Sev eral tufa com plexes are known in the Slo vak Karst which is a typ i cal karst area of a tem per ate cli mate. This area is built of Me so zoic car bon ates, mainly Tri as sic in age. The karst sys tems drain car bon ate pla teaux and lead wa ter to resurgences located in val leys which are up to 300 m deep. Be low the resurgences there are Ho lo cene fos sil tufa de pos its that ex ceed 12 m in thick ness. The tufas in clude stromatolite, moss, phytoclastic, oncoidal, and intraclastic fa cies. Ex ten sive bar rages which once dammed the up per reaches of the streams were formed in nar row val leys. They are com posed pre dom i nantly of moss fa cies and stromatolites, with sub or di nate oncoidal and phytoclastic fa cies. Phytoclastic, oncoidal and intraclastic fa cies are dom i nant in dammed seg ments of streams, and in clude gas tro pod shells and char coal frag ments. Some small moss cushions are also de vel oped. Bar rages and dammed ar eas formed in a lon gi tu di nal flu vial depositional sys tem. Con versely, below resurgences lo cated on pla teau slopes tufas of a perched springline depositional sys tem were formed. These com prise de pos its of prograding cas cades con structed by moss, phytoclastic and stromatolitic fa cies. Pres ently, the tufas ana lysed are in ac tive. They stopped grow ing in the Late Ho lo cene time, af ter which there was abrupt in ci sion of the streams. This caused downcutting into Ho lo cene tufas, in some places reach ing Me so zoic bed rock. At pres ent tufa is be ing pre cip i tated from streams in all the sites stud ied.Key words: flu vial tufa, perched spingline tufa, ra dio car bon dat ing, Qua ter nary, Late Ho lo cene tufa de cline, Cen tral Carpathians.
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