Famennian Fusulinina (Foraminifera) from the Holy Cross Mountains (central Poland)

Abstract

Calcareous foraminifers representing 9 species and 5 genera were investigated in two Famennian sections located in the south‐western part of the Holy Cross Mountains (HCM), central Poland. They constitute redeposited material that, together with crinoids and calcareous algae, comprise the dominant component of limestone turbidite beds intercalated with deep‐marine marly sediments. The calcareous material was redeposited from an unknown carbonate platform located probably to the south of the HCM area. The first appearance data of foraminifers, mainly from the quasiendothyrid group, correlated to the Standard Conodont Zonation, indicate a diachronous appearance of the same species in different parts of Europe due to a migration delay from the foraminiferal evolutionary centre located in the south‐eastern shelves of Laurussia in the neighbouring areas. As a result, the Moravian foraminiferal zonation, where index taxa appeared in similar stratigraphic intervals, was chosen as the most applicable to the stratigraphy in the central Polish area. The Quasiendothyra communis–Eonodosaria evlanensis Interzone, the Quasiendothyra communis–Quasiendothyra regularis Zone and Quasiendothyra kobeitusana–Quasiendothyra konensis Zone were distinguished, respectively, in the HCM sections. Copyright © 2012 John Wiley & Sons, Ltd.

Large sulphur isotopic perturbations and oceanic changes during the Frasnian–Famennian transition of the Late Devonian

“…This basin was bounded to the north by the Kielce Swell (Diminy Reef) and to the south by a platform that was subsequently buried under a Mesozoic succession (Fig. 1c;Racki 1993;Wojcik 2012). The F-F boundary succession is characterized by marly shales intercalated with thin-to medium-bedded limestones in which normally graded and hummocky cross-stratified beds are common (Fig.…”

A new early Frasnian (Late Devonian) foraminifer from eastern Taurides (Turkey): Evolutionary and paleobiogeographic implications

“…From the Early Carboniferous and up to the latest Permian, the types of wall 2 and 6 largely dominated or remained the unique types of tests. The Frasnian/Famennian crisis can make the types 3 and 5 totally disappear and the types 2 and 6 dominate (Vachard et al, 2010;Wojcik, 2012). By these disappearances, the Frasnian-Famennian crisis is therefore almost so drastic for the foraminifers as the Permian-Triassic boundary crisis.…”

“…The calcareous Devonian foraminifers, especially the Frasnian forms, have been determined primarily from the Russian Platform, the Urals, Siberia (Russia) and former USSR Central Asia (or Tian Shan; currently part of Kirgizstan) by Birina, 1948;Vissarionova, 1950;Antropov, 1950;Lipina, 1950;Bykova, 1952;Bykova in Bykova and Polenova, 1955;Reitlinger, 1954Reitlinger, , 1962Pronina, 1960;Chuvashov, 1965;Poyarkov, 1969Poyarkov, , 1979Petrova, 1981;andZadorozhnyi, 1985, 1987. They were also recognised in Canada (Toomey, 1965); Europe (e.g., Vachard, 1974Vachard, , 1988Vachard, , 1991Vachard, , 1994Neumann et al, 1975;Conil and Lys, 1970;Kalvoda, 1990;Racki and Sobón-Podgórska, 1992;Wojcik, 2012) and Australia (Edgell, 2004;Vachard and Haig, work in progress).…”

The uppermost Emsian and lower Eifelian in the Kielce Region of the Holy Cross Mts. Part I: Lithostratigraphy

“…The Palaeozoic rocks in this locality are exposed in the Zbrza Antycline as a part of the Wolica-Zbrza Fold, the largest tectonic structure of the southern Mesozoic surrounding of the HCM. The Cambrian to Upper Devonian strata of the area were the subject of detailed investigations (Deczkowski and Tomczyk 1969;Filonowicz 1968Filonowicz , 1973Kucia 1987;Wójcik 2009Wójcik , 2012see also Czarnocki 1919;Studencka 1983;Hajłasz 1967;Racki 1993, p. 95). The Zbrza Anticline is also one of the most important outcrops of the Dąbrowa Horizon (Gürich 1896;Zbroja et al 2007).…”

“…2). This consecutively resulted in: (i) late Emsian termination of continental sedimentation and development of marginal and marine clastic deposition (Łobanowski 1971, 1991Szulczewski and Porębski 2008); (ii) latest Emsian-early Eifelian retrogradation of clastic lithotypes beyond the Holy Cross area and development of carbonate lagoonal environments (Wójcik 2013); (iii) early Eifelian short-term constitution of open-marine environments (Malec 2005;Wójcik 2013); (iv) late Eifelian unification of shallow carbonate shelf environments (Skompski and Szulczewski 1994;Narkiewicz and Narkiewicz 2010;Niedźwiedzki et al 2010;Narkiewicz and Ratellack 2014;Wójcik 2013;Narkiewicz et al 2015); (v) Givetian to Frasnian transformation of a carbonate shelf into an isolated reef-rimmed shallow-marine "Dyminy" carbonate platform surrounded by deeper Łysogóry and Chęciny-Zbrza intrashelf basins (Szulczewski 1971;Racki 1993;Racki et al 2002;Wójcik 2012); (vi) late Frasnian to early Famennian drowning of a carbonate platform and its transformation into a pelagic platform (Szulczewski 1978;Szulczewski et al 1996;Wójcik 2009Wójcik , 2012; and (vii) late Famennian-Early Carboniferous unification of deep marine marly sedimentation (Szulczewski 1971(Szulczewski , 1973(Szulczewski , 1995(Szulczewski , 2006.…”