The position and age of flysch deposits in the Crimean Mountains (Southern Ukraine).

Oszczypko, Nestor; Ślączka, Andrzej; Bubniak, Іhor; Olszewska, Barbara; Garecka, Małgorzata

doi:10.7306/gq.1359

Cited by 4 publications

(17 citation statements)

References 17 publications

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“…is formed by sedimentary rocks ranging from Triassic to Lower Cretaceous in age (e.g., Muratov 1973;Mileev et al 2006;Krajewski and Olszewska 2007;Nikishin et al 2015a, b;Arkadiev et al 2018). Both the age and the evolution of particular tectonic units however still remain controversial (Mileev et al 2006;Yudin et al 2015;Oszczypko et al 2017). According to Nikishin et al (2015b), these sedimentary rocks represent three major mega-sequences: (a) Triassic-Early Jurassic; (b) Aalenian-Bathonian; and (c) Callovian-Berriasian.…”

Section: Location and Geological Settingmentioning

confidence: 99%

Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula

Krajewski

Schlagintweit²

2018

Facies

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In the Upper Jurassic reef successions of the Crimean Peninsula (Sudak and Jalta areas), the microencruster Crescentiella morronensis (Crescenti), microbialites, and multiple generations of cements, form microframeworks. They were observed in two stages of the carbonate platform evolution, in the Middle-Upper Oxfordian, and in the Upper Kimmeridgian-Tithonian. Generally, in both stages, the features of the microframeworks are similar and consist of densely packed Crescentiella associated with microbialites and branched colonies of the sclerosponge Neuropora lusitanica Termier. The difference between the occurrences of the two stages is the variable amount of nubecularid foraminifera and enigmatic tube-shaped structures forming the central cavities of Crescentiella. The Crescentiella-microbial-cement microframeworks formed under phreatic conditions in the upper slope and seaward marginal depositional settings where intensive synsedimentary cementation took place. They formed in the initial stages of long cycles of restoration and blooming of the reefs. The late Jurassic examples resemble the Permian algae-microbial-cement reefs as well as the Triassic Tubiphytes and cement crust-dominated reefs. Concurrently, all these examples formed a transitional facies zone between typical slope facies to shallow subtidal platform margin facies characterized by high taxonomic diversity of calcified sponges, corals, and microencrusters forming the principal part of the reefs.

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Section: Location and Geological Settingmentioning

confidence: 99%

Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula

Krajewski

Schlagintweit²

2018

Facies

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“…A zigzag line means that both flysches are deformed into folds. I would also draw your attention to an article that went unnoticed by you, but which is important for understanding the relationship between flysch of different ages in the southern part of the Crimean Mountains [Oszczypko et al, 2017]. This work also supports the stratigraphic contact between two flyshes and , according to the cross-section constructed using data of new foraminifers dating of flysch rocks, both flysches are folded and deformed [Oszczypko et al, 2017].…”

mentioning

confidence: 56%

Comments to a publication of Stovba et al., 2020 «Geological structure and tectonic evolution of the Ukrainian sector of the Black Sea», Geophysical journal, 2020, Vol. 42, № 5, P. 53-106

Sheremet

2020

Geofizicheskiy Zhurnal

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“…The oldest rocks exposed in Crimea, belong to the Tauric Complex, attributed to the Upper Triassic-Lower Liassic (e.g. Nikishin et al, 2017;Oszczypko et al, 2017). They include deep-water terrigenous flysch deposits similar to deposits of the Küre Complex in the Central Pontides (Ustaömer and Robertson 1994;Nikishin et al, 2011).…”

Section: 2-stratigraphy Of the Crimean Mountainsmentioning

confidence: 99%

“…They include deep-water terrigenous flysch deposits similar to deposits of the Küre Complex in the Central Pontides (Ustaömer and Robertson 1994;Nikishin et al, 2011). In the eastern Crimean Mountains, formations mapped as Tauric Complex (Muratov, 1969) have been dated as Early Cretaceous in age (Popadyuk and Smirnov, 1991;Popadyuk et al, 2013;Sheremet et al, 2016a;Oszczypko et al, 2017). The age of this complex is still the subject of debate (e.g.…”

Section: 2-stratigraphy Of the Crimean Mountainsmentioning

confidence: 99%

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Age and geodynamic evolution of the Black Sea Basin: Tectonic evidences of rifting in Crimea

Hippolyte

Murovskaya

Volfman³

et al. 2018

Marine and Petroleum Geology

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The timing and direction of opening of the Black Sea Basin are debated. However, parts of its margins were inverted during Cenozoic and can be studied onshore. The Crimean Mountains are located in the middle of the northern margin of the basin, and at the onshore prolongation of the mid-Black Sea High. We present the first detailed mapping of large striated normal faults in Crimea. These faults define graben structures that trend parallel to the continental margin. Kinematic analysis of the faults combined with new biostratigraphic data show that the syn-rift sequence is Valanginian to Late Albian in age. It consists of siliciclastic deposits with limestone olistoliths. In contrast, the post-rift Late Cretaceous carbonaceous sequence of Crimea is devoid of normal faults or olistoliths. It unconformably overlies the graben structures. The onset ages, and the trends of extension are quite similar in the northern (Crimea) and the southern (Turkey) inverted margins of the basin. The Early Cretaceous extension directions are normal to the mid-Black Sea High and the Black Sea margins. We conclude that rifting of Black Sea Basin occurred from the Valanginian to the Late Albian (~39 Ma) and drifting during the Late Cretaceous. Based on the directions of rifting, on the lack of evidence of strike slip motions near the mid-Black Sea High, and on published paleomagnetic data, we propose that the Black Sea opened with rotations accommodated by transform faults at its western and eastern margins, as a response to asymmetric slab rollbacks of the Neo-Tethys plate. The inversion of the Crimean margin results from two successive shortening events: Early Eocene NE-SW compression, Eocene to Present SE-NW compression. Their timing support the idea that compressional stresses generated by continental collisions in Turkey were transmitted through the strong Black Sea lithosphere up to Crimea. 1-Introduction: The Black Sea is a 2200 m deep marine basin surrounded by alpine mountains including the Balkanides, the Pontides, the Greater Caucasus and the Crimean Mountains (Fig. 1A). Because of its location, at the rear of the Srednegorie-Pontides-Achara-Trialet magmatic arc, it is classically interpreted as a back arc basin that opened from Cretaceous to Paleocene times within the East European platform, behind the north-dipping Neotethyan subduction zone (e.g. Zonenshain and Le

show abstract

The position and age of flysch deposits in the Crimean Mountains (Southern Ukraine).

Cited by 4 publications

References 17 publications

Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula

Crescentiella-microbial-cement microframeworks in the Upper Jurassic reefs of the Crimean Peninsula

Comments to a publication of Stovba et al., 2020 «Geological structure and tectonic evolution of the Ukrainian sector of the Black Sea», Geophysical journal, 2020, Vol. 42, № 5, P. 53-106

Age and geodynamic evolution of the Black Sea Basin: Tectonic evidences of rifting in Crimea

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