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Paleoenvironment. the Stone Age

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Paleoenvironment. the Stone Age 2 PALEOENVIRONMENT. THE STONE AGE E.V. Bezrukova1, D.G. Anderson2, O.P. Vinkovskaya3, A.V. Kharinsky4, and N.V. Kulagina5 1Irkutsk Laboratory of Archaeology and Paleoecology, Institute of Archaeology and Ethnography, Siberian Branch, Russian Academy of Sciences, Favorskogo 1A, Irkutsk, 664003, Russia E-mail: [email protected] 2Department of Anthropology, University of Aberdeen, Aberdeen AB24 4QY, United Kingdom E-mail: [email protected] 3Irkutsk State Agricultural Academy, Molodezhnii1/1, Irkutsk, 664036, Russia E-mail: urbanofl [email protected] 4Irkutsk State Technical University, Lermontova 83, Irkutsk, 664074, Russia E-mail: [email protected] 5Institute of the Earth’s Crust, Siberian Branch, Russian Academy of Sciences, Lermontova 128, Irkutsk, 664033, Russia E-mail: [email protected] VEGETATION AND CLIMATE CHANGES IN THE BOLSHOE INYAPTUKSKOE LAKE BASIN (NORTH BAIKAL PLATEAU) IN THE MIDDLE AND LATE HOLOCENE This article presents new interdisciplinary observations relating to environmental changes in the Bolshoe Inyaptukskoe Lake Basin, North Baikal Plateau. A column taken from a loam/turf deposit at 1320 m above sea level is shown to refl ect changes in vegetation and climate over the last 8–9 thousand years through its palynology, radiocarbon chronology, and the count of charcoal particles. The chronology of the reconstructed changes in the vegetation around the Ozernyi-5 trench agrees well with existing regional and global climatic trends. However, the local processes also show their own peculiarities. The discrepancies are associated with the elevation and the altitude of the site. Keywords: Siberia, North Baikal Plateau, high resolution pollen record, vegetation and climate changes, Middle Holocene, Late Holocene. Introduction the Holocene and responded to them rather rapidly (Bezrukova, 1999; Demske et al., 2005; Tarasov et al., It is well known that the vegetation of the Baikal region, 2007; Tarasov, Bezrukova, Krivonogov, 2009). It has which includes the North Baikal Plateau, was highly been also demonstrated that climatic changes in this susceptible to global and regional climate changes during territory occurred almost synchronously with the climate 3 oscillations of the Northern Hemisphere (Prokopenko average annual precipitation exceeds 500 mm while in the et al., 2010). Until recently, no continuous, dated, high intermontane basins, it is 300–350 mm. The thickness of resolution pollen records of environmental changes have snow cover fl uctuates markedly: from 20–30 cm to 180– been obtained for the mountainous part of the North 200 cm in areas near Lake Baikal. The main air currents are Baikal Plateau. This region presents itself as a large inland western. In summer and autumn, the effect of northwestern system of medium-sized mountains and fl at-topped ridges winds increases. The North Baikal Plateau is situated in the with contrasting relief, fl ora, and climate, and a complex zone of discontinuous permafrost (Baikal…, 1993). glacial history. The diversity of plant communities on the North This article presents the fi rst results of palynological Baikal Plateau is determined by zones which vary by study of loose mineral and organic (peat) sediments from altitude. Mountain taiga (larch and pine-larch forests), the basin of Lake Bolshoe (Great) Inyaptukskoe located subalpine (larch forests with dark conifers and Siberian on the North Baikal Plateau. The results are unique for dwarf pine), and mountain tundra zones are characteristic the region due to the fi ne-grained selection of samples of this region (Zony…, 1999). which makes it possible to read pollen changes with a The Ozernyi-5 trench was placed within the subalpine 180 year resolution on average. Such detailed information larch forest belt in the Olokit River valley, near Bolshoe makes it possible to trace environmental variations Inyaptukskoe Lake (Fig. 1). The valley fl oor consists beyond the regional level, to trace local vegetation of a wetland covered with dwarf birch and tussock changes (Kuoppamaa, Goslar, Hicks, 2009; Schlütz, meadows. The slopes of the southern and western valleys Lehmkuhl, 2007), and to establish the causes of these are covered by subalpine larch open woodlands with changes as either climatic or anthropogenic. The impact dark conifers and Siberian dwarf pine (Fig. 2). Alpine of anthropogenic factors is not analyzed in full here. tundra plant communities (primarily, dwarf birch with Instead we focus on the way that major climatic changes were manifested in a peculiar way in mountainous areas. 0 40 km Description of the study area The Ozernyi-5 trench (56°22′49.1″ N; 109°54′09.0″ E) was located at the northeastern foothills of the Synnyr Ridge in the central portion of the North Baikal Plateau – a part of the Baikal Mountains lying between the Stanovoi Highland and the Lena and Vitim river valleys. The highest peak of the North Baikal Plateau is Mount Inyaptuk; it reaches 2578 m asl. Bolshoe Inyaptukskoe Lake lies 10 km west of the peak. In the 19th–20th centuries, a camp of Evenki reindeer-herders was situated on its western shore; and in the mid-20th century, a settlement of geologists was built there (Kharinsky, 2010). The Ozernyi-5 trench was dug on the northeastern periphery of the former reindeer-herding camp, 370 m from the lake shore. This region has a continental climate. The annual temperature varies from –5 to –12 °С and the winters are cold and long. Temperatures in January average –30 °С. The daily temperature drops below zero until May. Summers are short and moderately warm. At the elevation of 500– 600 m, the mean July temperature does not exceed +14 °С, while the growing season lasts for less than 90 days (Atlas…, 1967). Most precipitation falls in July and August as well as in the first half of the autumn. In mountainous areas, the Fig. 1. The location of the Ozernyi-5 trench. 4 Pollen analysis. One sample was taken from every centimeter of the column creating an archive of 50 samples. To extract pollen and spores in the laboratory, 1 cm3 of undried sediment from each layer Ozernyi-5 was processed using a standard process using hydrofluoric acid followed by acetolysis (Faegri, Iversen, 1989). Before the start of the procedure, two tablets of Lycopodium clavatum marker spores (18,584 grains per tablet) were added to each sample in order to control the pollen concentration (Maher, 1981). Pollen grains and spores were counted until either their total number, or the quantity of the Lycopodium markers reached 1000. The count of naturally-occurring Lycopodium spores was excluded from these totals. The relative percentage of all pollen-bearing Fig. 2. Bolshoe Inyaptukskoe Lake from the southwest. taxa was calculated relative to the total count of pollen coming from terrestrial species. The percentages of spores from lichen) are more pronounced on the northern and eastern fern, moss, and club moss were calculated relative to slopes. Vegetation near the Ozernyi-5 trench is part of the total count of both pollen grains and spores in each the valley wetland system with hummocks covered by sample. At the same time, the number of charcoal particles ground birch (Betula rotundifolia Spach), isolated larches was counted from the same prepared samples. The counts (Larix dahurica Laws.), juniper (Juníperus communis L.), of each charcoal microparticle were calibrated to the size golden rhododendron (Rhododendron aureum Georgi), of 30 microns in diameter (the approximate size of a grain bilberry (Vaccínium uliginosum L.), white arctic mountain of the Lycopodium clavatum marker) (Innes, Blackford, heather (Cassiope tetragona (L.) D. Don), crowberry Simmons, 2004). We did not carry out an inventory of (Empetrum sibíricum V.N. Vassil.), and lingonberry different sizes of charcoal. (Vaccínium vítis-idaea L.). Lichen grows above the soil AMS dating. Two bulk AMS dates were obtained surface of hummocks. Hollows between the hummocks from samples taken from the depths of 19 and 32 cm at the are occupied by willows (Salix arctica Pall., S. bebbiana Ångström laboratory at Uppsala University in Sweden. Sarg., S. coasia Vill., S. divaricata Pall., and others) The fi rst was taken from the bottom of the layer composed and by tussocked cotton grass or grassy sedge bogs on of light gray loam. The second, from an isolated black permafrost-affected meadow soil. loam layer. The uncalibrated radiocarbon dates for these samples are 5935 ± 36 (Ua-38926) and 7005 ± 40 (Ua-38927), respectively. The dates when calibrated Materials and methods using CalPal software give the values of 6764 ± 50 (68 % confi dence limit: 6713–6814 calibrated years) and The trench was dug near Ozernyi, an abandoned 7858 ± 56 (68 % confi dence limit: 7801–7914 calibrated settlement built by geologists, at an elevation of 1320 m years) (Danzeglocke, Joris, Weninger, 2011). Only the asl in the Olokit River valley. The trench was 50 cm deep calibrated dates are cited from this point forward. and was composed primarily of loam sediments with turf The alternation of light and dark conifer taxa. in its upper part. A damp site was chosen near to an alpine Light conifers are represented by Pinus sylvestris and lake with the expectation that it would better preserve a Larix. The group of dark conifers includes Pinus sibirica, local pollen signature. Further, the trench was placed near Abies sibirica, and Picea obovata. Given the different a camp once used by reindeer-herders with the hope that ecological (edaphic and climatic) needs of these two we would pick up a signature of pollen associated with groups of arboreal species, changes in the counts of their the concentration of a large number of domestic animals pollen are thought to point to changes in the continental once held there. This methodology of site selection was climate (Bykov, 1960; Koropachinsky, Vstovskaya, developed in Scandinavia, where pollen samples are taken 2002). This is usually interpreted as a change in the 6–50 m away from a geoarchaeological object (Aronsson, relative humidity or as a change in the difference between 1991; Räsänen, Froyd, Goslar, 2007).
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