Geology of Slovakia

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Geological map of Slovakia

The geology of Slovakia is structurally complex, with a highly varied array of mountain ranges and belts largely formed during the Alpine orogeny in Mesozoic and Cenozoic eras and with relicts of older Variscan structures of Paleozoic age.[1][2] The internal zones of the West Carpathian orogen collapsed during Paleogene forming the Central Carpathian Paleogne Basin and later in Miocene the Pannonian Basin and Carpathian volcanic chain were formed.[3][4]

Stratigraphy, tectonics & geologic history[edit]

Most of Slovakia is situated within the West Carpathian orogenic belt, except for the east of the country which is in the East Carpathians. However, the geological boundary does not coincide with the geographical one. A large area in the southern part of Slovakia is covered with Miocene sediments of the Pannonian Basin system. The West Carpathians are Mesozoic to Cenozoic in age. The internal zones were formed on the collapsed Variscan crust during Late Paleozoic and Mesozoic extension.

Outer Western Carpathians[edit]

Marl from the Pieniny Klippen Belt at Horné Srnie quarry

The Outer Carpathians represent a externides of the Inner Carpathian crustal scale thick-skinned nappes.

Internal Western Carpathians[edit]

  • Gemericum: the structurally highest thick-skinned crustal scale unit composed of Cambrian or Ordovician through Triassic age phyllite, metaquartzite, lydite (black chert) and crystalline limestone partly replaced with siderite belonging to the Gelnica and Rakovec Group. Five to 10 kilometers thick in the Spišsko-gemerske rudohorie Mountains. Also contains marine rocks from the Carboniferous and Permian volcanic rocks and Permian granite intrusions. The Gemericum was thrust to the North above the Veporicum unit in mid-Cretaceous. The contact is marked by the Lubeník-Margecany shear zone.[5]
  • Veporicum: middle thick-skinned crustal scale unit formed by Variscan granites and medium- to high-grade metamorphic rocks, mostly gneisses, amphibolites and mica-schists. Also contains Late Paleozoic to Mesozoic sedimentary cover, often with varying degrees of Alpine metamorphism.[6] The contact with the underlying Tatricum is marked by the Čertovica shear zone.[7] The Veporicum represents the axial zone of West Carpahtian orogen affected by pervasive Alpine metamorphism and exhumation.[8] The complex of Muráň orthogneiss represents one of the oldest rocks in the West Carpathians.
  • Tatricum: lower thick-skinned crustal scale unit with similar composition as Veporicum, containing Variscan granites and gneiss, and Mesozoic sedimentary cover.[9] Overlain by the Fatric and Hronic nappes.
  • Meliaticum: Represents Jurassic subduction melánge. Containing Permian gypsum, Triassic limestones and basalts as well as serpentinte as blocks in Jurassic claystones and shales. Represents a suture after closure of the Meliata-Hallstatt ocean. The Melaticum usually occurrs in tectonic windows within the Silica Nappe (e.g., at type locality near Meliata village) and often in hangingwall of Gemericum (e.g, near Jaklovce village).
  • Bôrka Nappe: A narrow belt between Slovak Karst and Gemericum with glaucophanitized, thus affected by HP/LT metamorphism, basic volcanites and other rocks. Most of the protolith formerly belonged to Gemeric rocks. Usually considered as part of Meliaticum.
  • Tornaicum: nappe unit in the footwall of Silicium, affected by low pressure metamorphism, containing Triassic metacarbonates of deep water origin.
  • Silicicum or Silica Nappe: thin-skinned nappe, with up to 1.2 kilometer thick Triassic Wetterstein Limestone. The karst plain of the Slovak Karst are formed within the Silica Nappe. It did originally include Jurassic rocks, but these have mostly eroded away. The nappe was emplaced in Late Jurassic or earliest Cretaceous. Represents structurally highest nappe unit of the West Carpathians.
  • Hronicum or Choč Nappe: thin-skinned nappe system[10] composed of Carboniferous to Lower Cretaceous rocks, mostly limestones (e.g., Wetterstein and Reifling limestones) and dolomites (Ramsau and Wetterstein), locally also thick shales and sandstones of Lunz Formation. Also includes thick Late Paleozoic volcano-sedimentary Ipoltica Group.[11] Represents structurally highest nappe above the Tatricum, ususally overlying Fatricum. Locally overlain by the Upper Cretaceous Gosau type basins (e.g. Brezová Group).[12]
  • Fatricum or Krížna Nappe: thin-skinned nappe composed of typical sequence of Triassic to Cretaceous limestones, dolomites, shales (e.g., Carpathian Keuper), marlstones (e.g., Allgäu Formation), radiolarites (Ždiar Formation) and sandstones is thrust over the Tatricum in Albian-Turonian.[9][8] The sedimentary sequence of Fatricum is similar to Tatric and Veporic sedimentary cover, and its knowledge is suitable from an educational point of view for understanding the development of the Internal Western Carpathians.[13]
  • Transdanubicum: Mesozoic nappe unit of Austroalpine affinity occurring in the basement of the Danube Basin south of the Raaba-Hurbanovo-Diosjenő fault zone.[14]
  • Zemplinicum: tectonic unit composed of Paleozoic basement and Upper Paleozoic to Mesozoic cover of uncertain tectonic affinity emerging from the basement of the East Slovak Basin in the Zemplín Mountains.

Important nappe stacking of the Internal Western Carpathians occurred gradually since the early Cretaceous. With peak metamorphism in the core of the internal zones of the orogen at approx. 120 - 80 million years ago.[8]

Cenozoic (66 million years ago-present)[edit]

Neogene andesite from Krupina

In the zone surrounding the Pieniny Klippen Belt, sedimentation was not interrupted and continued from the Late Cretaceous to Paleocene in Gosau type basins, forming the Myjava-Hričov Group including the Súľov Paleogene. Conglomerates, marlstones as well as the Kambühel Limestone were deposited in this period.[15]

Another marine transgression flooded the region from the vicinity of the Flysch Belt into the area of the Internal West Carpathians during the middle Eocene represented by the Sub-Tatra (or Podtatranská) Group or the Central Carpathian Paleogene Basin. Paleogene sediments are found in the Orava, Liptov, Spiš, Žilina and Podhale depressions. Conglomerates are common as the bottom of the succession, overlain by flysch (alternating sandstones and claystones).[16] At the edge of the subducting Flysch Belt, sedimentary rocks are up to four kilometers thick. The Central Carpathian Paleogene Basin rocks are usually not folded, however, local backthrusting was documented.[17]

Molasse deposits laid down in the Oligocene span into southern Slovakia from the Pannonian Basin in Hungary. The back-arc molasse formed several large basins, including the Vienna Basin, Danube Basin, South Slovak Basin and East Slovak Basin in the Neogene (the Danube, South Slovak and East Slovak are all subdivisions of the larger Pannonian Basin).[18] The basins are filled with the sediments associated with the Paratethys Ocean, up to five kilometers thick. Shales and marls are particularly common, intercalated with sandstone, tuff, conglomerate and algal limestones. Sediments became brackish over time as the Paratethys was isolated from the rest of the world's oceans since Sarmatian to Panonian. Overall, the basins are split up by numerous faults and small grabens, such as the Trenčín, Ilava, Horná Nitra Basin, Turiec Basin, Žiar Basin and Orava Basin, often filled with lake sediments.[4]

The volcanic activity was important in the Miocene especially in the Central and Eastern Slovakia.[19] Geophysical research and boreholes have shed light also on the buried volcanic rocks in the Danube Basin. The buried centers were at Šurany or Kráľová.[20] The volcanic rocks are found throughout the Central Western Carpathians and eastern Slovakia. The volcanism was related to the subduction of the Flysch Belt and back-arc extension of the Pannonian Basin.[6] The main phase of volcanism occurred in Badenian and Sarmatian.[21] It is represented by andesite, dacite and rhyolite.[22] Intrusion of granodiorite is known in the area of Hodruša and Banská Štiavnica.[23] Youngest late Miocene/Pliocene to Quaternary volcanic activity was represented by alkaline basalts to basanites.

A swarm of andesite dikes is also documented in the Pieniny Klippen Belt, however, the Cenozoic volcanic activity was negligible compared to the aforementioned.

In the Upper Pliocene, prior to the Quaternary glaciations Slovakia had a subtropical climate akin to Mediterranean climate.[24]

Quaternary[edit]

The Quaternary glaciations identified in Slovakia are, from oldest to youngest: Donau, Günz, Mindel, Riss and Würm.[24] During these glaciations glaciers extender downhill from the High Tatras and nonglaciated uplands were subject to frost weathering and solifluction.[24] Deflation of soils is also evident in mountaineous locations.[24]

Peat, eolian wind-blown sands, fluvial sand and gravel and loess are all typical Quaternary sediments, formed in the past 2.5 million years old and dominating the surface of Slovak lowlands.[25] The loess sheets of Slovakia are named, from the lowest to the highest W1, W2 and W3. In between W1 and W2 lies a layer of black-earth soil and between W2 and W3 lies an incipient soil which in parts is gleyed or cryoturbated.[24]

The Váh River has up to seven terraces of sand and gravel. Travertine is also common, including travertine which preserved a cranial mold of a Neanderthal from Gánovce. Moraine formations remain in the high mountains from the Pleistocene glaciations.[25]

Economic geology[edit]

The moderately metamorphosed Spišsko-gemerské rudohorie Mts. formed by Paleozoic rocks of Gemericum hosts veins of siderite, chalcopyrite and tetrahedrite along with the Veitsch-type magnesite. Permian rocks often hold uranium ore.[26]

The Kremnica and Štiavnica Mountains formed by the Miocene volcanic rocks have polymetallic lead, zinc, copper, gold and silver veins.

Salt is found in the Neogene East Slovak Basin and brown coal is extracted from both the Handlová-Nováky Basin and the Modrý Kameň-Potor Basin. There are small deposits of natural gas and oil in the Neogene strata of the Vienna Basin together with older Triassic rocks.[27]

References[edit]

  1. ^ Moores, E.M.; Fairbridge, Rhodes W. (1997). Encyclopedia of European & Asian Regional Geology. Springer. pp. 656–665.
  2. ^ Plašienka, D., Grecula, P., Putiš, M., Kováč, M., a Hovorka, D., 1997: Evolution and structure of the Western Carpathians: An overview. In Grecula, M., Hovorka, D. a Putiš, M., Geological Evolution of the Western Carpathians. Mineralia Slovaca – Monograph, Bratislava, 1 – 24.
  3. ^ Kováč, M., Plašienka, D., Soták, J., Vojtko, R., Oszcypko, N., Less, Gy., Cosovic, V., Fügenschuh, B. & Králiková, S., 2016: Paleogene paleogeography and basin evolution of the Western Carpathians, Northern Pannonian domain and adjoining areas. Global and Planetary Change 140, 9-27.
  4. ^ a b Kováč, M., 2000: Geodynamický, paleografický a štruktúrny vývoj karpatsko-panónskeho regiónu v miocéne: Nový pohľad na neogénne panvy Slovenska, Veda vydavateľstvo Slovenskej akadémie vied, Bratislava, 202 pp.
  5. ^ Andrusov, D., Bystrický, J. & Fusán, O., 1973: Outline of the structure of the Western Carpathians. Guide book, X Congress CBGA, GÚDŠ, Bratislava, 44 pp.
  6. ^ a b Biely, A. (ed.) Bezák, V., Elečko, M., Kaličiak, M., Konečný, V., Lexa, J., Mello, J., Nemčok, J., Potfaj, M., Rakús, M., Vass, D., Vozár, J. & Vozárová, A., 1996: Geological map of Slovak Republic 1 : 500,000 / Geologická mapa Slovenskej republiky M = 1 : 500 000. MŽP SR, Geologická služba Slovenskej republiky. Bratislava.
  7. ^ Kriváňová, K., Vojtko, R., Droppa, D.M., Gerátová, S., 2023: Deformation record and revised tectonic evolution of the Nízke Tatry Mts. in the Tatric – Veporic junction area: Insights from structural analysis. Geol. Carpathica, 74, 3, 197-210.
  8. ^ a b c Plašienka, D. 2018: Continuity and episodicity in the early Alpine tectonic evolution of the Western Carpathians: How large-scale processes are expressed by the orogenic architecture and rock record data. Tectonics, 37, 2029–2079. https://doi.org/10.1029/2017TC004779
  9. ^ a b Hók, J., Pelech, O., Teťák, F., Németh, Z. & Nagy, A., 2019: Outline of the geology of Slovakia (W. Carpathians). Miner. Slovaca, 51, 1, 31 – 60.
  10. ^ Kováč, P. & Havrila, M., 1998: Inner structure of the Hronicum. Slovak Geological Magazine, 4, 4, 275 – 280.
  11. ^ Vozárová A. & Vozár J., 1981: Litostratigrafická charakteristika mladšieho paleozoika hronika. Mineralia slovaca, 13, 5, 385–403.
  12. ^ Samuel, O., Salaj, J. & Began, A., 1980: Litostratigrafická charakteristika vrchnokriedových a paleogénnych sedimentov Myjavskej pahorkatiny. Západné Karpaty, Séria Geológia, 6, s. 81 – 111
  13. ^ Mišík, M., Chlupáč, I. a Cicha, I., 1985: Historická a stratigrafická geológia. SPN, Bratislava, 541 s.
  14. ^ Hók, J., Šujan, M., Šipka, F., 2014: Tektonické členenie Západných Karpát - prehľad názorov a nový prístup. Acta Geologica Slovaca, 6, 2, 135 – 143.
  15. ^ Samuel, O., Borza, K. & Köhler, E., 1972: Microfauna and litostratigraphy of the Paleogene and adjacent Cretaceous of the middle Vah valley (West Carpathians). Bratislava, Geol. ústav. D. Štúra, 246 pp.
  16. ^ Gross, P., 2008: Litostratigrafia Západných Karpát: Paleogén – Podtatranská skupina. Štátny geologický ústav Dionýza Štúra, Bratislava. 78.
  17. ^ Pelech, O. & Olšavský, M., 2018: Post-early Eocene backthrusting in the northeastern Strážovské vrchy Mts. (Western Carpathians). Mineralia Slovaca, 50, 2, 147 – 156.
  18. ^ Vass, D., Began, A., Gross, P., Kahan, Š., Krystek, I. Köhler, E., Lexa, J., Nemčok, J., Ružička, M. a Vaškovský, I., 1988: Regionálne geologické členenie Západných Karpát a severných výbežkov Panónskej panvy na území ČSSR. Mapa 1 : 500 000. Geologický ústav Dionýza Štúra, Bratislava.
  19. ^ Konečný, V. Lexa, J., Šimon, L. a Dublan, L., 2001: Neogénny vulkanizmus stredného Slovenska. Mineralia Slovaca, 33, s. 159 – 178
  20. ^ Rybár, S., Šarinová, K., Joirdan, F., Mayers, C., Sliva, Ľ., 2024: Middle Miocene volcanic flare up preceding and synchronous with the Langhian/Serravallian sea-level decline in the North Pannonian Basin: Insights from 40Ar/39Ar dating, geo-seismic analysis and 3D visualization of the subterranean Kráľová stratovolcano. Basin Research, 36, e12844, 1-31, https://doi.org/10.1111/bre.12844
  21. ^ Pécskay Z., Lexa J., Szakács A., Seghedi I., Balogh, K., Konečný V., Zelenka T., Kovacs M., Poka, T., Fulop, A., Marton, E., Panaiotu, C., Cvetkovic, V., 2010: Geochronology of Neogene-Quaternary magmatism in the Carpathian arc and Intra-Carpathian area: a Review, Geol. Carpath., 2006, 57, 511-530.
  22. ^ Lexa, J., Seghedi, I., Németh, K., Szakácz, A., Konečný, V., Pécskay, Z., Fülöp, M., 2010: Neogene-Quaternary Volcanic forms in the Carpathian-Pannonian Region: a review. Central European Journal of Geosciences, 2, 3, 207 – 270
  23. ^ Kohút, M., Danišík, M., 2017: Rapid cooling and geospeedometry of granitic rocks exhumation within a volcanic arc: A case study from the Central Slovakian Neovolcanic Field (Western Carpathians). Island Arc, 26:e12201, https://doi.org/10.1111/iar.12201
  24. ^ a b c d e Vaškovský, Imrich; Vaškovská, Eugenia (1981). "The development of the natural landscape in Slovakia during the Quaternary". Biuletyn Peryglacjalny. 28: 249–258.
  25. ^ a b Moores & Fairbridge 1997, p. 663.
  26. ^ Kohút, M., Trubač, J., Novotný, L., Ackermann, L., Demko, R., Bartalský, B., Erban, V., 2013: Geology and Re–Os molybdenite geochronology of the Kurišková U–Mo deposit (Western Carpathians, Slovakia). Journal of Geosciences, 58, 271–282, https://doi.org/ 10.3190/jgeosci.150
  27. ^ Moores & Fairbridge 1997, p. 664.
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