Late Jurassic facies architecture of the Złoczew Graben: implications for evolution of the tectonic-controlled northern peri-Tethyan shelf (Upper Oxfordian–Lower Kimmeridgian, Poland)

Oxfordian neptunian dykes with brachiopods from the southern part of the Kraków-Częstochowa Upland (southern Poland) and their links to hydrothermal vents

“…The opening of both the Northern Atlantic and Tethys Oceans resulted in the Late Jurassic Pan-European stress-field reorganization, which also included the passive, northern margin of the Tethys (Ziegler 1990;Allenbach 2001Allenbach , 2002Nieto et al 2012) together with the recent KCU. In the same period, Paleozoic faults were also rejuvenated, which gave rise to pulses of subsidence and localization of Late Jurassic depocenters over the Late Paleozoic tectonic grabens (Rioult et al 1991;Faerseth 1996;Pittet and Strasser 1998;de Wet 1998;Allenbach 2001Allenbach , 2002Wetzel et al 2003;Krajewski et al 2014Krajewski et al , 2016. These processes continued in the Cretaceous and Neogene.…”

Kimmeridgian hardground-sequence boundary from the Mesozoic margin of the Holy Cross Mountains (central Poland): implications for the evolution of the northern Tethyan carbonate shelf

“…Probably, seismic events associated with fault movements initiated mass movements along tectonically controlled scarps during Lower Platynota Zone time. The effects of such movements are observable in many other sites in central and southern Poland (e.g., Kutek 1968Kutek , 1994Matyszkiewicz 1996;Krajewski et al 2016). The sediment forming the lower part of the layer with bored clasts was deposited as a debris flow, conglomerate and in the higher part from turbidity current where normal grading is observed (Fig.…”

“…Evaluation of the current state of knowledge about the Upper Oxfordian and Lower Kimmeridgian successions may lead to the discovery of significant implications, which will help with the understanding Matyja et al 1989;Kutek 1994;Gutowski et al 2005;Krajewski et al 2011a). Rapid sedimentation on the platform occurred during the Upper Transversarium-Bifurcatus and Planula Zones, when reef and biostrome facies became common (e.g., Matyszkiewicz et al 2012Matyszkiewicz et al , 2015Matyszkiewicz et al , 2016Krajewski et al 2016). This may have been connected with the Middle Oxfordian (Transversarium Zone) warming of climate and sea-level rise (e.g., Price and Rogov 2009;Brigaud et al 2014;Colombié et al 2014;Wierzbowski 2015), which initiated the vast development of carbonate platforms across many European areas (e.g., Leinfelder et al 1996;Matyszkiewicz 1997;Olóriz et al 2003;Reolid et al 2005;Báde-nas and Aurell 2010;Olivier et al 2011;Colombié et al 2014).…”

“…1) during the Late Jurassic was controlled mainly by sea-level and climate changes, the mosaic architecture of the Paleozoic basement and synsedimentary tectonics (e.g., Kutek 1994;Matyszkiewicz et al 2012Matyszkiewicz et al , 2016Gutowski et al 2005;Krajewski et al 2011aKrajewski et al , 2016. On a larger scale, these factors were related to Late Jurassic reactivation of older faults at the margins of the Paleozoic terranes forming the margin of the West European Platform near the Teisseyre-Tornquist Zone (Fig.…”

“…At the break between intervals I and II, significant changes in facies occurred in the Polish part of the northern peri-Tethyan shelf ( Fig. 2; e.g., Kutek 1994;Matyszkiewicz 1996;Krajewski et al 2016). These changes were marked by: (i) the disappearance of microbial-sponge, microbial-Crescentiella, and coral buildups characteristic of the Upper Oxfordian; (ii) drowning of the platform in the Lower Platynota Zone and development of marly facies, and (iii) common occurrence of gravity-flow deposits in the form of debrites, conglomerates, calciturbidites, and olistoliths.…”