The studied section of the Pieniny Klippen Belt is, apart from tectonic klippens, characterized by the presence of sedimentary-type klippens – olistoliths situated in the Upper Cretaceous and Paleogene flysch sediments (Jarmuta and Proc fms.) of the Oravic Subpieniny and Saris units, respectively. These tectono-sedimentary breccias are known as the Gregorianka and Milpos breccias (Nemcok et al., 1989; Plasienka and Mikus, 2010) and represent synorogenic deposits formed in response to superficial thrusting processes. The Gregorianka breccias form tabular to lenticular bodies in the upper parts of the Maastrichtian Jarmuta Fm. of the Subpieniny unit. They contain mostly monomictic material derived from the structurally highest Pieniny unit of the Pieniny Klippen Belt. In contrast, the Paleocene – Lower Eocene Milpos Breccia from the structurally lowermost Saris Unit contains variegated material derived mainly from the overlying Subpieniny unit and probably also from the Pieniny unit, including some recycled “exotic” material. They also carry blocks – olistoliths derived from these units which range up to the size of megaolistolites. These can be considered as already partly disintegrated fronts of the overriding Subpieniny nappe that were transformed to bodies of tectono-sedimentary breccias and transported gravitationally as mass-flows into the frontal Proc flysch basin. Consequently, the Gregorianka and Milpos breccias represent important sedimentary records of the tectonic thrust processes in the Oravic Superunit of the Pieniny Klippen Belt. The main aim of this contribution is sedimentological, biostratigraphical and lithologic-petrographic analysis of the breccia material and interpretation of their origin and significance for dating of the thrusting events within the Pieniny Klippen Belt.
Abstract An exceptional, briefly exposed section across the boundary between the Pieniny Klippen Belt (PKB) and the Central Carpathian Paleogene Basin (CCPB) in Eastern Slovakia showed that the contact is formed by a single, subvertical fault plane. Whereas the Oligocene CCPB deposits exhibit only weak deformation with S-verging fold-and-thrust structures, the Cretaceous PKB sediments are internally strongly sheared with scaly fabric and numerous calcite veins. It is inferred that the PKB suffered strong thrusting- and wrenching-related deformation in pre-Oligocene times, while the Early Miocene oblique backthrusting resulted in exhumation of the PKB and formation of its steep fault boundaries
Biostratigraphic investigations of carbonate strata that sandwich volcanic rocks and studies of the volcanic rocks were made along five composite lithological sections across the Upper Jurassic-Lower Cretaceous carbonate rocks of autochthonous cover of the High-Tatric Unit in the Osobitá peak area of the Western Tatra Mts. A carbonate microbreccia that consists almost exclusively of limestone clasts containing calpionellids occurs immediately below the volcanics. The youngest identified microfossil Calpionella elliptica Cadisch in the individual limestone clasts showed the age of breccia formation to be younger than late Early-early Middle Berriasian. The volcanic rocks are overlain by the Osobitá Limestone Formation, which in the lowermost horizons consists of a few metres thick crinoidal limestone containing the foraminifers Meandrospira favrei (Charollais, Brönnimann & Zaninetti), Sabaudia minuta Hofker and Montsalevia salevensis (Charollais, Brönnimann & Zaninetti) indicating a Late Valanginian-Early Hauterivian age. The biostratigraphical and sedimentological data obtained show that volcanism took place in several phases. Less intense phases of volcanism are recorded as thin tuffitic laminae within the upper parts of the Tithonian-early Mid Berriasian Sobótka Limestone Member and as fragments of volcanic rock in the carbonate breccia. The main phase(s) of volcanism took place during the Late Berriasian-?Early Valanginian.
Abstract We present the latest magnetotelluric models on profiles in the northeastern part of Slovakia and the southeastern part of Poland. These models are focused on deciphering the tectonic structures at the contact of the Inner Carpathians with the European Platform in this area. For the Inner Carpathian block, we propose the term Carpathia. Profile SA-01 shows shallower structures and the parallel MT-05 profile shows deeper structures. These models are also correlated with the seismic profile CEL-05. All results are compatible and show an original subduction-collisional structure, which was later replaced by a transpressive-transtensional one. The most striking structures are thick highly conductive subhorizontal zones in the middle crust and a tectonically controlled deep vertical conductive structure—the Carpathian conductive zone. Other significant structures, which also appear in the seismic section, are back thrusting of Flysch Belt and the Klippen Belt basement (Penninic crust) uplift.
