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Stratigraphy and microfacies of the Jurassic and lowermost Cretaceous of the Veliky Kamenets section (Pieniny Klippen Belt, Carpathians, Western Ukraine)

Rehakova D., Matyja B., Wierzbowski A., Schlogl J., Krobicki M., Barski M.

Volumina Jurassica

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2011

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Vol. 9, no. 1

61-104

EN

The Veliky Kamenets section in the eastern part of the Pieniny Klippen Belt in the Ukrainian Carpathians shows a well exposed, 83 m thick succession composed of Jurassic and lowermost Cretaceous (Berriasian) deposits. The terrigenous part of the section includes: gravels with a sandy matrix (unit 1A), massive grey-green sandstones (unit 1B) and shales with intercalations of siltstones/sandstones and oyster/gastropod lumachelles (unit 2). Organic-walled dinoflagellates document the Toarcian-Aalenian age of the siliciclastic deposits of unit 2. The carbonate part of the succession embraces: stromatactis mud-mounds interfingering with crinoidal limestones (unit 3A), lower nodular limestones (unit 3B), cherty limestones (unit 3C), upper nodular limestones (unit 3D), pink pelitic limestones (unit 3E), limestones with a volcanogenic bed (unit 5) and limestone breccia limestones (unit 6). This succession has yielded abundant ammonites from the Bathonian, Oxfordian and Kimmeridgian (with a stratigraphical hiatus covering the Callovian and Lower Oxfordian), as well as calcareous dinoflagellates (from the Upper Oxfordian towards the top of the succession), and calpionellids (in the Tithonian and Berriasian). Detailed stratigraphical study of the succession based both on ammonites and microfossils has resulted in the recognition of biostratigraphical units and their correlation with the chronostratigraphical scale.The microfacies recognized in the pelagic part of the succession include: the “filament” (Bositra) microfacies (Bathonian), the planktonic foraminifer microfacies (Oxfordian), the Saccocoma microfacies (Kimmeridgian to Upper Tithonian), and the calpionellid microfacies (Upper Tithonian–Berriasian). The volcanogenic rocks (lava flows and volcanic ash) appear in the topmost part of the succession (units 4 to 6) and this volcanic event is very precisely located in the Elliptica-Simplex chrons of the Middle and Late Berriasian.

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Towards better understanding of ammonoid taphofacies of pelagic carbonate platforms

Tomasovych A., Schlogl J.

Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie

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2009

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T. 35, z. 3/1

101-102

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The first occurrence of "Prosopidae" s.l. (Crustacea: Decapoda: Brachyura) and other findings of crustaceans in the Upper Jurassic limestones of the Pieniny Klippen Belt

Hyzny M., Schlogl J.

Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie

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2009

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T. 35, z. 3/1

61-63

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Jurassic to Lower Cretaceous deposits of the Pieniny Klippen Belt and Manin Unit in the Middle Vah Valley (Biele Karparty and Strazovske Vrchy Mts, Western Slovakia) : (field trip guide)

Schlogl J., Michalik J., Plasienka D., Aubrecht R., Rehakova D., Tomasovych A., Bucova J., Mikus V., Sykora M., Golej M.

Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie

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2009

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T. 35, z. 3/1

119-181

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New data on the classic "Callovian" locality in Babiarzowa Klippe (Pieniny Klippen Belt, Poland)

Schlogl J., Wierzbowski A., Golej M.

Geologia / Akademia Górniczo-Hutnicza im. Stanisława Staszica w Krakowie

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2008

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T. 34, z. 3/1

206-207

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Middle to Upper Jurassic stromatactis mud-mounds in the Pieniny Klippen Belt, Carpathians

Aubrecht R., Krobicki M., Schlogl J.

Volumina Jurassica

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2006

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Vol. 4, no. 1

76-76

EN

Stromatactis mud-mounds are structures still enigmatic, despite of many years of research. Recently, most authors consider stromatactis mud-mounds to be fossil microbial reefs. Particularly enigmatic is the origin of stromatactis structures that appear to be the main megascopic component of the mounds. Stromatactis mud mounds occur since Neoproterozoic time and reach their maximum in Palaeozoic, especially in Carboniferous and Devonian. Mesozoic examples are rare. They were reported mostly from Jurassic; later examples are dobtfull. Our research concerns Jurassic stromatactis mud-mounds. To date, stromatactis structures were only reported from the Early Jurassic of the Upper Austroalpine of the Eastern Alps, Early Jurassic of Sicily, Oxfordian mud-mounds of southern Germany, offshore Nova Scotia, Oxfordian of Cracow Upland, Poland and Lower Kimmeridgian of southern Portugal. Recently, Middle- and Upper Jurassic stromatactis mud-mounds were found in the Czorsztyn Unit of the Pieniny Klippen Belt in Slovakia and Transcarpathian Ukraine: Slavnicke Podhorie, Atepnicka Skala, Babina, Kyjov-Puste Pole, Priborzhavskoe and Velyky Kamenets. Stratigraphic range of the mounds is Bajocian to Lower Tithonian. Geometry of the mounds could only be studied at Atepnicka Skala, Priborzhavskoe and Veliky Kamenets, where flat mound shapes are revealed. Other outcrops show only fragments of the mounds or their shape is merged with the surrounding rocks. Rocks of the mounds are mostly micritic to micropeloidal mudstones, containing fauna of pelecypods, brachiopods, ammonites and crinoids. All the occurrences are characterized by mass occurrence of stromatactis structures. In some of them (Slavnicke Podhorie, Priborzhavskoe and Veliky Kamenets), the stromatactis cavities occur also in the crinoidal limestones underlying the mud-mounds which is an atypical feature. Only three sites investigated by us involve considerable portion of sponge spicules in the mound matrix which contradicts to a theory favouring sponges as stromatactis builders. There was no discernible type of biota that might serve as being responsible for the stromatactis structures. Also biota itself is variable. The Bajocian to Callovian mounds contain more benthic biota, e.g. brachiopods, bivalves, sponges, agglutinated foraminifers etc., although biota as a whole was dominated by planktonic representatives, as shells of Bositra bivalves. The Oxfordian and younger occurrences were fully dominated by planktonic biota, e.g. planktonic foraminifers Globuligerina, planktonic crinoids Saccocoma, ammonites, shells of Bositra or coccal algae Globochaete alpina. The latter type also lacks micropeloidal matrix which is ubiquitous in the first type. The micropeloidal to clotted structures are usually attributed to be typical for microbialites.