Loess-paleosol sequences in the East European Plain and Western Siberia make up a largest part of Eurasian loess belt. In Eastern Europe, loesses represent an almost continuous massif, extending from the Black and Azov Seas to the Ural Mountains, while loess sediments of Western Siberia make up the northeastern part of the Eurasian loess belt, separated from its European part by the Ural Mountains. Due to the flatness of the territory, loess sediments in Eastern Europe and Western Siberia have comparable stratigraphy and are well correlated between various sections, reflecting similar climatic trends. The composite stratigraphy comprises 14 pedogenetic levels in the loess-paleosol sequences of European Russia, including the surface soil, separated by 14 loess layers within the Brunhes Chron and 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19). The composite stratigraphy of LPS in Ukraine is somewhat similar, with 11 pedogenetic levels in the Brunhes Chron, 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19), and 1 within the Matuyama Chron. The composite loess-paleosol stratigraphy of Western Siberia comprises 11 pedogenetic levels, including the surface soil, separated by 9 loess layers within the Brunhes Chron, 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19), and 1 within the Matuyama Chron (MIS 21). Loess-paleosol cyclicity arose ca. 1.2 Ma. Pedogenetic levels are related to warm phases (interglacials or interstadials). Loess layers, corresponding to cold and dry phases, are considerably thicker than pedogenetic levels. Climatic oscillations determined the formation of two or three soils within most warm intervals, presented as composite paleosols or pedocomplexes. A succession of interglacial, interstadial, and pleniglacial soils formed during Pleistocene glacial-interglacial macrocycles was determined by differences in heat and moisture supply, pedogenic processes, and sedimentation rate. Interglacials are characterized by well-developed soils and a clear zonal pattern, with forest soils in the northern part of the loess belt and steppe soils in the south. In complete LPS zonal pattern is characteristic of all interglacials in the middle and late Pleistocene. Interstadials exhibit hyperzonality with a simplified zonal pattern. Stagnic Cambisols, enriched in secondary carbonates and influenced by cryogenesis, were the dominant soils during interstadials. Glacials didn’t completely exclude pedogenesis; the cold climate and the prevalence of sedimentation on pedogenesis resulted in the development of incipient synlithogenic soils.

Loess-Paleosol Sequences in the East European Plain and Western Siberia

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发表日期：

2026年

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Alexander Makeev

摘要

Loess-paleosol sequences in the East European Plain and Western Siberia make up a largest part of Eurasian loess belt. In Eastern Europe, loesses represent an almost continuous massif, extending from the Black and Azov Seas to the Ural Mountains, while loess sediments of Western Siberia make up the northeastern part of the Eurasian loess belt, separated from its European part by the Ural Mountains. Due to the flatness of the territory, loess sediments in Eastern Europe and Western Siberia have comparable stratigraphy and are well correlated between various sections, reflecting similar climatic trends. The composite stratigraphy comprises 14 pedogenetic levels in the loess-paleosol sequences of European Russia, including the surface soil, separated by 14 loess layers within the Brunhes Chron and 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19). The composite stratigraphy of LPS in Ukraine is somewhat similar, with 11 pedogenetic levels in the Brunhes Chron, 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19), and 1 within the Matuyama Chron. The composite loess-paleosol stratigraphy of Western Siberia comprises 11 pedogenetic levels, including the surface soil, separated by 9 loess layers within the Brunhes Chron, 1 pedogenetic level inside the Brunhes/Matuyama paleomagnetic reversal (MIS 19), and 1 within the Matuyama Chron (MIS 21). Loess-paleosol cyclicity arose ca. 1.2 Ma. Pedogenetic levels are related to warm phases (interglacials or interstadials). Loess layers, corresponding to cold and dry phases, are considerably thicker than pedogenetic levels. Climatic oscillations determined the formation of two or three soils within most warm intervals, presented as composite paleosols or pedocomplexes. A succession of interglacial, interstadial, and pleniglacial soils formed during Pleistocene glacial-interglacial macrocycles was determined by differences in heat and moisture supply, pedogenic processes, and sedimentation rate. Interglacials are characterized by well-developed soils and a clear zonal pattern, with forest soils in the northern part of the loess belt and steppe soils in the south. In complete LPS zonal pattern is characteristic of all interglacials in the middle and late Pleistocene. Interstadials exhibit hyperzonality with a simplified zonal pattern. Stagnic Cambisols, enriched in secondary carbonates and influenced by cryogenesis, were the dominant soils during interstadials. Glacials didn’t completely exclude pedogenesis; the cold climate and the prevalence of sedimentation on pedogenesis resulted in the development of incipient synlithogenic soils.