The loess-soil sequence of the Central Ciscaucasia: chronostratigraphy, composition, and sedimentation conditions during the late neopleistocene

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The study presents the results of sedimentological investigation of the core recovered from from the Pervomayskaya-1 (Pm-1) borehole, which revealed the most complete structure of the upland loess-soil series (LSS) in the central Pre-Caucasus. The borehole reached a depth of 13.8 m. Luminescence dating for two samples from the core yielded ages of 62±3 and 102±7 thousand years, attributing the entire studied sequence to the Upper Neopleistocene. Lithostratigraphic units were identified based on macroscopic core examination and geochemical analyses. The Mezin pedocomplex (13.8–9.1 m, MIS 5) consisting of three paleosols was identified at the base of the section. Above it lies a horizon of Valdai loess (9.1–1.2 m, MIS 4–2) of substantial thickness with weak signs of interstadial pedogenesis in its middle part. The section is capped by a Holocene chernozem (1.2–0.0 m, MIS 1) showing signs of anthropogenic transformation in its upper profile. The LSS structure revealed in the Pm-1 core shows stratigraphic unity with previously dated reference sections and boreholes of the Pre-Caucasus LSS: Beglitsa (Bg), Vorontsovka-4 (V-4), Sladkaya Balka-1 (Sb-1), and Otkaznoye-20 (Ot-20). Moreover, the Pm-1 column fits within the main trend of increasing loess thickness and grain size from west to east across the Pre-Caucasus. For the Pm-1 and Ot-20 columns, consistent variations in magnetic susceptibility and grain size were identified. Using these consistent variations as chronostratigraphic markers allowed for a more detailed depth-age model for Pm-1. Based on this model, estimates of loess accumulation rates for the Late Neopleistocene and Holocene were calculated: maximum rates (15.9–17.5 cm/thousand years) correspond to the interval of 36–16 thousand years ago; elevated rates (11.4–12.5 cm/thousand years) align with the interval of 80–40 thousand years ago; low rates (9.1–10.4 cm/thousand years) were recorded in the interval of 128–81 thousand years ago; minimal rates (6.0–6.6 cm/thousand years) correspond to the interval of 13–5 thousand years ago. The intensity of loess accumulation in Pm-1 shows consistency with the most complete LSSs of Eastern Europe, as well as with the mineral dust concentration in Greenland ice core NGRIP.

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N. Sychev

Institute of Geography RAS

编辑信件的主要联系方式.
Email: nvsychev25@igras.ru
俄罗斯联邦, Moscow

E. Konstantinov

Institute of Geography RAS

Email: nvsychev25@igras.ru
俄罗斯联邦, Moscow

A. Zakharov

Institute of Geography RAS

Email: nvsychev25@igras.ru
俄罗斯联邦, Moscow

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2. Fig. 1. Location of the research objects: (a) – Location of the reference boreholes of the Central and Eastern Ciscaucasia: Pervomayskaya-1 (Pm-1), Otkaznoye-20 (Ot-20), Sladkaya Balka-1 (Sb-1); (б) – Topography of the Ciscaucasia and the northern macroslope of the Stavropol Upland (topographic basis – digital elevation model SRTM); (в) – Terrain in the area of the Pm-1 borehole (Google Earth satellite image, 2022).

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3. Fig. 2. Structure and analytical characteristics of the loess-paleosoil series in the Pervomaiskaya core 1 (Pm-1): χlf – low-frequency magnetic susceptibility; FD – frequency-dependent magnetic susceptibility; ГС – granulometric composition; ППП – loss on ignition; L* – color brightness (lightness) negative values show black, positive – white; a* – red vs. green, where negative values indicate green and positive values indicate red; b* – yellow vs. blue, where negative values indicate blue and positive values indicate yellow; Stratigraphic horizons according to (Velichko, Morozova, 2010): Hol – Holocene soil, Br – Bryansk paleosol, MzKr – Mezin pedocomplex, Krutitsa paleosol, MzSl – Mezin pedocomplex, Salyn paleosol. Grain size, µm: 1 – <2, 2 – 2–4, 3 – 4–8, 4 – 8–16, 5 – 16–31, 6 – 31–63, 7 – 63–125, 8 – 125–250, 9 – 250–500; coloring and symbols on the lithologic column: 10 – horizons of “pure” loess, 11 – anthropogenically processed ground, 12 – mature soil with a full profile, 13 – ephemeral developed soil, 14 – carbonate concretions, 15 – gypsum concretions, 16 – luminescent dates in ka.

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4. Fig. 3. Correlation scheme of the columns Sladkaya Balka-1 (Sb-1) (Mazneva et al., 2021; Konstantinov et al., 2022, with modifications), Pervomayskaya-1 (Pm-1) (authors’ data) and Otkaznoye-20 (Ot-20) (Sychev et al., 2022; Konstantinov et al., 2022). МРЧ – median grain size (MGS); χlf – low-frequency magnetic susceptibility; Hol – Holocene soil, Br – Bryansk paleosol, MzKr – Krutitsa paleosol, MzSl – Salyn paleosol. 1 – technozem; 2 – loess horizons; 3 – developed soils with a full profile; 4 – levels of ephemeral soil formation; 5 – luminescent dates in ka; 6 – correlation markers (corresponds to the ordinal number in tab. 1).

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5. Fig. 4. Bayesian depth-age model of the Pm-1 core. 1 – simulated dates obtained by matching variations in grain size distribution and magnetic susceptibility between the Pm-1 and Ot-20 cores; 2 – simulated dates obtained by correlating stratigraphic unit boundaries between the Pm-1 and Ot-20 cores; 3 – direct luminescence dates; 4 – simulated dates obtained by correlating stratigraphic unit boundaries and marine isotope stages using the LR-04 model; 5 – direct luminescence dates corrected for 100% water saturation. The red dotted line is the mean value of the model age, the gray dotted line is the boundaries of the 95% confidence interval.

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6. Fig. 5. Changes in the main sedimentological characteristics of the Pervomayskaya-1 (this study) and Otkaznoye-20 (Sychev et al., 2022) cores at the end of the Quaternary. МРЧ – median grain size (MGS); П – sand content; ТО – average sedimentation rate; Г – clay content; FD – frequency dependence of magnetic susceptibility.

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