimate reconstruction for the the available data cover of both time intervals does Cenozoic of Eurasia based on the palaeobotanical not permit a detailed view. In Northeast China, record. Th ese quantitative climate data for continental possibly more temperate and more humid conditions areas are essential for the validation of the results persisted at the same time (Badaogou fl ora, Jilin; cf. obtained from palaeoclimate modelling. When Stachura-Suchoples & Jahn 2009; Kovar-Eder & Sun, combined with NECLIME data sets, comprising 2009). According to recent dating a Pliocene age of localities all over Eurasia, climate patterns and their this diverse, warmth-loving fl ora cannot be excluded changes throughout the Cenozoic can be studied, for (Sun Ge, personal communication 2010). the fi rst time also including the higher latitudes of So far General Circulation models have diffi culties Eastern Eurasia. In the present study this is done for in simulating palaeo-conditions with very warm and the Middle Miocene: Eurasia-wide reconstruction partly ice-free high northern latitudes (e.g., Knies for other Cenozoic time slices will follow. & Gaina 2008) under an only moderately raised Currently work is in progress to reconstruct the vegetation evolution of Siberia and the Russian Far atmospheric CO2 level (Micheels et al. 2007, 2009; Steppuhn et al. 2007). Nevertheless, model studies East, using the same localities and time intervals. provide clues for possible triggering mechanisms. Th us, it will be possible to reconstruct the full pattern A warming mechanism, e.g., the presence of polar of biodiversity evolution for the Siberian territory

327 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE

related to climate change in the time-span from the Fortelius, Sun Ge, and C. Liu for carefully reviewing Oligocene to the Pliocene. our manuscript, and for their kind advice on how to improve it. Th is work would not have been possible without the fi nancial support granted by DAAD Acknowledgments (A/08/80543) and we also thank the federal state We thank our colleagues A. Micheels and E. Herzog of Hessen (Germany) within the LOEWE initiative for many fruitful discussions. Special thanks are due (Bik-f (E. 1.12 R80573)) for the chance to continue to V.P. Nikitin for help in understanding questions of this study. Th is work is a contribution to the program Western Siberian stratigraphy. We are indebted to M. ‘Neogene Climate Evolution in Eurasia – NECLIME’.

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330 S. POPOVA ET AL. max MPwarm min MPwarm max MPdry. min MPdry. MPwetmin MPwetmax max MAP min MAP max WMT min WMT max Appendix CMT min CMT max MAT min MAT 82; 5572; 56 9.981; 54 7.381; 54 12.5 4.480; 55 –0.3 16.2 4.4 –3.8 0.7 7.3 6.673; 55 12.6 6.2 18.8 –6.4 –11.5 24.6 17.3 7.3 0.7 5.4 3.580; 55 676 23.8 –4.4 17.2 17.2 1076 565 7.3 24.4 4.6 24.4 6.6 1213 561 –5.9 21.6 88 631 11.1 24.4 705 0.7 84 971 –4.4 631 19.6 113 82 0.7 20.3 705 91 167 21.6 544 24 103 23.3 705 117 16 113 631 43 71 980 168 24 38 16 82 91 27 24 109 66 32 84 27 82 113 24 66 95 83; 58 82 125 79; 53 27 24 68 9.569; 56 95 41 9.5 55 13 9.568; 51 13 –2.7 73 68 13 –0.1 2.8 13.3 –0.1 2.8 21.9 94 15.7 24.6 2.8 21.9 –0.1 776 24.9 22.3 6.2 1322 897 23.3 24.9 776 900 25.1 103 971 776 150 1122 168 116 195 150 32 118 42 167 43 32 48 32 78 43 120 69 83 92 141 120 95 122 133; 63 6.9 7.8 –6.9 1.3 18.9 24.9 594 971 103165; 69 139 1.8 24 15.6 –12.9 32 7.8 17.5 82 25.6 373 84 1206 82 143 8 32 82 143 latitude) (longitude; (longitude; Coordinates Coordinates Geographical Geographical 2 2 2 2 3 2 2 1 2 1 1 1 1 Floras Late PlioceneLate Late Miocene Early Pliocene Middle Miocene Middle H3690 Yanran 161; 681.8593.3 16.1707.3 16.1 –12.9719.3 –8.1 7.8 6.4 17.5 16.1 15.9 25.6H3690 10.8 –3.8 25.6 161; 581 Yanran H4967 –2.8 6.4 581 1206 149; Yana H4954 1.1 21.7 1206 132; Temmirdekh-khaj H4954 25.6 21.6 91 133; Omoloy 91H3658 23.8 592 Chattian / early Nekkeveem 735 1206 143 975 143 102 12 88 12 143 32 53 131 18 82 55 24 32 141 32 95 82 82 143 84 H3642 Blizkiy 162; 64–0.6H4080 / Rannebarnaulsky Merkutlinskiy H2245 11.1 / Rannebarnaulsky Maly-shik H2216 –12.8663.4 / Rannebarnaulsky Logovskoy H2460636.9 5.2 / Rannebarnaulsky Kabinet H2646 15.6 / Rannebarnaulsky Delyankir 23.3 10.8H3642 453 –11.8 7.8 162; Blizkiy H3503 5.8 980 –8.7 42km/ Rannebarnaulsky 18.9 1.3H3685 68 25.6 177; 18.8 Tnekveem H2647 592 24.9 147; Hydzhak 1206 118 453 1206 103 8 64 143 53 143 22 55593.4 12 43 118 43 82 16.1 –12.9 33H2283 141 / Kaskovsky Urozhay 6.4H4534 / Kaskovsky Rogozino 107 18.9H3459 143; Residentsiya 25.6H4044 / Besheulsky Pokrov-ishym 592 1206 103 143 22 53 74 120 H3207 / Kaskovsky Yur’ev H3398 / Andreevsky Chernoluch’e 593.3649.1 16.1 –9.5 16.1 6.4 –2.7 17.8 7.8H2811 25.6 19.3 150; Magadan H3681 581 25.6 175; Osinovaja 1206 609 975 98 79 143 143 9 15 26 59 92 47 143 84 H2469 / Rannebarnaulsky Mirny N collect.

331 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE 9.1 20.8 –2.7 13.3 19.3 28.1 609 1322 103 195 22 43 78 195 80; 55 13.3 17.576; 55 –0.168; 56 12.5 7.773; 54 9.1 13 25 12.5 –0.1 27.9 13 13 897 2.8 –2.7 1146 –0.1 21.9 2.8 24.6 2.884; 56 19.3 108 776 22.8 24.683; 56 1122 24.6 6.9 609 13983; 56 776 1322 20.8 150 12.5 1122 –6.9 22 12.5 12.676; 58 103 13.3 150 –0.1 168 13.375; 57 19.3 50 –0.1 5.4 4.4 168 28.4 32 180 9.5 3.576; 58 24.9 16.4 631 84 24.976; 58 24.9 24 –6.5 13 1613 41 41 776 25.1 9.376; 58 7.1 –0.1 95 69 13.8 1076 776 10368; 58 18.9 120 13 2.8 43 11.2 1076 21.376; 58 25.1 102 –2.7 21.9 58 11.270; 62 1.8 195 13 592 141 120 103 24.9 2.8 9.176; 58 1520 13 13.3 –0.1 776 139 21.6 95 22 9.5 20.7 141 20.8 2.8 1.8 1281 24.9 113 103 27.9 9.383; 56 –2.7 13 21.9 32 592 2.8 43 632 10383; 56 13.3 20.8 24.6 32 1437 –2.7 21.9 167 12.5 128176; 58 18.9 –2.7 43 776 24.6 78 2.8 12.5 28.4 10382; 58 13.3 174 13 57 1146 103 776 21.9 22 11.2 592 21.5 82 13 –0.1 1281 24.6 107 150 1520 28.1 12.5 9.379; 52 41 82 195 –0.1 2.8 43 776 195 609 –0.1 15084; 56 94 16.4 2.8 103 24.9 1322 43 1322 168 0.776; 59 22 10 88 –2.7 24.9 78 24.9 24 12.5 103 21.9 168 6.4 776 24.9 11.6 103 195 82 43 32 24.6 9.5 13 43 1281 120 631 –0.1 21.9 776 32 168 25.9 1122 –0.1 0.2 13 22 195 43 107 78 116 1076 58 776 2.8 24.9 –6.4 116 67 32 67 900 24.9 120 150 24.9 22 2.8 154 167 107 631 24.9 120 20.2 43 103 167 58 141 69 648 816 24.6 195 32 900 141 594 82 22 116 195 109 58 32 1400 43 150 43 95 32 103 154 177 43 82 170 82 43 120 22 168 122 22 120 78 141 32 24 25 87 82 43 120 141 78 141 95 133; 63171; 65 12.5 13.7 9.1 –0.1 16.4 1.3 –2.5 21.6 6.4 24.7 19.3 776 25.9 847 609 1322 150 116 195 195 32 22 32 61 120 82 141 154 3 1 3 2 3 1 3 1 1 3 3 3 3 3 1 1 1 1 1 1 1 1 1 1 3 1 Early Miocene Yarsk / Yarsk - Burdigallian Aquitanian 12ss Tambov 40; 5215.7 20.8 2.2 13.6 25.6 28.1012ss 897 40; Tambov 900 109 109 50 67 84 87 84uv Tambov 40; 50145113.3 21.7 –0.1 14.7 13.16 –0.1 26.5 28.184uv 6.8 40; Tambov 594 20.2 1281 24.633uv 42; Tambov 897 116 1281 150 265 24 168 43 50 89 67 172 120 141 H502 / Tagansky Kozhevni H501 / Tagansky Kozhevni H476 / Kireevsky Kozhevni 83; 56 12.5 13.3 –0.1 3.5 24.9 26.2 776 1076 103 113 32 43 82 94 H1022 H3202 / Novomikhaylovsky Orlovka H2570 / Kaskovsky Gora Mamontova H2746 / Isakovsky Borovljan H1297 / Kaskovsky Achair 7013.3H3020 / Tagansky Voronovo H3016 15.7 / Kireevsky Voronovo H3065 –0.1 / Kireevsky Vilenka H2906 6.4 / Vasjuganojarsky Vasyugan H1689 21.6 / Aquitanian dem’yan V. H4950 25.6 133; Ulan-kyu H2891 592 Aquitanian / late yar Perekatny H2905 1206 Ognev/ Ekaterininsky yar H2894 103 / Aquitanian vasjugan Novy H2818 / Ljaminsky Nadtsy H2895 Aquitanian / late Medvedkovo 143H4490 Aquitanian / late Lyamin 65–6.2H1683 / Aquitanian Kulun’yah 22 43 16.1 –26.8H3440 78 6.4 Aquitanian / late yar Konev H2289 15.9 / Aquitanian Kolpashovo H2651 107 25.6 179; Koynatkhun H1039 407 / Tagansky Kluchi H3404 1206 Kireevskoe / Kireevsky H2879 / Vasjuganojarsky Katyl’ga 64 143 12 83 27 143 H3673 / Isakovsky Konachan H3192 / Langian Ivanovka

332 S. POPOVA ET AL. 84;56 9.1 20.8 –2.7 13.3 18.9 28.1 594 1520 103 195 24 67 58 154 73; 5779; 54 –7.7 12.5 27.7 –24.4 15.784; 56 27 –0.184; 56 10.5 9.3 6.480; 59 12.5 32 24.9 21.3 13.8 25.6 21.3 –2.8 76 776 –0.1 15.784; 56 17.8 3151 1122 13.384; 56 1.8 21.5 24.9 13.3 28.3 4684; 56 7.7 108 28.1 12.5 305 15.778; 53 21.9 776 12.1 1534 –0.179; 58 13 26.2 389 170 1322 9.5 7.184; 56 13 776 –0.1 65 12.582; 56 24.9 1146 103 16.8 9 2.8 0.9 41 26.2 15.7 9.583; 60 –6.5 21.9 2.8 103 195 13.3 776 –0.1 16584; 56 16.4 64 9.6 24.9 180 22.3 12.5 1281 15.7 7.183; 56 –2.7 897 20.2 24.6 39 139 2 –0.1 108 16.4 24.9 14 28.2 32 1146 7.1 122 979 –0.1 25.9 2.8 14 338 21.9 14.7 1134 85 258 32 150 141 776 69 7.186; 54 24.9 1194 25.1 –0.1 14.7 174 24.9 900 15084; 56 24.9 776 6.4 1.8 64 27 92 74 12.5 180 776 25.686; 56 1520 21.9 41 6.4 109 13.3 1281 776 15.7 180 24.6 82 177 103 21.9 107 42 13.3 1122 14.7 22083; 56 3.8 43 776 109 24.6 109 –0.1 17.784; 56 42 1213 7.1 95 103 776 43 167 11.2 –0.1 108 6.879; 57 9 24.9 1213 180 32 116 43 13.3 14.7 2.8 21.9 25.6 120 170 32 141 25 24.6 21.3 9.5 11673; 54 1146 3.8 24.9 48 41 120 168 1322 776 –0.1 24.972; 56 141 14.7 6.4 43 32 66 1281 13.3 776 9.582; 52 168 –2.4 43 82 21.6 148 150 21.6 41 1281 5.4 24.6 43 4.4 82 13 103 27.9 214 1146 14 82 41 17.5 21.9 87 116 –0.1 43 170 592 1281 78 –6.9 24.6 107 16.4 168 2.8 1281 43 107 776 7.7 –0.5 78 103 41 180 21.7 120 1400 103 18.9 7.1 41 24.9 82 27.9 64 24.7 41 95 592 195 108 592 43 26.2 195 1146 95 120 1146 43 776 24 139 116 82 22 1213 103 141 82 27 32 116 41 95 139 139 107 85 43 58 174 22 22 95 82 43 32 68 64 83 39 82 58 76 95 95 120 84.2; 56 13.3 16.4 –0.1 7.1 23 25.1 776 1281 150 167 32 50 74 107 2 2 2 2 3 3 2 87; 579.5 87; 13 –2.7 2.8 21.9 24.6 776 1322 103 168 32 43 82 95 2 1 1 2 2 1 2 1 3 1 1 3 1 3 1 2 2 1 1 1 Late Oligocene Early Oligocene H514 / Ambrosimovsky yar Cherny H639 sad / Zhuravsky Lagerny H4036 / Altymsky Pavlograd H2031 / Aquitanian rechka Berezovaja H1792 142;67 Indigirka H1697 / Aquitanian Gorelaya 9.5 16.1 –2.8 6.4 21.9 25.6 776 1194 108 143 32 83 108 141 H1510 / Kireevsky Dovol’noe H2008 / Aquitanian Barchan H4766 / Aquitanian Amelich H4051 sad / Zhuravsky Lagerny 5213.3H2285 Ozeryan / Zhuravsky H4759569.5 / Zhuravsky Nevol’ka H2009 / Zhuravsky Nelyubino 17H1977 / Basandaysky Mura –0.1H4152 / Novomikhaylovsky bor Kompasskiy 20.8H3058 6.2 / Koshkulsky nagorny Ishym –2.7H1953 21.9 Khmelevka / Koshkulsky 13.3 28.1H1926 21.9 Ermak 76; 776H1952 28.1 84; Elegechevo 1281H1120 776 Dubovka / Koshkulsky H2000 102 1322 Barkhan / Koshkulsky H1123 / Koshkulsky Asino 92 195H1461 / Novomikhaylovsky Voronovo H3048 195 41 / Altymsky Trubachovo H4771 Pudino / Altymsky H3434 64 41 / Novomikhaylovsky Pozdnjakovo 43H1687 82 / Novomikhaylovsky Obuhovka H4601 / Novomikhaylovsky Novokolpakovo 82 154 154 H1939 13.3 Zakharov H3521 / Basandaysky Tomsk 16.4 –0.1 6.2 24.9 26.2 776 1281 103 174 41 83 82 107 H2030 / Burdigalian rechka Berezovaja

333 PALAEOCLIMATE OF SIBERIA FROM THE OLIGOCENE TO PLIOCENE 66; 5771; 55 9.183; 60 10.684; 56 14.7 14.7 9.576; 59 –2.7 –2.8 9.1 11.6 4.4 13.3 6.482; 57 –0.1 21.3 18.9 18.784; 56 21.5 –2.7 24.6 0.2 13.3 –0.1 24.680; 59 13.3 592 21.9 12.5 12.3 413 16.580; 59 18.9 1355 24.6 19.6 1400 –0.1 28.6 15.7 9.383; 57 776 103 26.1 13.3 592 –0.1 6.4 14.7 864 108 592 1520 14.7 9.3 6.465; 57 24.9 –1.6 1281 168 116 –0.1 27.4 24.9 6.8 13 103 168 11.1 776 26.2 6.8 103 21.5 –2.7 24 1281 776 177 21.9 13 24.6 24 195 2.8 1520 24.6 843 –0.1 195 116 43 21.6 776 32 1400 43 2.8 103 22 24.6 1146 22 78 21.9 592 180 122 32 108 43 24.6 108 1400 174 43 1146 83 108 41 154 195 103 1281 78 32 139 58 43 141 131 41 107 168 43 32 83 82 43 168 24 82 43 107 78 53 43 108 120 64 83 78 172 85 95 95 2 2 2 2 2 2 2 1 2 2 2 H914 / Novomikhaylovsky Antropovo H2642 / Altymsky tavda Nizhnya H1940 Ekaterininskoe 74; 5613.3H3196 / Novomikhaylovsky Lebyazh’e H4148 14.7 / Novomikhaylovsky bor Kompasskiy H3424 0.9 / Novomikhaylovsky Kolarovo 5412.1H1436 6.2 / Novomikhaylovsky Katyl’ga H1940 21.9 74; Ekaterininskoe H1269 24.6 14.7 / Basandaysky Chumakaevka H2029 979 –1.1 / Novomikhaylovsky rechka Berezovaja H4768 1281 / Novomikhaylovsky Amelich 6.4H4770 / Altymsky Amelich 21.9 106H3426 24.6 Ambartsevo / Novomikhaylovsky H1289 776 73; Achair 168 1322 41 150 43 195 90 32 95 41 120 141

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