extended abstracts - Geomorphic Processes and Geoarchaeology

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Geomorphic processes and geoarchaeology Figure 1. Stratigraphy and chronology of Kostenki-14 section Figure 2. Distribution of micromorphological features (right) and some palynologacal characreristics (left; after [2]) in Kostenki 14 241
Geomorphic processes and geoarchaeology The group of Upper Paleolithic sites at Kostenki, located in the Central Russia, some 40 km south of Voronezh is known as one of the earliest localities with the evidences of modern humans occupation in the Eastern European Plain [1]. In the profile Kostenki-14 nine cultural layers in the chronological frameworks of 22-42 nonCal. ka were identified within a colluvial sequence of the slope at the second terrace of a minor valley – right tributary of river Don. Thick Holocene Chernozem is underlain by the Late Pleistocene slope deposits intercalated with 5 paleosol units labeled K14-I to K14-V (fig. 1). Paleosols are thin and formed by rapid pedogenetic processes (humus accumulation; development of structure due to cryogenic and biogenic aggregation; cryogenic redistribution of skeletal material; precipitation of secondary calcite; gleyzation) both due to rather short formation intervals and severe climatic conditions during the Last Glaciation. Lower paleosols have more abundant redoximorphic features which require excessive moisture whereas upper ones have more abundant neoformed carbonates indicative of drier environment. These tendencies fit well to the decrease of tree pollen and increase of grasses towards the upper part of the profile. Thus the distribution of pedogenetic features in different units provide a local paleoecological proxy correlative with the paleobotanical record. The paleosols of the unit K14-II formed between ~ 28 and ~ 32 ka BP demonstrates stronger profile development and abundance of organic materials, biogenic aggregates as well as diversity of calcitic pedofeatures. Advanced decomposition of plant residues and accumulation of colloidal humus, together with the signs of intensive bioturbation and strong maximum of magnetic susceptibility cast doubt on the earlier hypothesis of hydromorphic origin of this paleosol. Instead we suppose pedogenesis in a drained soil environment, under cool meadow-steppe ecosystem, having modern analogues in the cryo-arid soils of Eastern Siberia (for details see [3]). A Figure 3. Micromorphology of paleosols. A: zoogenic structure in Ah horizon of PK14- IIb paleosol; B: ash inclusions (upper left) in PK14-III paleosol. Plain Polarized Light The K14-III paleosol unit is associated with the layer of volcanic ash (probably Campanian Ignimbrite, deposited ~ 40 ka BP. The microscopic observation demonstrated that the soil is developed in the local sediments whereas pyroclastic material is very poorly integrated in the matrix and not transformed by pedogenesis; implying that the ash was deposited at the final stage of the paleosol development. B 242
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ISBN 978-5-91412-129-9 Geomorphic P
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A Figure B 2. 3. Zwięczyca Lithic
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Ghahroudi Tali M. 13, 102 Giligny F
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Volokitin A.V. 281 Voronin K.V. 76
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