Terrane boundaries in the Bohemian Massif: Result of large-scale Variscan shearing

The Lower Jurassic Sub-system comprises four stages, in chronological order, the Hettangian, Sinemurian, Pliensbachian and Toarcian. Each stage is subdivided into a sequence of ‘standard zones’ (= chronozones) and subzones ‐ each correlated primarily on the basis of its ammonite fauna. A further increase in stratigraphical resolution is available by the use of intra-subzonal units known collectively as ‘horizons’. The close link between ammonites and chronostratigraphy means that faunal provincialism may determine which zonal framework, and therefore which subdivision of the Lower Jurassic, applies in different regions of Europe. Such provincialism is of minor importance in the early Jurassic (Hettangian ‐ Lower Pliensbachian) but increases significantly in the Upper Pliensbachian and into the Toarcian where at least three ammonoid faunal provinces are distinguishable. The standard zonal schemes for each relevant faunal area are discussed here, with greatest emphasis being placed on the Northwest European Province, which is characteristic of much of northern Europe throughout most of the Early Jurassic. Intra-subzonal units have only been described in certain regions for parts of the Lower Jurassic but where recognisable these are introduced.

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The Lower Jurassic of Europe: its subdivision and correlation

The Outer Carpathian Basin domain developed in its initial stage as a Jurassic-Early Cretaceous rifted passive margin that faced the eastern parts of the oceanic Alpine Tethys. Following closure of this oceanic basin during the Late Cretaceous and collision of the Inner Western Carpathian orogenic wedge with the Outer Carpathian passive margin at the Cretaceous-Paleocene transition, the Outer Carpathian Basin domain was transformed into a foreland basin that was progressively scooped out by nappes and thrust sheets. In the pre- and syn-orogenic evolution of the Outer Carpathian basins the following prominent periods can be distinguished: (1) Middle Jurassic-Early Cretaceous syn-rift opening of basins followed by Early Cretaceous post-rift thermal subsidence, (2) latest Cretaceous-Paleocene syn-collisional inversion, (3) Late Paleocene to Middle Eocene flexural subsidence and (4) Late Eocene-Early Miocene synorogenic closure of the basins. In the Outer Carpathian domain driving forces of tectonic subsidence were syn-rift and thermal post-rift processes, as well as tectonic loads related to the emplacement of nappes and slab-pull. Similar to other orogenic belts, folding of the Outer Carpathians commenced in their internal parts and progressed in time towards the continental foreland. This process was initiated at the end of the Paleocene at the Pieniny Klippen Belt/Magura Basin boundary and was completed during early Burdigalian in the northern part of the Krosno Flysch Basin. During Early and Middle Miocene times the Polish Carpathian Foredeep developed as a peripheral foreland basin in front of the advancing Carpathian orogenic wedge. Subsidence of this basin was controlled both by tectonic and sedimentary loads. The Miocene convergence of the Carpathian wedge with the foreland resulted in outward migration of the foredeep depocenters and onlap of successively younger deposits onto the foreland.

/pdf/late-jurassic-miocene-evolution-of-the-outer-carpathian-fold-3r3wif531m.pdf

Late Jurassic-Miocene evolution of the Outer Carpathian fold-and-thrust belt and its foredeep basin (Western Carpathians, Poland)

POLONAISE '97 — an international seismic experiment between Precambrian and Variscan Europe in Poland

The Variscan orogeny, resulting from the collision of Laurussia with Gondwana to form the supercontinent of Pangaea, was followed by a period of crustal instability and re-equilibration throughout Western and Central Europe. An extensive and significant phase of Permo-Carboniferous magmatism led to the extrusion of thick volcanic successions across the region (e.g. NE German Basin, NW part of the Polish Basin, Oslo Rift, northern Spain). Coeval transtensional activity led to the formation of more than 70 rift basins across the region. The various basins differ in terms of their form and infill according to their position relative to the Variscan orogen (i.e. internide or externide location) and to the controls that acted on basin development (e.g. basement structure configuration). This paper provides an overview of a variety of basin types, to more fully explore the controls upon the tectonomagmatic-sedimentary evolution of these important basins.

Post-Variscan (end Carboniferous-Early Permian) basin evolution in Western and Central Europe

Evidence is presented that a distinct elevation never existed in the area of the present Holy Cross Mts during Permian and Mesozoic time. This area as well as that of the present San anticlinorium were embraced within the Danish-Polish trough and were subsequently subjected to tectonic inversion at the turn of the Cretaceous and Tertiary. Thus, the whole Middle-Polish anticlinorium, was generated in a similar way by Laramide movements on the site of the preceding Danish-Polish trough. Some other tectonic and paleogeographic problems, concerning mainly the Holy Cross Mts and the Middle-Polish anticlinorium, are also discussed.

https://geojournals.pgi.gov.pl/agp/article/download/9923/8456

The Holy Cross area, Central Poland, in the Alpine cycle

The Meta-Carpathian Arch, that comprised cratonic areas of SE Poland, usually experienced in the Mesozoic much less subsidence, or showed uplift, with regard to the Polish part of the Central European Basin situated farther north. In marked contrast, the areas of the Meta-Carpathian Arch were affected by strong subsidence in Middle and Late Jurassic time, and the peri-Carpathian segment of the Polish Rift began to develop in the Middle Jurassic as a southern extention of that rift, the existence of which north of the Holy Cross Lineament dates back to the Triassic or Permian. A stronger attenuation of continental crust can be recognized south of the Holy Cross Transfer Fault, which bounded the peri-Carpathian segment to the north; this is a feature consistent with the extention of the Polish Rift into the domain of the Carpathian Tethys. The Jurassic tectonic events controlled in the studied areas the formation of the three transgressive-regressive tectono-stratigraphic units: the COK Sequence (CaIlovian, Oxfordian and Lower Kimmeridgian, upper boundary near the top of the Hypselocyclum Zone); the LUK Sequence (Lower and Upper Kimmeridgian, upper boundary within the Eudoxus Zone); and the KVB Sequence (topmost Kimmeridgian, Volgian and Lower Berriasian). Coeval tectonic events, corresponding to those recorded in cratonic Poland, can be recognized in different parts of Europe, particularly in the Carpathians. The alternating phases of relative uplift and subsidence, experienced by the areas of the Meta-Carpathian Arch that flanked the Central European Basin on the south, can be attributed to fluctuations of intraplate stresses. The peculiar behavior of the Cracow region in Mesozoic and Miocene time, as an area never affected by strong subsidence, is thought to have resulted from the presence of Variscan granitoids at its depths. A development of the Polish Rift Basin in agreement with models assuming simple shear on Iithospheric scale is suggested. Normal 0 21 false false false PL X-NONE X-NONE /* Style Definitions */
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Jurassic tectonic events in south-eastern cratonic Poland

The Czorsztyn succession in the Pieniny Klippen Belt of Poland comprises, at the Rogoza klippes near Rogoźnik, the Rogoźnik Coquina Member (Lower Tithonian - Berriasian) and the Rogoza Coquina Member (Lower and Middle Tithonian) overlain by white micritic coquinas (? Upper Tithonian - Berriasian); and at the Stankowa-Skala klippe, the Czorsztyn Limestone Formation (Oxfordian - Klmmeridgian) and the Rogoźnik Member (Tithonian - Berriasian). It is suggested that the Rogoza Coquina ranges down to the Kimmeridgian (and Oxfordian ?), its lower part thus being coeval with the Czorsztyn Limestone of other sections. A new formal lithostratigraphic unit is suggested which should comprise the white micritic coquinas that form the upper part of the present Rogoźnik Member and overlie the Rogoza Member. The succession of Early and Middle Tithonian ammonites in both localities comprises i. a. the genera Semiforfmiceras , Taramelliceras, Sutneria and Simocosmoceras, the representatives of which are described and illustrated, and a new species, Semiformiceras birkenmajeri sp. n., is established. An analysis of the ammonite faunas of the classical section at Stankowa Skala allows to conclude that in the Czorsztyn Limestone there appears a stratigraphic gap which corresponds to the uppermost Callovian and Lower Oxfordian. The Mediterranean ammonite assemblages of the Late Jurassic Czorsztyn ridge show affinities with assemblages from platformic Europe and several units of the Alpine and Carpatho-Balcanic regions; this indicates migration of ammonites across bathyal basin. A special attention is paid to stratigraphic and biogeographic aspects of the genus Pseudovirgatites, and arguments are put forward in favour of approximate stratigraphic equivalence of the Middle/Upper Tithonian and Lower/Middle Volgian boundaries.

https://geojournals.pgi.gov.pl/agp/article/download/9477/8025

A new account on the Upper Jurassic stratigraphy and ammonites of the Czorsztyn succession, Pieniny Klippen Belt, Poland

New paleontological material comprising Middle Volgian ammonites from the classical region of Tomaszow Mazowiecki in Central Poland, chiefly from the section at Brzostowka, is presented. A new species, Zaraiskites regularis sp.n., is established. Four new horizons are established in the Scythicus Zone of Poland: the Quenstedti and Scythicus Horizons in the Scythicus Subzone, followed by the Regularis and Zarajskensis Horizones in the Zarajskensis Subzone. These horizones are based on four successive assemblages of Zaraiskites , interpreted as biospecies. The new horizons allow to establish some more precise interregional stratigraphic correlations; e.g ., the Regularis Horizon has its age equivalent at some level in the Calpionellid Zone A in the Upper Tithonian Substage. Normal 0 21 false false false PL X-NONE X-NONE /* Style Definitions */
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https://geojournals.pgi.gov.pl/agp/article/download/13653/12094

The Scythicus Zone (Middle Volgian) in Poland: its ammonites and biostratigraphic subdivision

The Upper Kimmeridgian Eudoxus and Autissiodorensis Zones, with the Fallax Subzone at the top of the latter zone, as well as the Lower Volgian Klimovi, Sokolovi, Pseudoscythica, and Tenuicostata Zones, can be recognized in several expanded and continuous sections of the Paluki Formation in Central Poland. There can be reconstructed a Subboreal lineage of the Perisphinctaceae, leading from Discosphinctoides subborealis sp.n. and Sarmatisphinctes gen.n. in the Autissiodorensis Zone, through Ilowaiskya and Pseudovirgatites in the Lower Volgian, to Zaraiskites in the Middle Volgian. The ammonite assemblages of the Paluki Formation, which also include Aulacostephanus and Amoeboceras in the Upper Kimmeridgian, are predominantly of Subboreal type, but Mediterranean/Submediterranean ammonites, chiefly the Haplocerataceae, are also represented at some stratigraphic levels. Interregional stratigraphic correlations are discussed in the paper, especially those between the Tithonian and Volgian Stages. The new biostratigraphic material permits e.g. to correlate the top of the Klimovi Zone with the top of the Tithonian Hybonotum Zone, and the top of the Sokolovi Zone with a level situated slightly beneath the base of the Middle Tithonian in Franconia.

Jan Kutek

Papers

The Holy Cross area, Central Poland, in the Alpine cycle

Jurassic tectonic events in south-eastern cratonic Poland

A new account on the Upper Jurassic stratigraphy and ammonites of the Czorsztyn succession, Pieniny Klippen Belt, Poland

The Scythicus Zone (Middle Volgian) in Poland: its ammonites and biostratigraphic subdivision

The highest Kimmeridgian and Lower Volgian in Central Poland; their ammonites and biostratigraphy