Veress Márton: A Bakony természettudományi kutatásának eredményei 23. - Covered karst evolution... (Zirc, 2000)

RESEARCH HISTORY

The extension of sequences containing main karst water and karst water storeys is delimited (JASKÓ 1961). It is described that main karst water is stored in „Hauptdolomit", Dachstein and Dachstein-type Liassic Limestones, the aquifers of karst water storeys are Alban Requienian, Upper Cretaceous Hippuritic and Middle Eocene Nummulitic Limestones, while karst water storeys below the main karst water occur in Megyehegy Dolomite, „Muschelkalk" and Füred Limestone. The flow conditions of main karst water and changes in karst water table are studied in detail (BÖCKER 1972) and subsidence of karst water table as a result of mining are investigated (SÁRVÁRY 1971). Establishing a network of observation wells (BÖCKER 1977), detailed and reliable maps of karst water table have been prepared in recent decades. With the abundant data, attempts have been made to construct a model of the main karst water system (SZILÁGYI 1976; CSEPREGI 1995). Paleokarst In the Transdanubian Mountains several stages of karstification have been identified: Tithonian-Aptian, pre-Senonian, pre-Eocene, pre-Oligocene, pre-Pannonian and neokarstification (VÉGH 1976). The paleokarst landform assemblage was first mentioned by FÖLDVÁRI (1933), who claimed that the manganese ore at Úrkút and Eplény accumulated in pre-Eocene dolines. Dolomite pulverisation is also regarded a consequence of paleokarstification. The paleokarst landform assemblage is particularly well exposed in and described from quarries and mines. The paleokarst landscape has been described in numerous papers (BÁRDOSSY 1977; BÁRDOSSY-PATAKI-NÁNDORI 1983; PATAKI-NYIRŐ 1983; MÉREI-ERDÉLYI 1989) and exhumed paleokarst landforms have also been studied (SZABÓ 1966; VERESS-FUTÓ-HÁMOS 1987; VERESS-FUTÓ 1990; VERESS 1991). The buried paleokarst of Triassic dolomite (Megyehegy Dolomite) in the mountains, Which developed on the Triassic surface and was later covered by younger Triassic limestone (Berekhegyi Limestone), has been studied by KORPÁS (1999): BULLA (1958, 1964) and LÁNG (1952) interpreted the surfaces of blocks at various elevations as planated surfaces of various age. Their starting point was that tropical peneplanation was continuous from the Upper Cretaceous to the Middle Miocene. During the prolonged peneplanation, however, karst landforms must have been destroyed entirely. According to PÉCSI (1980, 1991) tropical planation ceased by the end of the Cretaceous. As a consequence, a peneplain with conical karst developed and its dissection began in the Upper Cretaceous. The oscillating movements and burial of blocks favoured the partial preservation of the paleokarst landform assemblage. On exhumed blocks karstification could resume but this time outside the tropical belt. According to SZABÓ (1956), this primarily resulted in cavity formation. SZABÓ (1956) claims that fossilised karst features did not activate in a later stage of karstification. Consequently, the landforms resulting from a recent stage of karstification cannot be considered further developed varieties of the products of older karstification periods. The various authors have described the following paleokarst features: - karstic plains, peneplains (SZABÓ 1956, PÉCSI 1980), tower karsts and planated karsts (BULLA 1968); - paleopoljes (SZABÓ 1956,1966), denudation poljes (BULLA 1968); - basins bordered by dolomite hillocks (VADÁSZ 1946); - shallow and deep dolines (PATAKI 1983) and steep-sided dolines (SZABÓ 1956); - composite dolines (BÁRDOSSY-PATAKI-NÁNDORI 1983);