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Fossil karst in the Jurassic of the Kościuszko Mound in Kraków (southern Poland) : discussion

Felisiak I.

Geological Quarterly

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2016

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Vol. 60, No. 1

252--255

2

Lower Kimmeridgian layer with bored and encrusted hiatus concretions (Upper Jurassic, Central Poland) : implications for stratigraphy and basin evolution

Krajewski M., Olchowy P., Felisiak I.

Annales Societatis Geologorum Poloniae

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2014

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Vol. 84, No. 2

113--129

EN

The paper presents a comparative analysis of a Lower Kimmeridgian layer with bored and encrusted hiatus concretions collected in three study areas, located in Central Poland. These studies demonstrate distinct similarities between the hiatus concretions in terms of their origin, development and stratigraphic position. The layer with its characteristic concretions seems to represent an important marker horizon for the Lower Kimmeridgian successions in Central Poland. The identification of this marker horizon in drill cores and exposures could be important for definition of the stratigraphic position of the sediments, which otherwise lack appropriate biostratigraphic information. The matrix of the concretions is composed of pelagic calciturbidites, which reflect flooding of the early Kimmeridgian platform. These sediments were lithified early and formed a hardground. The origin of the hiatus concretions probably is related to erosion of the hardground, followed by redeposition and several phases of exhumation and erosion, preceding final burial. The characteristic ecological successions, observed in the concretions, document an evolution from soft to firm and hard marine substrates, typical of hardgrounds and evidenced by various burrows, borings (Gastrochaenolites, Trypanites), and epizoans. Calciturbidite sedimentation, hardground erosion and redeposition of the hiatus concretions, known from deposits of the Platynota Zone in Central Poland, were associated with synsedimentary activity of the Holy Cross Fault, on the NE margin of the extensive, tectonic Małopolska Block.

3

Facies of the Upper Jurassic–Lower Cretaceous sediments in the basement of the Carpathian Foredeep (western Ukraine)

Krajewski M., Król K., Olszewska B., Felisiak I., Skwarczek M.

Annales Societatis Geologorum Poloniae

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2011

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Vol. 81, No 3

291-307

EN

The Upper Jurassic–Lower Cretaceous carbonate sediments developed in a narrow, Ukrainian part of the basement of the Carpathian Foredeep show high facies diversity. Based upon thin section studies, the authors identified eleven principal microfacies varieties. Three main stages of development of carbonate platform were distinguished: (i) Oxfordian–Early Kimmeridgian, (ii) Kimmeridgian–Tithonian, and (iii) Berriasian–Valanginian. The Oxfordian sediments are rather thin and represent both the outer and inner, distally steepened ramp facies. In the Late Kimmeridgian and, mainly, in the Tithonian, the intensive growth of rimmed platform took place with distinct zones of peritidal, margin barrier and platform slope, bearing calciturbidite facies. Development of the rimmed platform was controlled by synsedimentary tectonic movements along faults rejuvenated southwest of the Holy Cross Mts. Fault Zone. In the Berriasian–Valanginian, the dominant process was sedimentation onto not-rimmed platform controlled by small sea-level changes. Both the facies development and literature data indicate that the Late Jurassic sedimentation in the Ukrainian part of the Carpathian Foredeep basement shows considerable differences in comparison to that of the Polish part. In the studied successions, large Oxfordian microbial-siliceous sponge reef complexes, known from the Polish part of the Carpathian Foredeep basement and other areas in Europe, were rare. In the study area carbonate buildups were encountered mainly in the intervals representing the Upper Kimmeridgian–Tithonian where small, microbial-sponge and microbial-coral biostromes or patch-reefs were formed. Their growth was presumably restricted to a narrow zone of the upper slope, close to ooidal-bioclastic margin platform facies. In the Polish part of the Carpathian Foredeep basement, the Late Jurassic sedimentation took place on a vast, homoclinal ramp while in the Ukrainian part it proceeded on a narrow, distally steepened ramp and rimmed platform with distinct marginal platform barrier. Similar platform facies distribution in both regions appeared mainly in the Early Cretaceous, although with some stratigraphical differences. The facies distribution of the Upper Jurassic sediments was closely controlled by the block structure of the basement and by orientation of the main, transcontinental Holy Cross Mts. Fault Zone, which supports the opinion on its activity in the Mesozoic era. The Ukrainian part of the Carpathian Foredeep basement located over the Palaeozoic Kokhanivka Block, between the Krakovets and Holy Cross fault zones, includes predominantly the slope, marginal and inner platform facies. Facies observed over the Palaeozoic Rava Ruska Block (south-western part of the East-European Platform), between the Holy Cross and Rava Ruska fault zones, represents mainly the inner platform and the peri-shore deposits.

4

The Tatras - nappes and landscapes

Felisiak I.

Geoturystyka

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2008

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nr 2

75-87

EN

Geological structure of the Tatra Mts is a result of long-lasting processes. The key nappes have already been completed some 65 Ma ago. However as a mountain range the Tatras has emerged at the surface only 5 Ma ago, when a piece of continental crust separated from African continent at the beginning of Mesozoic era ultimately collided with Europe. Thus, the crystalline core of the Tatras, which builts also the highest crest is a fragment of Africa. This monumental mountains are, however, not an effect of the overthrusting but they resulted from young, vertical tectonic movements, which are still active and which sometimes shake the whole Podhale region. The following paper explains how the Tatras were formed. The figures enclosed illustrate the succeeding formation stages of the mountain range and the photographs allow the Reader to compare drawings with the field. Welcome to the Tatras.

PL

Struktura geologiczna Tatr formowała się bardzo długo, a kluczowe dla niej płaszczowiny były już gotowe przed 65 milionami lat. Pomimo tego jako góry Tatry zaczęły się wyraźnie zaznaczać na powierzchni dopiero 5 mln lat temu. Trzeba było aby kawał skorupy kontynentalnej, oderwany od Afryki z początkiem ery Mezozoicznej, ostatecznie wbił się w kontynent Europejski. Jego fragmentem, okruchem Afryki, jest trzon krystaliczny tworzący m. in. Tatry Wysokie. Ich imponujący wygląd nie jest wszakże efektem ruchów nasuwczych a młodych przesunięć pionowych, które do dziś czasami trzęsą Podhalem. Jak to się stało opisuje poniższy artykuł. Zamieszczone w nim rysunki ilustrują kolejne stadia rozwoju Tatr. Liczne zdjęcia pozwalają porównać papierowe konstrukcje z rzeczywistymi dziełami natury. Zapraszam do lektury i wycieczki w Tatry. Autor.

5

The Tatra Mts - rocks, landforms, weathering and soils

Drewnik M., Felisiak I., Jerzykowska I., Magiera J.

Geoturystyka

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2008

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nr 2

51-74

EN

The trip gives insight into geology and landforms as well as into past and present dynamic geological, geomorphologic and soil-forming processes in the central part of Polish Tatra Mts. The area is easily accessible from Zakopane. However not the highest and not the most impressive of all parts of the mountains it offers a concise review of all sites crucial for understanding the geologic history of the Tatras and their forefield. Crystalline core has not only been covered by overthrusted sedimentary rocks but also forms tectonically displaced bodies like crystalline islands over the sediments. Post-orogenic erosion strongly differentiated the mountains landscape. High valleys shaped in resistant granitoids of the High Tatras were much better reservoirs of snow and ice during the Pleistocene then the West Tatras valleys deeply cut into softer sediments and metamorphic rocks. Therefore, the High Tatric glaciers were longer and thicker than the West Tatric ones. Post-glacial weathering, mass movements and accumulation of organic matter resulted finally in formation of rich variety of specific mountain soils.

PL

Trasa wycieczki prowadzi przez środkową część Tatr Polskich: Dolinę Bystrej, Kasprowy Wierch, przełęcz Karb i Dolinę Suchej Wody (Fig. 1). Różnice między dwiema głównymi częściami tych gór: Tatrami Zachodnimi i Wysokimi są stamtąd wyjątkowo dobrze widoczne. Teren ten jest ponadto przedmiotem intensywnych badań od przynajmniej 200 lat, a najnowsze doniesienia pojawiają się co roku. Stamtąd pochodzą liczne datowania moren, wreszcie, to w Dolinie Suchej Wody L. Zejszner pierwszy rozpoznał w 1849 r. ślady zlodowacenia. Przemierzając Tatry podczas planowanej wycieczki będzie można zaobserwować tak wyraźnie widoczne w górach efekty działania procesów prowadzących do niszczenia gór, bardziej szczegółowo przyjrzymy się przejawom wietrzenia. Wietrzenie jest bardzo ważnym procesem warunkującym powstawanie gleb a co za tym idzie wpływającym na rozwój roślin i zwierząt czyli na środowisko życia człowieka.

6

Teaching of geological mapping at Geological Mapping Department, AGH University of Science and Technology, Kraków

Felisiak I., Matyszkiewicz J., Sokołowski T.

Przegląd Geologiczny

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2005

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Vol. 53, nr 10/2

899-903

EN

This paper presents the methods and scope of teaching geological mapping at the Geological Mapping Department, Faculty of Geology, Geophysics and Environments Protection, Stanisław Staszic AGH University of Science and Technology. The main curriculum of Structural Geology and Geological Mapping consists of lectures, laboratory exercises and a summer field practice in Poland, Croatia, Slovakia or Ukraine. Teaching of geological mapping is linked to research done by the staff and to the content of the course Geomorphology and Quaternary Geology (geomorphological mapping). Students have been also taught practical use of the GPS (Global Positioning System).

7

Południowy uskok główny rowu Kleszczowa - koncepcja a rzeczywistość

Felisiak I.

Przegląd Geologiczny

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2001

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Vol. 49, nr 4

307-311

PL

Południowy uskok główny (PUG) rowu Kleszczowa odsłonięto w KWB Bełchatów na długości kilometra we wschodniej części rowu II rzędu. Uskok cechuje generalny bieg 85o przy znacznej lokalnej zmienności w zakresie 65-110o, upad średnio 70o, szeroka strefa brekcji. Towarzyszą mu podłużne uskoki zrzutowe i znacznie młodsze nasunięcia o wergencji południowej oraz połogie uskoki zrzutowe NE-SW, występujące też w kombinacji z uskokami przesuwczymi WNW-ESE. Nie ma stromych uskoków przesuwczych NW-SE przesuwających prawoskrętnie PUG a przyjmowanych na mapach konstruowanych z wierceń.