An Albian demise of the carbonate platform in the Manín Unit (Western Carpathians, Slovakia)

Abstract

Abstract:The production of platform carbonates of the Manín Unit (Manín Straits, Central Western Carpathians) belonging to the Podhorie and Manín formations and formed by remains of rudists and benthic foraminifers (Urgonian-type carbonates), was previously assumed to terminate during the Aptian. First, we show that these deposits were primarily formed on the upper slope (Podhorie Formation) and in a fore-reef environment (Manín Formation). Second, biostratigraphic data indicate that the shallow-water production persisted up to the Albian, just as it did in another succession of the Manín Unit. The Podhorie Fm contains colomiellids (Colomiella recta, C. mexicana) and calcareous dinoflagellates (Calcisphaerula innominata) that indicate the Albian age. It also contains planktonic foraminifers (Ticinella roberti, Ticinella cf. primula, Ticinella cf. madecassiana, Ticinella cf. praeticinensis) of the Albian Ticinella primula Zone. The Podhorie Formation passes upwards into peri-reefal facies of the Manín Fm where we designate the Malý Manín Member on the basis of rudists shell fragments and redeposited orbitolinids. Microfacies associations share similarities with the Urgonian-type microfacies from Mediterranean Tethys and allow us to restrict the growth and the demise of the carbonate platform. δ 13 C and δ 18 O isotopes change over a broad range of both formations: δ 13C is in the range +1.03 to +4.20 ‰ V-PDB and δ 18O is in the range −0.14 to −5.55 ‰ V-PDB. Although a close correlation between δ 13 C and δ 18 O indicates diagenetic overprint, a long-term increase of δ 13C can indicate a gradual increase in the aragonite production and/or increasing effects of oceanic water masses in the course of the Albian, prior to the final platform drowning. Carbonate platform evolution was connected with submarine slumps and debris flows leading to redeposition and accumulation of carbonate lithoclasts and bioclastic debris on the slope. Our study confirms that the growth of carbonate platforms in the Central Western Carpathians was stopped and the platform collapsed during the Albian, in contrast to the westernmost Tethys. A hardground formed during the Late Albian is overlain by Albian -Cenomanian marls of the Butkov Formation with calcisphaerulid limestones characterized by planktonic foraminifers of the Parathalmanninella appenninica Zone and calcareous dinoflagellates of the Innominata Acme Zone.

Demise of the Middle Jurassic carbonate platform: Responses to sea‐level fall in the Qiangtang Basin, Eastern Tethys

“…The growth and demise of carbonate platforms are dependent on the carbonate production rate (Chesnel et al, 2016; Fekete, Daniela Boorova, Lintnerova, Michalik, & Grabowski, 2017). The high carbonate production rate can be favoured by decreasing detrital flux and oligotrophic surface water conditions in an arid or semi‐arid climatic environment.…”

Nucleation and amplification of doubly-plunging anticlines: the Butkov pericline case study (Manín Unit, Western Carpathians)

“…Massive Urgon-type limestones are thicker and were deposited in a more proximal position to the platform margin compared to the Butkov area (upper slope to fore-reef; cf. Fekete et al 2017). PLIOC.…”

“…8A). This is mainly due to the fact that the Urgontype limestones are mostly resediments composed of the platform-derived detritus deposited in slope aprons and slope-toe fans (e.g., Fekete et al 2017). Real bioherms only occur on Mt.…”

Paleoenvironment and paleobiogeography of Lower Cretaceous carbonate successions of the northern Tethyan margin: Examples from Northeastern and Central Iran

“…(at 24 m, 33 m, 37 m and 40 m), C. mexicana (at 33 m and 37 m) and Hedbergella sp. (at 40 m), the recognition of the late Aptian to Albian for this thickness is possible (24 to 40 m; Longoria 1972Longoria , 1973Longoria and Gamper 1974;Trejo, 1975;Fekete et al, 2017 andGheiasvand et al, 2019). We also defined a stratigraphic range for the Padeha section, where the first appearance of orbitolinidae occurs at 15 m, which coincides with the presence of Kopetdagaria sphaerica.…”