Pleistocene loess-soil sequence and aeolian relief of Western Siberia: chronology and features of their formation

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The article discusses the current state of chronostratigraphy and paleogeography of the loess-soil sequence of the Pleistocene of Western Siberia, which is one of the most complete in Northern Eurasia. It is shown that genetically loess is closely related to eolian formations formed as a result of activation of eolian processes in earlier arid epochs of the Late Cenozoic in North Asia. A deflationary and accumulative eolian relief, paragenetically associated with the formation of the subaerial formation, is described, showing a slight transfer of material that forms the loess stratum. It has been established that the eolian relief and the activation of eolian processes occurred during the cold periods of the Pleistocene with the predominance of southwestern winds. The basis of the stratigraphic subdivision and correlation of sections of the loess strata are fossil soils formed under strictly defined climatic conditions. Consistent tracking of the loess and soil horizons of the loess sequence of the Pleistocene of Western Siberia, taking into account radiocarbon and luminescent dating and the use of climatostratigraphic correlations, showed that its structure and composition clearly reflect the uniqueness of each paleogeographic epoch, associated with changes in the intensity of atmospheric circulation in the cold and warm epochs of the Pleistocene. The features of each specific epoch are recorded in a combination of unique individual features of certain horizons of the loess-soil sequence. In the alternating horizons of loesses and soils, a record of global and regional changes in landscapes and climate has been preserved, reflecting the originality and uniqueness of the paleogeography of each time epoch. The structure and composition of the loess strata reflect the different intensity of atmospheric circulation during the cold and warm epochs of the Pleistocene. It is shown that the chronological sequence of the loess-soil sequence of Western Siberia, based only on OSL dates, does not always coincide with the loess-soil sequence of Western Siberia, built on the integration of various approaches, with the predominant use of the paleopedological method, and therefore needs to be corrected. The best correlation results are achieved by combining all available dating methods with the involvement of biostratigraphic, sedimentological and geological data, based on the climatostratigraphic principle.

Sobre autores

V. Zykina

Sobolev Institute of Geology and Mineralogy, SB RAS; Institute of Geography RAS

Autor responsável pela correspondência
Email: zykina@igm.nsc.ru
Rússia, Novosibirsk; Moscow

V. Zykin

Sobolev Institute of Geology and Mineralogy, SB RAS; Institute of Geography RAS; Novosibirsk State University

Email: zykina@igm.nsc.ru
Rússia, Novosibirsk; Moscow; Novosibirsk

E. Malikova

Sobolev Institute of Geology and Mineralogy, SB RAS

Email: zykina@igm.nsc.ru
Rússia, Novosibirsk

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2. Fig. 1. Stratigraphic scheme of the loess-soil sequence of the Pleistocene of Siberia (Zykina, Zykin, 2012, with refinement). Soil horizons: 1 — humus soil horizons, 2 — illuvial soil horizons; 3 — cryogenic formations; 4 — loess; 5 — stage warming; 6 — colder and shorter than the Holocene; intervals: 7 — interval having 14C date, 8 — interval having luminescent dates; ПК — pedocomplex; Л — loess.

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3. Fig. 2. Deflationary relief of the time of the last glaciation in the western part of the Kulunda Plain with a large number of small rounded basins blown by the wind and filled with water in Holocene (source: ArcGIS Earth).

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4. Fig. 3. Crescent-shaped, transverse to the prevailing winds, eolian ridges (grivas) on the lee shores of lake basins, composed of material taken out of them, and a longitudinal griva on the southeastern shore of the Lake Sargul.

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5. Fig. 4. The grivas relief of the Chany depression of the time of the last glaciation, composed of low longitudinal ridges (grivas) to the southwest winds.

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6. Fig. 5. Geological section of the southeastern flank of the Chany Lake basin. 1 — loam; 2 — solifluction deposits; 3 — sand; 4 — silt; 5 — ice wedge casts; 6 — buried soil; 7 — aeolian deposits; 8 — lacustrine deposits.

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7. Fig. 6. Digital elevation model of the Uvals of the Priobskoye Loess Plateau. Ouvals (local name for crests) are ridges elongated in a straight line from the southwest to the northeast, almost parallel to each other (outlined by the red line). The length of the ouvals reaches 120—350 km, and the width is from 15 to 70 km. They are separated by wide rectilinear hollows from 8 to 20 km wide; relative height of ouvals above hollows is from 5 to 100 m. The map is based on SRTM DEM with 30 m resolution (source: https://opentopography.org/) and was designed in ArcGIS Pro.

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8. Fig. 7. Geological structure of the Belovo section (Zykina, Zykin, 2012). 1 — loam; 2 — sandy silt; 3 — sandy loam; 4 — sand; 5 — indistinctly layered sand; 6 — fossil soil; 7 — locations of transects; pedocomplexes: 8 — Shadrinsky, 9 — Charyshsky, 10 — Volodarsky, 11 — Belovsky, 12 — Evsinsky, 13 — Iskitimsky, 14 — Koinikhinsky, 15 — Berdsky.

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9. Fig. 8. Structure of the lower soil of the Berdsk pedocomplex (MIS5e): (а) — Toguchin Quarry, (б) — Lozhok Quarry. Loam: 1 — strongly humusified loam, 2 — moderately humusified loam, 3 — slightly humusified loam, 4 — loess-like loam; burrows of shrews: 5 — filled with loess-like loam, 6 — filled with humusified loam; 7 — cracks of desiccation; 8 — pseudomycelium and spots of white-eye weevil; 9 — vertical fracturing; 10 — rubble.

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10. Fig. 9. Correlation of sections of the loess-soil sequence of the Pleistocene of the Novosibirsk region. Soil horizons: 1 — soil humus horizons, 2 — illuvial horizon; 3 — silt; 4 — sandy silt; 5 — Mn spots; 6 — carbonates (а) and carbonate concretions (б); 7 — neoplasms of iron; 8 — gleying; 9 — drying cracks (а) and humus streaks (б); 10 — Fe–Mn concretions; 11 — fine crushed stone and slate plates; 12 — gravel; 13 — krotovinas; 14 — weathering crust; 15 — limestone.

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11. Fig. 10. Structure of the lower soil of the Iskitim pedocomplex (MIS 3) in the Lozhok quarry. For the symbols, see fig. 8.

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