Provenance changes of the holocene deposits of Oga and Tsivolki bays (Novaya Zemlya archipelago) according to SR, ND, PB isotope data

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The paper is devoted to the Sr-, Nd-, Pb-isotope data obtained for two cores of bottom sediments taken in the Oga and Tsivolki bays of the Severny Island of the Novaya Zemlya archipelago. The studied sequence of sediments from Oga Bay has been accumulated over the last thousand years. The 87Sr/86Sr ratio decreases from top to bottom down the section from 0.72225 to 0.71995, the value of εNd varies from –6.1 to –5.5. The Pb isotopic composition varies within narrow limits: the 206Pb/204Pb ratio from 19.107 to 19.139, the 207Pb/204Pb ratio from 15.632 to 15.635, and the 208Pb/204Pb ratio from 38.568 to 38.635. A rapid decrease in the 87Sr/86Sr ratio at a relatively stable neodymium and lead isotope composition indicates a change in the source of the clastogenic material. This can be explained by the fact that the material of the destruction of Permian clay shales, and then the Devonian-Silurian sedimentary carbonates, first entered the area of glacier abrasion and further, respectively, into the sedimentation zone.

The sediment column from the Tsivolki Bay was formed over a little more than 10 thousand years. Based on the Sr, Nd, and Pb isotope ratios, these bottom sediments are divided into lower and upper parts: before and after 150 cm (or ~3500 years). In the lower part of the column, the 87Sr/86Sr ratio increases from 0.72055 to 0.72580, the value of εNd remains approximately the same and varies around –8.2. In the upper part, the 87Sr/86Sr ratio drops to 0.72049 in the near-surface layer; at the same time, the value of εNd increases to –6.4. At the boundary of these two units, the 206Pb/204Pb ratio abruptly changes from about 18.0 in the lower part to 19.3 in the upper part and 208Pb/204Pb from about 36.5 in the lower part to 38.7 in the upper part of the section. The change in the Sr, Nd, and Pb isotope characteristics is likely a reflection of changes in the composition of the rocks in the area where the basin was removed, which is now being eroded by the glacier.

Comparison with modern sources supplying clastic material to the Kara Sea showed that the material inputs the Oga and Tsivolki bays only from Novaya Zemlya.

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I. Vishnevskaya

Vernadsky Institute of Geochemistry and Analytical Chemistry (GEOKHI) RAS

编辑信件的主要联系方式.
Email: vishnevskaia@geokhi.ru
俄罗斯联邦, Kosygina str., 19, Moscow, 119334

Y. Kostitsyn

Vernadsky Institute of Geochemistry and Analytical Chemistry (GEOKHI) RAS

Email: vishnevskaia@geokhi.ru
俄罗斯联邦, Kosygina str., 19, Moscow, 119334

T. Okuneva

Zavaritsky Institute of Geology and Geochemistry UB RAS

Email: vishnevskaia@geokhi.ru
俄罗斯联邦, Akademika Vonsovskogo str.,15, Ekaterinburg, 620016

N. Soloshenko

Zavaritsky Institute of Geology and Geochemistry UB RAS

Email: vishnevskaia@geokhi.ru
俄罗斯联邦, Akademika Vonsovskogo str.,15, Ekaterinburg, 620016

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2. Fig. 1. Sampling location. (a) The position of the Novaya Zemlya archipelago in the waters of the Arctic Ocean. (b) The area of work, the blue arrows show near-surface currents (Gorshkov et al., 1980, source of the IBCAO map). (c) Sampling points in the bays of Oga (AMK-5248) and Tsivolki (AMK-5251) are shown with asterisks.

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3. Fig. 2. Distribution of Sr content and isotope ratios of Sr, Nd, Pb in the column of sediment AMK-5248 (Oga Bay). Circles indicate samples from warm stages, triangles – from cold ones, the measurement error (±2σ) is indicated by horizontal risks for the ratio 207Pb/204Pb, in other cases it does not exceed the size of the sign.

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4. Fig. 3. Diagrams of paired ratios of isotopic compositions of Sr, Nd, Pb and Sr content for rocks from the Oga Bay. The dotted line marks the intended boundary between the lower and upper parts of the section, the same divisions are marked by trend lines and an oval. Circles indicate samples from warm stages, triangles – from cold ones, numbers on graphs – sample numbers, measurement error (±2σ) is indicated by horizontal and vertical risks, where there is no sign, it does not exceed the size of the sign.

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5. Fig. 4. Distribution of Sr content and isotopic compositions of Sr, Nd, Pb in the AMK-5251 column (Tsivolki Bay). The arrows show the trends of changes in compositions, the dotted line shows the boundary of the change of the demolition source. The measurement error (±2σ) is indicated by horizontal risks in cases where it exceeds the size of the sign.

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6. Fig. 5. The position of the samples from the Gulf of Tsivolka in coordinates (a) the content of Nd–eNd, (b) 87Sr/86Sr– eNd (the dotted line separates the horizons located above and below the boundaries of the divisions proposed in the text), and (c) 206Pb/204Pb–208Pb/204Pb. The graphs show that the precipitation of the upper and lower parts of the section occupy different fields. This is a clear indication of the change of rocks at the source of the demolition.

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7. Fig. 6. Mineral composition of sediments from the cores of the Oga Bay (squares) and segments (circles), data taken from (Rusakov et al., 2022a, b), Ill – illite, Cl – chlorite, Kl – kaolinite.

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8. Fig. 7. Evolution of the Sr isotopic composition over time for the assumed source (solid line) of sedimentary rocks (a) of the Oga Bay and (b) of the Tsivolki Bay of the Novaya Zemlya archipelago.

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9. 8. Isotopic composition of sediments of the Oga and Tsivolka bays in comparison with probable sources of demolition in coordinates (a) eNd –87Sr/86Sr and (b) 208Pb/206Pb–206Pb/204Pb. Data for sediments from different provinces are taken from the following works: the southeastern coast of Novaya Zemlya and Svalbard (Tütken et al., 2002), the Yenisei and Ob Rivers (Guo et al., 2004; Schmitt, 2007), the North Pole (Eisenhauer et al., 1999), East Siberian sea, Kara sea, sea Laptev, Barents Sea, Fram Strait, Mackenzie River and the Canadian Arctic (Maccali et al., 2018), Lena River (Millot et al., 2004), Lomonosov Ridge (Stevenson et al., 2015), Beaufort Sea (Gartside, 1996); basalts Siberian trap province (Lightfoot et al., 1992; Wooden et al., 1993).

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