Wyniki wyszukiwania - Biblioteka Nauki

1

Tectonics of the Subtatric units, Eastern Tatra Mts

100%

Lefeld J.

Studia Geologica Polonica

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1999

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tom Vol. 115

139-166

EN

Three partial nappes occur within the Subtatric zone in the eastern part of the Tatra Mts. These are (from base to top or from south to north respectively): (1) the lower Subtatric partial nappe sensu stricto corresponding to the Suchy Wierch unit of the Zakopane Subtatric area, (2) the Bielskie Tatry partial nappe (= the Hawrań digitation of Sokołowski, 1950) and (3) the Jastrzębia Turnia-Palenica partial nappe (= the Bujaczy digitation of Andrusov, 1936). Their lithostratigraphic completeness and tectonic character differ depending on their situation on transversal elevations and/or depressions, respectively. At the Hawrań-Jagnięcy elevation only the Bielskie Tatry nappe is more or less completely preserved. It is thrust onto the tectonically reduced Middle Triassic of the lower Subtatric nappe. The Bielskie Tatry nappe is superposed by the Jastrzębia Turnia-Palenica nappe which contains the Middle-Upper Triassic members and the Fatra Formation. Farther west, in the Szeroka Jaworzyńska depression (in the Jaworzyna subtatric area), the lower Subtatric nappe is represented by two tectonic scales, namely the Holica-Zadnia Kopa and the Czerwona Skałka ones. Both units show but a part of the Middle Triassic carbonate sequence, and a complete Jurassic and Lower Cretaceous sequence (the latter is reduced at its top). These lower Subtatric scales are overlaid by the Tatry Bielskie nappe and this, in turn, by the Jastrzębia Turnia-Palenica partial nappe. On the Koszysta transversal elevation, still farther west, the lower Subtatric nappe is reduced to a few very small scales. It is overlaid there by a tectonically overturned Kopy Sołtysie unit, a part of the Bielskie Tatry nappe. The Kopy Sołtysie unit is tectonically covered by the Triassic carbonates of the Jastrzębia Turnia-Palenica partial nappe along the line: Gęsia Szyja - Filipczański Wierch. A continuation of the lower Subtatric nappe eastward, up to the Jaworowa Valley, is documented. The Triassic formations cropping out at Filipczański Wierch, Gęsia Szyja, Łysa Skałka, and Wierch Skałki are included to the Jastrzębia Turnia-Palenica partial nappe. Tectonic affiliation of several small tectonic scales of the Križna nappe (sensu lato) in the Gęsia Szyja-Kopy Sołtysie area remains an open question.

2

Correlation of the Subtatric tectonic units south of Zakopane (Polish Tatra Mts)

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Bac-Moszaszwili M. , Lefeld J.

Studia Geologica Polonica

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1999

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tom Vol. 115

131-138

EN

Tectonic units of the lower Subtatric nappe were correlated between the western and eastern parts of the Tatra Mts. It was found that the Mała Świnica unit does not continue toward the east beyond the western slopes of the Dolina Białego valley. North of the Krokiew tectonic scale, there is another unit called the Jastrzębia Turnia scale which, most probably, is a western continuation of the Jastrzębia Turnia-Palenica partial nappe. Fragments of the Middle and Upper Triassic and Lower Liassic rocks, exposed in tectonically reversed position under the Krokiew scale and the Mała Świnica unit, are classified to the Bielske Tatry partial nappe on the basis of identity of their lithostratigraphic sequences and facies development of the Fatra Formation. The so called “Czerwona Przełęcz syncline” thus loses its tectonic meaning: it should be eliminated from the tectonic nomenclature of the Subtatric zone

3

Toarcian ammonites (Adneth facies) from the Subtatris Succession of the Tatra Mts (Western Carpathians)

100%

Myczyński R. , Lefeld J.

Studia Geologica Polonica

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2003

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tom Vol. 121

51-79

EN

Ammonite fauna is described and illustrated from the Kliny Limestone Member (Toarcian-Aalenian - Adneth facies) of the Subtatric Succession in the Tatra Mts. The described forms belong to families Phylloceratidae, Lytoceratidae and Hildoceratidae. The age of the Kliny Limestone Member established on the basis of this fauna is Middle Toarcian-lowermost Aalenian. One form points to Pliensbachian age of the Długa Encrinite Member. Abundance of juvenile ammonite phragmocones has been stated in a horizon of red limestone.

4

The Tatra Mts - rocks, landforms, weathering and soils

63%

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

Geoturystyka

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2008

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tom 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.

5

Facies development and lithostratigraphy of the Hightatric mid-Cretaceous (Zabijak Formation) in the Polish Tatra Mountains

63%

Krajewski K. P.

Studia Geologica Polonica

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2003

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tom Vol. 121

81-158

EN

The paper presents facies development and lithostratigraphy of the mid-Cretaceous Zabijak Formation in the Polish part of the Tatra Mountains. Reference is also made to all known occurrences of the formation in the Slovak part of the Tatra. Geological maps, general and detailed sections, and representative selection of rock samples (Figs 1-60) as well as panoramic photographs of the formation outcrops (Pls 1-17) give insight into the distribution, facies, sedimentary features, lithostratigraphic units, and tectonic position of the mid-Cretaceous sequence in the Tatra Mts. The Zabijak Formation embraces the youngest sedimentary sequence occurring in the Mesozoic Hightatric Succession. It rests disconformably upon various units of the Lower Cretaceous substratum, and is cut discordantly by the Hightatric and/or Subtatric overthrusts. There are three main sedimentary facies in the formation: (1) the limestone facies; (2) the marly facies; and (3) the marly-silty-sandy (flysch-type) facies. They record three consequent stages in the mid-Cretaceous history of the Hightatric sedimentary basin: (1) submerged carbonate platform with prevailing non-depositional conditions and/or condensed sedimentation (Early to Late Albian); and two basinal stages: (2) hemipelagic marly basin with increasing-upwards input of fine terrigenous material (Late Albian through Cenomanian); and (3) marly distal flysch basin with considerable input of fine terrigenous material (?Early Turonian). The Zabijak Formation is subdivided into three superimposed members (new units): (1) the Żeleźniak Member, (2) the Kamienne Member, and (3) the Pisana Member, that correspond to the three main facies of the formation. Five units of bed rank (new units) are defined as well in the basal part of the formation: (1) the Ku Stawku Bed(s), (2) the Wielka Rówień Bed, (3) the Spady Bed, (4) the Upłazkowa Bed, and (5) the Mułowy Beds. The former two represent condensed limestone facies and infillings of cavities and dykes in the direct substratum, whereas the latter three embrace basal conglomeratic and sandy deposits of the overlying Kamienne Member.

6

Piaskowiec kwarcytowy w dolnej części formacji z Kopieńca między Doliną Bystrej i Doliną Olczyską w Tatrach

51%

Iwanow A. , Zabielski R. , Połońska M.

Przegląd Geologiczny

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2011

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tom Vol. 59, nr 3

235-235

EN

Quartzitic sandstone was distinguished at the lower part of the Kopieniec Formation from the Lower Subtatric Nappe (Kriżna Nappe; Fatricum) between the Bystra Valley and the Olczyska Valley, in the Tatra Mts. In previous editions of the detail geological maps of the Tatra Mts, this sandstone was not marked in this area. The quartzitic sandstone crops out at Wysokie hill, east of Kuźnice and can be easily recognized in the field. The sandstone is located above the series of the dark-grey organodetrital limestones and the black calcareous sandstones of the Fatra Formation (Rhaetian) and below the typical brownish- gray claystone of the Kopieniec Formation (Hettangian). Maximum thickness of quartzitic sandstone is about 15 m.

7

Effect of snow patches on vegetation in the high-mountain nival gullies (Tatra Mts. Poland)

51%

Kozłowska A. , Rączkowska Z.

Polish Journal of Ecology

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2006

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tom Vol. 54, nr 1

69-90

EN

The purposes of the present paper are: a) to characterise the spatial pattern of vegetation in the high mountain nival gullies, b) to assess the factors determining the differentiation of vegetation in the gullies with particular consideration of the role of snow patches, and c) to present the similarities and the differences of relations between plant species composition and thickness and duration of snow patches existing in the gullies and in their vicinities.The studies have been carried out in the Polish part of Tatra Mountains (19[degrees]45[minutes]36[second] - 20[degrees]08[minutes]00[second] E and 49[degrees]10[minutes]42[second]-49[degrees]20[minutes]05[second] N), in two nival gullies, located above the upper timberline (i. e. 1500 m a.s.l) . The coverage of each plant species was correlated with the thickness of a snow patch on the basis of the sample plots of 0.25 m^2 (n = 889), located along the vertical transects in the gullies. The relations between variables were established based on the Spearman rank correlation analysis. In order to present the general character of relations between the features analysed the PCA method was applied. The differentiation of vegetation reflects the habitat conditions, which result from the terrain topography, morphometry of the relief forms, as well as from the thickness and duration of the snow patch. In the nival niches there are the species which positively or negatively correlate with the snow patch thickness. It is manifested through the decrease in the number of species as the snow thickness increases. Two species, Luzula alpino-pilosa (Chaix) Breistr. and Festuca picta Kit., can be accepted as indicators of the sites with the long persistent snow cover. The negative correlation of the plant species coverage with the snow patch thickness is not so unambiguous, since the role of the snow patch depends upon the duration of its persistence. The study showed the effect of factors featuring the high-mountain vegetation at different spatial scale, i. e. according to altitude, local sites and micro-site factors connected with the place inside the gully with the snow patch.

8

Lower Jurassic spiculite facies from the Lower Sub-Tatric Succession of the Tatra Mountains, Poland

51%

Jach R.

Biuletyn Państwowego Instytutu Geologicznego

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2001

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tom nr 396

70-71

9

Outline of Quaternary glaciations in the Tatra Mts. : their development, age and limits

51%

Lindner L. , Dzierżek J. , Marciniak B. , Nitychoruk J.

Geological Quarterly

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2003

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tom Vol. 47, No 3

269-280

EN

Geomorphological and geological data collected over many years suggest at least eight episodes during which the Tatra Mts. were glaciated during the Quaternary. Evidence of glaciers can be found both in the Slovakian and Polish parts of the mountains as glaciofluvial deposits located at different altitudes, and in some cases also as terminal and lateral moraines. There are no moraines for the three oldest glaciations, Biber, Donau and Günz, maybe as a result of less intense development of glaciers. During the Mindel (Sanian 2) Glaciation the glaciers occuped a larger area in the High Tatra Mts. in comparison to the Western Tatra Mts., whereas during the succeeding younger pre-Riss (Liviecian) Glaciation their development was more restricted. A greater extent of the Tatra Mts. glaciers occurred again during the Riss I (Odranian) Glaciation, while they were less extensive during the Riss II (Wartanian) Glaciation. During the Würm (Vistulian) Glaciation the glaciers were surprisingly large. This might have resulted from many factors, including changes in atmospheric circulation responsible for the distribution of precipitation, as well as changes in the position of the permanent snow limit due to climatic changes and/or neotectonic movements. Glaciers finally retreated from the Tatra Mts. by the end of the pre-optimal part of the Holocene.

10

Gosau-type conglomerate in the Rusinowa Polana area, Polish Tatra Mts: its relation to the Lower Subtatric Nappe

51%

Birkenmajer K.

Bulletin of the Polish Academy of Sciences. Earth Sciences

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2000

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tom Vol. 48, nr 1

117-133

EN

Unfossiliferous conglomerate consisting of fragments of Triassic through Lower Cretaceous sedimentary rock pebbles derived from the Lower Subtatric Nappe, occurs in the Rusinowa Polana area, Polish Tatra Mts (Carpathians). Thus far, this conglomerate was considered to represent a basal unit of the Eocene transgression deposits post-dating the meso-Cretaceous nappes. New field survey shows, however, that it takes part in architecture of the pre-Eocene Lower Subtatric Nappe system. The conglomerate, formally distinguished as the Rusinowa Conglomerate Formation (new formation), is here correlated with the Upper Cretaceous Gosau Group, as known from the Northern Limestone Alps. A post-Gosau but pre-Eocene, Laramian phase of folding is postulated as a new and important stage of tectonism in the Tatra Mts. The Rusinowa Conglomerate Formation is, moreover, displaced by numerous SW-NE-trending faults of post-Oligocene (probably Sarmatian) age.

11

Spatial relationship in interaction between glacier and permafrost in different mountainous environments of high and mid latitudes, based on GPR research

51%

Dobinski W. , Grabiec M. , Gądek B.

Geological Quarterly

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2011

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tom Vol. 55, No. 4

375-388

EN

Ground penetrating radar (GPR) surveys were conducted on both the glaciers and their forefields in the Tatra Mountains, Northern Scandinavia and on Spitsbergen – between the 49 degrees and 77 degrees latitudes. The results show that the glacial and periglacial environments interpenetrate. Permafrost is present in the glacier, and glacial ice may occur in the periglacial environment. What is common for both the environments is the perennial melting point surface, with the temperature close to 0°C. In the glacier it is the boundary of the cold-temperate transition surface and on the forefield – permafrost base.

12

The spatial patterns of the Tatra high - mountain landscape structure

51%

Boltižiar M.

Landform Analysis

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2009

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tom Vol. 10

11-17

EN

The paper focuses on the identification and classification of spatial patterns in the relation to landforms and geomorphic processes considering the middle-scale and micro-scale of the high-mountain landscape. These determine not only the shape of patches or the character of boundaries, but also the character of fragmentation, the heterogeneity of patches, the gradient and the tendency of patches development. Georelief, especially its spatial morphodynamic attributes, represents relevant phenomena of the landscape which facilitate to understand the scale and hierarchy of the landscape structure. The algorithm of this study is based on the spatial identification of landforms, processes and patterns considering large-scale aerial photographs, a field reconnaissance and the partial classification. The main aim of this paper is to create the classification system of spatial patterns as the physiognomic spatial attributes of the landscape structure mosaic in the high-mountain areas. The genesis of spatial structure patterns and their formation enables us to understand better the origin of the high-mountain landscape structure, its function and contents in this environment. Such a classification can be regarded as a basis for the quantitative statistic analyses of the landscape structure and for the detailed research of spatial patterns.

13

Applying geomathics to determination of landscape altitudinal zones in the mountains

51%

Guzik M. , Skawiński P.

Landform Analysis

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2009

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tom Vol. 11

25-32

EN

The paper presents a method enabling determination of the extent of landscape zones, based on the criterion of area coverage by vegetation. This method made it possible to objectively determine the extent of landscape zones both in the entire Tatra Mts. and in their particular parts. The altitude, at which dominant type of vegetation changes, is considered to mark the boundary of a landscape zone. Boundaries distinguished in this way in the Tatra Mts. are presently situated at: 1,510 m a.s.l. (forest zone), 1,730 m a.s.l. (subalpine zone), and 1,880 m a.s.l. (alpine zone).

14

Geophysical methods in research of permafrost in the Tatra Mountains and northern Scandinavia

51%

Dobiński W.

Landform Analysis

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2009

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tom Vol. 10

26-32

EN

A set of geophysical methods were implemented in the research conducted on permafrost of the Tatra Mountains and the Abisko area, Northern Sweden. Results of geophysical surveys show evidence of permafrost in both areas. Comparative studies on the occurrence of permafrost in the Tatras and in the Abisko area indicate that contemporary active as well as fossil permafrost might occur in both locations. Results of the electric resistivity, electromagnetic, shallow refraction seismic, and ground penetrating radar methods reveal similar results and might be successfully used in indirect research on permafrost in the mountainous regions.

15

Kartografia geologiczna Tatr

51%

Piotrowska K. , Wójcik Z.

Przegląd Geologiczny

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2008

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tom Vol. 56, nr 12

1069-1078

EN

The area in question represents northern part of the centralWest Carpathians and the boundary zone of Poland and Slovakia (before 1918 the boundary of Galicia and Upper Hungary). From the end of 18th century the authors of geological maps of this area were mostly Austro-Hungarian geologists, but also specialists from other countries. The first cartographic documents refer to the occurrence of mineral raw materials (Hacquet, 1796). A little later some elements of stratigraphy and tectonics were also considered (Staszic, 1815). Zejszner (1844) was the first to pay attention to biostratigraphy and this problem was continued by his followers. In the "Geological Atlas of Galicia" (1885-1914) the authors took into account tectogenesis, at first following the theory of contraction (Uhlig, 1897, 1899) and, subsequently, the concept of nappes (e.g. Lugeon, 1902, 1903; Uhlig, 1907; Limanowski, 1911; Rabowski & Goetel, 1925; Goetel &. Sokołowski, 1930; Guzik, 1939). Until the beginning of the 21st century, the number of cartographic works (maps and cross-sections) printed separately or as attachments and inserts within texts, reached more than 1000 positions. Particularly the cartography of the 20th century, including the map of the Tatra Mts. 1 : 10 000, represents very valuable basic material for the recently prepared "Detailed Geological Map of the Tatra Mts. 1 : 10 000".

16

The Little Ice Age in the High Tatra mountains

51%

Kotarba A.

Studia Quaternaria

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2006

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tom Vol. 23

47-53

EN

Climate deterioration of the Little Ice Age was manifested in the most spectacular way in the glaciated high mountains, but it should also be analysed in term of a climatic concept. Spatial variation in LIA climate is illustrated also in non-glaciated areas of the Northern Hemisphere in a broader contex. Extreme climatic events were forcing factors for mountain slope deformation by geomorphic processes in the High Tatra Mountains. The old chronicles, lichenometric dating of landforms and lacustrine sediments are used to determine the beginning of "Little Ice Age - type events" (about AD 1400) and its end (about AD 1920). During this time span the set of climatic conditions responsible for triggering high-energy geomorphic processes was recognised. The catastrophic hydrometeorological events were concentrated in certain periods. Clustering of weather anomalies and natural disasters resulting from them are discussed in the paper.

17

Kościeliska Marl Formation (Lower Cretaceous) in the Polish Western Tatra Mountainss: lithostratigraphy and microfossil zones

51%

Pszczółkowski A.

Studia Geologica Polonica

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2003

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tom Vol. 121

7-50

EN

The Kościeliska Marl Formation (Middle-Upper Berriasian to Lower Aptian) terminates the Lower Subtatric Succession in the Western Tatra Mountains. The Upper Berriasian to lowermost Hauterivian deposits of the lower part of this formation are subdivided into four members (Pod Furkaską Member, Kryta Member, Wściekły Żleb Member and Muráň Limestone Member), which are formally described. Two informal units are recognised in the Barremian-Lower Aptian deposits of the upper part of the formation: the nannoconid-foraminiferal limestone unit and glauconitic biocalcarenite bed. The Middle/Upper Berriasian to Upper Hauterivian deposits are subdivided into calpionellid zones and subzones. The upper part of the Kościeliska Marl Formation is biostratigraphically documented by planktonic foraminifers identified in thin sections. The following foraminiferal zones are recognised: Praehedbergella sigali, Blefuscuiana aptiana (new zone), Liliputianella similis, Blowiella blowi and Leupoldina cabri. In the type section, the total thickness of the Kościeliska Marl Formation is 272 m. In general, the deposits of this formation exposed in the Kościeliska Valley, although tectonically disturbed, appear to rest in normal position. The Kira Miętusia sub-unit of the Bobrowiec tectonic unit consists of two tectonic elements (slices): a larger one outcropped in the Wściekły Żleb-Zahradziska area and a smaller scale (composed of the Valanginian-Lower Aptian deposits), poorly exposed south of the Brama Kantaka gate. The studied sections are compared with the selected sections in Slovakia. Sedimentation of the Early Hauterivian Muráň Member (Western Tatra Mts) occurred approximately at the same time as the onset of the Muráň Formation deposition in the Eastern Tatra Mts. The Hauterivian Muráň Member of the Kościeliska Marl Formation and the Strážovce Turbidite Member of the Mráznica Formation (Strážovské Vrchy Mts) are not strictly coeval, the former unit being probably older than the latter one.

18

Inferred fault pattern and reinterpretation of architecture of the Siroka Javorinska Tectonic Depression, Eastern Tatra Mts, West Carpathians, Slovakia

51%

Birkenmajer K.

Studia Geologica Polonica

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2000

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tom Vol. 117

37-48

EN

Reinterpretation of Andrusov?s (1950), 1:25,000 scale, tectonic map of the Široká Javorinská (PL: Szeroka Jaworzyńska) Tectonic Depression, Eastern Tatra Mts, allows to distinguish a number of SSW-NNE-trending faults which cut both the Subtatric and the Hightatric tectonic units. Recognition of these faults, belonging to the post-Palaeogene (probably Sarmatian) fault system, have a bearing on correct interpretation of architecture of the area. Eight Hightatric tectonic units and five Subtatric tectonic units shown in maps and geological cross-sections, are based on reinterpretation of the data provided in papers by D. Andrusov, Z. Kotański and J. Lefeld. Some problems related to interregional correlation of these units, their age and direction of thrusting are outlined.

19

Budowa geologiczna jednostek reglowych Tatr Zachodnich

51%

Bac-Moszaszwili M.

Studia Geologica Polonica

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1998

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tom Vol. 111

113-136

PL

Omówiono budowę geologiczną jednostek reglowych w Tatrach na zachód od Doliny Suchej Wody. Składają się one z dwóch zasadniczych części: regli zachodnich zbudowanych z monoklinalnej kriżniańskiej jednostki Bobrowca i leżących na niej jednostek płaszczowiny choczańskiej oraz regli zakopiańskich zbudowanych z większej ilości drobnych jednostek tektonicznych płaszczowiny kriżniańskiej. Obie te części kontaktują ze sobą wzdłuż strefy nasunięcia regli zachodnich na zakopiańskie. Strefa ta jest jedną z poprzecznych dyslokacji o kierunku SW-NE przecinających jednostki reglowe i nadległy kompleks eoceński.W strefie reglowej Tatr dyslokacje te mają złożoną budowę i najczęściej charakter nasunięć lub uskoków pochylonych ku NW. Tworzą one system imbrykacyjny, interpretowany tu jako kontrakcyjny dupleks. Przesunięcia na poprzecznych uskokach powodują prawoskrętną rotację poszczególnych bloków jednostek reglowych.

EN

The Subtatric zone makes up a longitudinal belt along northern edge of the High Tatra Mts (Fig. 1). It is represented by the Križna nad the Choč nappes of the Inner Carpathians. The western subtatric zone. West of the Kościeliska Valley, the Bobrowiec unit makes up the main subtatric mass (Fig. 2). It consists of monoclinal Triassic, Jurassic and Lower Cretaceous units in the typical Križna nappe development. Its Middle Triassic competent dolostones are split into smaller blocks. Amplitude of fault displacement between these block dimnishes upward. The entire zone is cut by a large Siodło dislocation in its central part. Enrichment in iron and manganese ores (Krajewski & Myszka, 1958), is associated wit the dislocation (Fig. 7). The tectonic sole of the Bobrowiec unit is thrust onto the Hightatric zone along a shear plane (Fig. 6). The Bobrowiec unit is overlain by a higher nappe showing lithostratigraphic characteristics of the Choč nappe (Nemčok et al., 1996). In the western part of the Tatra Mts, it consists of Triassic formations, but in the Kościeliska Valley - of Lower Jurassic ones (Fig. 3). The whole nappe structure had been peneplenised during early Paleogene, being then covered with clastic sediments of Middle Eocene age (Fig. 4). At the Siodło dislocation, and the one that terminates the western Subtaric zone in the east (between the Kościeliska and Mała Łąka Valleys), changes occur in the composition and thickness of the basal Eocene beds (Bac, 1971). The Zakopane Subtatric zone. The Zakopane Subtatric zone makes up a complicated tectonic structure consisting of several nappe units composed of Triassic and Lower Jurassic formations in the Križna nappe development (Fig. 8). The zone consists of two belts of Middle Triassic dolostones with the so-called Czerwona Przełęcz syncline inbetween. The latter is built of Upper Triassic and Lower Jurassic shaly beds. Knowledge of the Subtatric Triassic lithostratigraphy (Kotański, 1963) allowed to state that this part of the Subtatric zone is composed of isoclinal slice elements usually in tectonically normal position (Guzik & Kotański, 1963). Tectonic model of the western Subtatric zone in the Western Tatra Mts. The set of tectonic scales in the Zakopane Subtatric zone makes a form of duplexes in the sense of contraction tectonics (see Boyer & Elliott, 1982; Mitra, 1986). It is proved by isoclinal, normal position of the majority of the scales, with shearing planes cutting horizons of incompetent Lower Triassic and Keuper shales, with passing of overthrust planes into shearing planes. The cross-sections (Fig. 10) are limited to structural elements visible in the field. They show a distinct imbrication of tectonic units in the Zakopane Subtatric zone. One must, however, subtract the effect of postorogenic tectonic processes and, first of all, of a rotational post-nappe tilt of the Tatra massif which caused the nothward dip of the Mesozoic Subtatric sequence that primarily was nearly flat or only slightly tilted toward the south (Bac-Moszaszwili et al., 1982). Within the Zakopane Subtatric zone, the duplexing process had embraced the sequence from the Triassic to the Lower Jurassic. Younger formations are unknown from that zone. Such a process did not take place in the Western Tatra Mts where the Lower Subtatric nappe include sedimentary formations from Middle Triassic through the Lower Cretaceous inclusively. The two above mentioned Subtatric zones namely the Zakopane and the western one, contact with each other in a tectonically complicated area of Upłaz Miętusi. It was argued (Bac, 1971) that there is no superposition of these two zones as supposed earlier by Rabowski (1954) and Kotański (1965). The tectonic structure of Upłaz Miętusi is best explained by an en bloc thrust of the western Subtatric zone onto the Zakopane one (Figs 2-5, 8, 9). The basal Eocene beds also take part in this thrust (Bac-Moszaszwili et al., 1979), and reverse folds so common in the Bobrowiec unit (Bac, 1971; Piotrowski, 1987) are associated with it. Displacement of an upper part of the Bobrowiec unit, recognized in the Chochołowska Valley, also shows a reverse character (Figs 2, 5). Folds in the Zakopane subtatric zone are of similar character (Fig. 11). The Subtatric units of the Zakopane zone are cut in several places by transverse, rather broad dislocations (Figs 8, 9), of fault overthrust character. As follows from studies by Iwanow (1965), and Bac-Moszaszwili & Rudnicki (1979), the above mentioned thrust zones are tilted toward NW, similarly as it is the case with the thrust of the western subtatric zone over the Zakopane one. They separate units differing in structure (Fig. 9) and are accompanied by small retrofolds usually of drag fold type (Fig. 11). The amplitudes of displacements vary in particular units. They are largest in the lowermost Suchy Wierch unit and smallest within the basal Eocene. This suggests a gradual development of this zone that started already during the nappe process, and was subsequently rejuvenated. The development of reverse structures, and transformation of the transverse dislocation zones into flat overthrusts dipping from NW toward SE, may have been caused by the formation of the Parnica Sigmoide at the western termination of the Tatra Mts (Bac-Moszaszwili, 1993) as well as by other tectonic phenomena that took place at the Inner/Outer Carpathian boundary. The last post-Paleogene stage of displacements along the mentioned transverse dislocations, shown in fig. 12, was a clockwise rotation of the Subtatric blocks. This may be one of effects of transpression and block displacements at the Inner/Outer Carpathian boundary. This direction agrees well with results of palaeomagnetic (Grabowski, 1995) and geotectonic studies (Birkenmajer, 1985). The morphological observations done by the authoress (1995) in the Subtatric units led to acceptation of such direction of recent rotation along the north-Tatra lineament.

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Recent results of the Dye Tracer Tests of the Chochołowskie Vaucluse Spring karst system (Western Tatra Mts.)

51%

Barczyk G.

Acta Geologica Polonica

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2004

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tom Vol. 54, no. 1

169-177

EN

The region of the Bobrowiec Massif, crucial in underground flows within the Chochołowski Stream catchment area, was not studied in details until the 50ies. The Chochołowskie Vaucluse Spring is recharged mainly by karst systems, including that of the Szczelina Chochołowska - Jaskinia Rybia caves. The remaining 20% of water in the system comes from surface waters of the Chochołowski Stream. First succesful dye tests were conducted on this system in 1971/1972. The paper presents data and interpretation of the recent dye-tracer experiments for the Chochołowskie Vaucluse Spring recharge area. The results of these tests prove that the connection between the Szczelina Chochołowska - Rybia caves karst system and the Chochołowskie Vaucluse spring is of a karst-fissure character. This hydraulic connection is a typical example of a sub-channel circulation, where flow through a karst-fissure system takes place beneath the bottom of an existing river channel. Comparing the time of dye flow through the system with water stages indicates that the system of fissures linking the sinkhole zone with the vaucluse spring is at least three fold. The inverse relation between watermark stands reflecting the degree of watering in the massif and the time, at which dye penetrates the system, is also distincly visible.