Cretaceous–eocene flysch of the sochi synclinorium (western caucasus): sources of clastic material based on the results of U–Th–Pb isotope dating of detrital zircons

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Abstract

The first results of U–Th–Pb isotope dating of detrital zircons (dZr, N = 130, n = 91) from the Middle Danian sandstones (63.9–65.3 Ma) of the Cretaceous–Eocene Novorossiysk–Anapa flysch, widely developed in the Sochi synclinorium (Southern slope of the Western Caucasus) are presented. The maximum dZr age is 2973 ± 12 Ma, the minimum dZr age is 318 ± 3 Ma; weighted average age of the 4 youngest dZr ~ 322 ± 7 Ma. There are no signs of the destruction products of the Jurassic magmatites involved in the structure of the Greater Caucasus and the Crimean Mountains into the sedimentary basin, in which the Novorossiysk-Anapa flysch was formed. A high degree of similarity between the provenance signals of the Danian sandstones from the Novorossiysk-Anapa flysch, some Paleogene-Neogene and Early Quaternary (Early Pleistocene) sandstones of the Western Caucasus and Western Cis-Caucasia, red-colored Upper Permian and Lower Triassic sandstones of the Moscow syneclise, as well as Late Quaternary alluvium of the lower reaches of the draining vast expanses of the Russian plate Don and Volga rivers has been revealed. On this basis, it was concluded that in the Middle Danian there were no eroded mountain structures of the Greater Caucasus and Crimea, and the main volume of detrital material composing the Novorossiysk-Anapa flysch was formed due to the recycling of Permian-Triassic and younger strata of the Russian Plate.

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About the authors

N. B. Kuznetsov

Geological Institute RAS

Author for correspondence.
Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

T. V. Romanyuk

Schmidt Institute of Physics of the Earth RAS

Email: kouznikbor@mail.ru
Russian Federation, 123242, Moscow, Bolshaya Gruzinskaya, 10, bld. 1

A. V. Shatsillo

Schmidt Institute of Physics of the Earth RAS

Email: kouznikbor@mail.ru
Russian Federation, 123242, Moscow, Bolshaya Gruzinskaya, 10, bld. 1

I. V. Latysheva

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

I. V. Fedyukin

Schmidt Institute of Physics of the Earth RAS

Email: kouznikbor@mail.ru
Russian Federation, 123242, Moscow, Bolshaya Gruzinskaya, 10, bld. 1

A. V. Strashko

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

A. S. Novikova

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

E. A. Shcherbinina

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

A. V. Drazdova

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

E. I. Makhinya

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

A. V. Marinin

Schmidt Institute of Physics of the Earth RAS

Email: kouznikbor@mail.ru
Russian Federation, 123242, Moscow, Bolshaya Gruzinskaya, 10, bld. 1

A. S. Dubenskiy

Geological Institute RAS; Lomonosov Moscow State University

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1; 119991, Moscow, Leninskiye Gory, 1, bld. 3

K. G. Erofeeva

Geological Institute RAS; Institute of Geology of Ore Deposits, Petrography, Mineralogy and Geochemistry RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1; 119017, Moscow, Staromonetny lane, 35

V. S. Sheshukov

Geological Institute RAS

Email: kouznikbor@mail.ru
Russian Federation, 119017, Moscow, Pyzhevsky lane 7, bld. 1

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2. Fig. 1. Tectonic zonality of the Black Sea-Balkan-Anatolian megaregion. The basis of the drawing with simplifications (according to [Okay et al., 2001]) and additions (according to [Okay et al., 2013]). The red asterisk and marking Z0 is the place of sampling K21–012 from the Novorossiysk-Anapa fleece. The markings Z1–Z8 in red indicate the position of the regions or sampling sites. The results of U–Pb dating of detrital zircon grains from them are discussed in the text and are shown further in Figs. 8 and 9.

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3. Fig. 2. The tectonic zonality of the Caucasus (above) and the scheme of the geological structure of the Nebug-Tuapse region (below) are based on materials from [Korsakov et al., 2002, 2021; Marinin et al., 2017] with simplifications and additions based on the results of the authors' own field research 1-7 – strata distribution fields: anthropogenic – alluvial deposits (1), Eocene (2), Upper Paleocene (3), Lower Paleocene –Denmark (4), Campana–Maastricht (5), Cenomanian–Santonian (6), Alba (7); 8 – discontinuous faults; 9 – elements stratification occurrences: inclined (a), vertical (b), inverted (c); 10th place of sampling K21-012 from the Novorossiysk-Anapa fleece.

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4. Fig. 3. General view and details of the rock outcrops of the Novorossiysk-Anapa flish, located directly south of the “Kiselyov Rock“ a – ”Kiselyov Rock" (far view) and the rocks bordering the beach located south of it (view from the southern limit of this beach); b – “Kiselyov Rock” (medium plan) and the rocky outcrop of the Novorossiysk-Anapa flish (observation point K21- 012, 44°06ʹ 36.83ʺ s. w. 39°01ʹ 59.13ʺ vd); c is a detail of the structure of a vertical rock outcrop in the southern frame of the beach located south of the “Kiselyov Rock”, illustrating the distinctly rhythmic structure of the Novorossiysk-Anapa fleece; g – one of the turbidite rhythms (incomplete Bowm cycle) in the fragment of the Novorossiysk-Anapa flish section studied in the area of the Kiselyov Rock, indicating the sampling sites for the separation of detrital zircon grains from the sandstones of the turbidite rhythm base – sample K21-012 (dZr), and for micropaleontological studies from siltstone mudstones of the upper element of Togo the same rhythm is the K21-012 (MP) sample.

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5. Fig. 4. Some features of the internal structure of the Novorossiysk-Anapa flysch section fragment at the Kiselyov Rock site a – abundant ichnofossils (casts of creeping footprints of bottom organisms) on the sole of the sandstone layer forming the base of one of the turbidite rhythms; b, c – convolute stratification in sandy rocks of one of the turbidite rhythms; g – erosion channels filled with sandy materials in the sole of an incomplete rhythm represented by thin rocks (elements "d“ and ”e" of the Bowm cycle).

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6. Fig. 5. Micrographs of sandstone sections of sample K21–012. On the left (1, 3, 5, 7) – micrographs with parallel nichols, on the right (2, 4, 6, 8) – with crossed knees. 1, 2 – sandstone essentially quartz Q (with glauconite Gl) unsorted massive appearance with basal calcite cement Cc; 3, 4 – sandstone is essentially quartz (with glauconite) unsorted, massive in appearance with abundant calcite cement, numerous needle-like formations of carbonate and siliceous composition (bioclasts), as well as an entire shell of foraminifera of the genus Globigerina filled with silica (chalcedony); 5, 6 – sandstone is essentially quartz (with glauconite) unsorted, massive in appearance with basal calcite cement, with an entire shell of Nodosaria foraminifera filled with crystalline carbonate (calcite); 7, 8 – sandstone is essentially quartz (with glauconite) unsorted, massive in appearance with very abundant calcite cement, bioclasts and whole shells of foraminifera of the genus Lenticulina.

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7. Fig. 6. Installation of optical images of the studied grains of detrital zircon from sandstones of the Danish interval of the Novorossiysk-Anapa flish section (sample K21-012) For each image, the analysis number is indicated in the upper left corner (missing if sampling has not been performed). The index "o” means that the image is obtained in reflected light, without an index – in passing light with parallel nichols, the index “x” – in passing light with crossed nichols. For some grains, two or three images are shown. If there was a sampling, then the position of the laser ablation crater (circle, diameter 25 mk) and the age of the grain in million years are shown, if a conditional dating was obtained. White dotted lines mark visible kernels or boundaries between dissimilar parts inside the grain. The three images without numbers are examples of grains with such a complex internal structure that they did not contain an area with a diameter of 25 microns without obvious irregularities or inclusions, and therefore sampling for U–Pb dating was not carried out. Images 13, 14, 28, 34, 84, 89, 94, 98, 118 and others are examples of grains with various inclusions. Three images of grain 65 in transmitted and reflected light demonstrate an example of void space (P).

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8. Fig. 7. Results of the study of the U–Th–Pb isotope system of detrital zircon grains from sample K21-012 a – diagram with concordia. The ellipses show a 68% confidence interval of measurements for all analyses (± 1σ); b - an enlarged fragment of concordia is shown on a gray background; c – a diagram illustrating the weighted average age of 322 ± 7 million years, calculated from the four youngest U–Pb dates; g is a diagram of the contents of Th and U. Analysis of a55 (very low contents of U = 0.2 g/t and Th = 0.4 g/t) is not shown.

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9. Fig. 8. Comparison of the results of studying the U–Th–Pb isotope system of detrital zircon grains from sandstones of sample K21–012, selected from the Srednedatsky fragment of the Novorossiysk-Anapa flish section, with similar data on sandstones and sands from pre-quaternary strata of the Western Caucasus and other regions

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10. Fig. 9. Comparison of probability density curves (KPV) of U–Pb ages of detrital zircon grains from sample K21-012 with similar data for Crimea in the age range < 1 billion years In circles: Z7 is an integral CPV summarizing the results of U–Pb dating of detrital zircon grains from the Middle and Upper Jurassic rough–clastic strata of the Mountainous Crimea (4 samples in different geographical locations, n = 269, according to [Romanyuk et al., 2020], Z8 is an integral CPV summarizing data on 9 samples from Middle Jurassic-Neogene sandstones of the Mountainous Crimea (according to [Nikishin et al., 2015a], n = 602); n is the number of analyses used to construct the KPV. Yellow ovals mark three stages of magmatic activity manifested in the Scythian-Pontid volcanic belt: 360-315 million years, 315-270 million years and 270– 200 million years. The blue band J2 marks the widespread Middle Jurassic magmatism in the Mountainous Crimea, Western and Central Caucasus. Information about possible primary sources of zircon of different ages is given in lilac font.

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