Przegląd Geologiczny, vol. 46, nr 8/2, 1998 geofizycznych i geologicznych (zagadnienia wybrane). Ref. sesji, Kra­ PERYT D. 1991 - Kokkolity z osadów badenu zatoki rzeszowskiej. ków 30 marca 1989. Komis. Tektoniki Kom. Nauk Geol. PAN, Kraków, [In:] . Paleontologia a batymetria. Wyd. AGH, 24: 41-43. 1989: 170-195. PERYT T. M., PERYT D., SZARAN 1., HAŁAS S. & JASINOWSKI M. NEY R. 1968 - Rola rygla krakowskiego w geologii zapadliska przed­ 1998 - O poziomie anchydrytowym badenu w otworze wiertniczym Ry­ karpackiego i rozmieszczeniu złóż ropy i gazu. Pr. GeoI. Kom. Nauk Ge­ szkowa Wola 7 k. Jarosławia (SE Polska). BiuI. PIG, 379: 61-78. ol. PAN Oddz. w Krakowie, 45: 7-82 ROGL F. 1995 - Stratigraphis Tabelle des Obereozan bis Pliozan mit NOWAK W. 1959 - Geologia brzegu karpackiego między Andrycho­ der Standard-Stufengliderung und den Stufen fUr die Zentrale und wem a Sołą. BiuI. Inst. Geol., 131: 149-195. Ostliche Paratetchys. [In:] Die Molassezone in Oberosterreich und Salz­ NOWAK W. 1966 - Szczegółowa mapa geologiczna Polski (bez utworów burg (Roetzel R., Krenmayr H.G.) Exkursion B2. ExkursionsfUhrer SE­ czwarrtorzędowych) . Region Karpat i Przedgórza (wydanie tymczasowe), DIMENT'96, Wien, 1996. arkusz Wadowice M 34-75B, arkusz Kęty M 34-75 A. Warszawa. SZYMAKOWSKA F. 1986 - Zjawiska olistostromowe w obrębie mio­ OSZCZYPKO N., STUCHLIK L. & WÓJCIK A. 1991 - Startigraphy ceńskiego rowu przedgórskiego w rejonie Cieszyn-Zamarski-Dębowiec offresh-water Miocene deposits ofthe Nowy Sącz Basin. Polish Wes­ na podstawie danych z głębokich wierceń. Spraw. Pos. Komis. Nauk. tern Carpathians. BulI. Pol. Acad. Sc. Earth Sc., 39: 433-445. PAN w Krakowie, 27: 215-216. OSZCZYPKO N., OLSZEWSKA B ., ŚLĘZAK J. & STRZĘPKA J. TOŁWIŃSKI K. 1950 - Brzeg Karpat. Acta Geol. PoL, l: 13-35. 1992 - Miocene marine and brackish deposits of the Nowy Sącz Basin ŻYTKO K.,GUCIK S., RYŁKO W., OSZCZYPKO N., ZAJĄC R., (Polish Western Carparhians). New lithostratigraphic and biostratygrap­ GARLICKA 1., NEMCOK J., ELIAS M., MENCIK E., DVORAK J., hic standards. BulI. Pol. Acad. Sc. Earth Sc., 40: 83-96. STRANIK Z., RAKUS M. &MATEJOVSKA O. 1989 - Geologica1 PERCH-NIELSEN K. 1985 - Cenozoic calcareous nannofossils. [In:] Map of the Western Outer Carpathians and their foreland without Bolli H.M., Saunders J.B. & Perch Nielson K. (eds) - Plankton strati­ Quaternary formations l : 500000. [In:] Geological atlas ofthe Western graphy. Cambridge University Press: 427- 554. Outer Carpathians and their Foreland. Wyd. Geol., Warszawa. Thermal waters of the Polish part of the Carpathians Józef Chowaniec*, Danuta Poprawa* Occurrences oj thermal waters, their TDS and chemistry are briejly characterised. When considering usage, the most important are thermal waters occurring in the Podhale Basin due to their high temperature (to 82°C at the suiface), yield (to 270 m3/s - outflow) and 3 low TDS (to 3 g/dm ). Thermal waters in the Podhale Basin are protected by a complex ojlow permeable or almost impermeable,jlysch rocks. Key words: Polish Carpathians, Tatra Mountains, Poland, Podhale, thermal waters, water wells, characterization Introduction Outer and Inner (Central) Carpathians, the latter inc1uding the Tatras, Podhale Basin, and Pieniny Klippen Belt (Fig. 1). The Carpathians have always attracted research interest In the Tatras two facial-tectonic series are distinguished: the as a potential groundwater reservoir, however, the literature southem, High-Tatric Series being widely spread and the de alin g with thermal waters of this region since the 1960s northem, Sub-Tatric Series extending as a narrow belt along was very scarce. A dynamie development of investigations the northem margin of the Tatras. The High-Tatric Series is on thermal waters in the Carpathians was initiated just in the built of Paleozoic, igneous and metamorphic rocks as weB 1960s (Sokołowski, 1973; Poprawa, 1978; Karnkowski & as of Mesozoic sedimentary rocks. The Sub-Tatric Series Jastrząb, 1994; Marszczek & Płochniewski, 1989; Chowa­ consists of nappes thrust over the folding High-Tatric Series niec & Poprawa, 1985, 1995; Ostrowicka-Chrząstowska & from the south. This proces s to ok place from the Upper Płonka, 1986; Chowaniec et al., 1997b). Cretaceous to the Middle Eocene. The Sub-Tatric Series is Polish Geological Institute has been participating in the built of sedimentary rocks of the Triassic-Jurassic-Creta­ investigations on thermal waters for over thirty years. ceous age. Thermal waters are specific groundwaters whose tempe­ The Podhale Basin, located between the Tatras and the rature at a spring outlet or at weB head outflow is at least Pieniny Klippen Belt, is filled up with Paleogene sandstone­ 20°C. In Poland thermal waters are known to occur in three shale deposits of the thickness reaching up to 3,000 m. These major regions of the country: the Polis h Lowland, the Sude­ deposits rest on the Mesozoic Tatric Units. The bottom, ten, and the Carpathians. transgressive part of the Paleogene is formed by ca1careous Thermal waters which might be of economic or balneo­ rocks developed as conglomerates, nummulite limestones logie importance have been identified in Podhale region, in and mudstones. Poręba Wielka, in the vicinity of Wiśniowa near Strzyżów, The Pieniny Klippen Belt, separated from the Podhale in Jaworze and Ustroń spas (Fig. 1). Basin (as from the Outer Carpathians) by a dislocation zone is built of ca1careous and sandstone-shale Jurassic-Creta­ Generał geołogicał characteristics ceous-Tertiary rocks. A number of separate tectonic-struc­ tural units are distinguished which can be traced along the The Carpathians show an extremely diversified geologi­ whole klippen belt. cal structure as to both their litho-facial development and The Outer Carpathians are built of some tectonic units tectonics. With respect to the geological diversity and histo­ of the lower order, strongly folded, faulted into blocks and rical development, the Carpathians are divided into the segments and thrust over each other (Fig. 1). These are: the Magura Nappe, Fore-Magura Unit, Dukla-Grybów Unit *Polish Geological Institute, Carpathian Branch, occurring in tectonic windows of the Magura Nappe, Dukla ul. Skrzatów 1,31-560 Kraków, Poland scales and folds, Silesian Nappe, Sub-Silesian Nappe and 770 Przegląd Geologiczny, vol. 46, nr 8/2, 1998 Tectonic units: SS - Sub-Silesian S - Silesian D - Dukla ~ external Carpathian overthrust G - Grybów ~ overthrusts of Carpathian units ..... M - Magura ...... SK - Skole extent of Neogene deposits Sl - Stebnik o borehole with thermal waters in Podhale Basin PPS - Pieniny Klippen Belt FWK - Podhale Basin • borehole with thermal waters in Outer Carpathians lM - Tatric Units prospective geothermal water areas N - Neogene deposits ~ Fig. 1. Tectonic map of the Polish Carpathians and location of geotherrnal water boreholes Skole Nappe. Particular units are developed as flysch, sand­ fonned that caused leaning of the Paleogene deposits from stone-shale deposits of the Upper Jurassic to the Lower their initial position. Then, an asymmetrical basin, delimited Miocene. by the Pieniny Klippen Belt in the north and the Tatras in the south, was formed. An upliftofthe Tatric massifbrought Thermal waters oC the Podhale Basin about formation of fissures and cracks, local folds and dislocations (sometimes of a regional extent) which have The Podhale Basin is built of Paleogene deposits under­ their sources in the Mesozoic rocks. The most important are lain by ca1careous Mesozoic rocks. A litho-stratigraphic faults of Jurgów-Trybsz, Biały and Czarny Dunajec, and profile of these deposits has been recognized best by bore­ Krowiarki (Fig. 2). holes Zakopane IG-l (Sokołowski, 1973) and Bańska IG-l Thermal waters in Podhale attracted the interest from the (Sokołowski,1985). previous mid-century, when Zejszner (1844) discovered the In subsequent years the boreholes which were located as spring of temperature of 20.4°C in Jaszczurówka. This is the shown in Fig. 2 provided a very advantageous infonnation. only naturai discharge of thermal waters in the area of the Results of the investigations show that the sub-Paleogene entire Carpathians. substratum is an extension of geological-structural elements The first hydrogeological drilling (to the depth of of the Tatric massif to which the Sub-Tatric and High-Tatric 150.3 m) was located in Jaszczurówka, in a direct neigh­ nappes belong. Moreover, in profile s of some deep drillings bourhood of the hot spring and aim at obtaining waters of out-of-sequence deposits (Sokołowski, 1973; Chowaniec, the temperature exceeding that of the spring. Indeed, at the 1989) as well as the facial elements similar to certain rock borehole depth of 20.0 m the temperature of water reached types of the Pieniny series were stated. After a retreat of the 22.7°C. However, the further drilling led to a decrease in U pper Cretaceous sea, a subsequent trans gression took place water temperature due to inflow of cool surface waters by a in the Middle Eocene that resulted in formation of conglo­ system of fissures. Therma1 waters of temperature of 36°C merates, limestones and dolomites in the initial phase. These were obtained for the first time in borehole Zakopane 10-1 0 deposits form a base member ofthe Podhale Paleogene. (Sokołowski, 1973), and then temperatures were 20 e in Then typical flysch deposits were fonned. Sediments of the borehole Siwa Woda IG-l (Chowaniec & Poprawa, 1985) ca1careous Eocene are know from numerous natural expo­ and 26°C in borehole Zakopane-2 (Małecka, 1981). sures at the outlets of the valleys of the Tatric massif and New interesting results referring to the occurrence of from the drillings made in the area of the Podhale Basin. thermal waters in the Podhale Basin and on their exploitation Directly on the transgressive deposits of the ca1careous possibilities were obtained from the investigations perfor­ Eocene rest the younger stratigraphic beds of the Paleogene med in five boreholes selected by the Carpathian Branch of - the Podhale flysch. The largest thickness of the latter, ca the Polish Geological Institute and Podhale Geotennia S.A.