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2 Pol ish Geo log i cal In sti tute -Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land Jurewicz E. and Stępień U. (2013) Tec ton ics of the Chęciny Anticline (Holy Cross Mts., cen tral Po land) in the light of new carto graphic data and cal cite vein anal y sis (re ply). Geo log i cal Quar terly, 57 (1): 181-186, doi: 10.7306/gq.1069 In our pa per (Jurewicz and Stępień, 2012) we pro posed a sim ple method for ex ten sion mag ni tude es ti ma tion and we dem on strated the pres ence of an anticline to the south of the Rzepka Syncline. Mastella et al. (2013) chal lenge our newly found out crops of Cam brian rocks and their in ter pre ta tion.Cam brian rocks at point "B" (Jurewicz and Stępień 2012: fig. 2A), which could in di cate the lo ca tion of the anticline axis, were un cov ered in earth works ex ca vated dur ing the fenc ing-off of a gas sta tion by the E7 motor way in 2006. Not with stand ing two tiny dip sym bols point ing to south-dip ping De vo nian strata, can be seen in Czarnocki's (1938) map south of Rzepka with help of a mag ni fy ing glass. This map had been pro duced be fore stone be gan to be ex ploited in Korzecko Quarry at Rzepka Hill -thus when nu mer ous De vo nian ex po sure were scat tered across the area. Both Mastella et al. (2013) and many oth ers be fore them (e.g., Hakenberg, 1973;Konon, 2006;Jurewicz and Stępień, 2012) have not no ticed these dip sym bols on Czarnocki's (1938) map.An other prob lem is a gap in De vo nian out crops be tween Rzepka and Sosnówka. Tri as sic out crops shown on pho tographs in Mastella et al. (2013) in di rectly point to the ab sence of De vo nian, be cause the lat ter would form pos i tive mor phol ogy. Those pho tos thus would sup port the idea that Tri as sic palaeomorphology has been un cov ered, with Tri as sic fill ing nat u ral de pres sions cre ated due to e.g., un der ly ing soft Cambrian rocks -a phe nom e non com monly seen in this area. More over, Mastella et al. (2013) do not at tempt to ex plain the pres ence of Cam brian rocks that they found ( fig. 1C). 30-50 cm thick Cam brian regolith over ly ing weath ered Tri as sic rocks and ex tend ing over sev eral hun dreds of square metres can not be ex plained as gla cial or i gin. We sug gest that the rea son is a pe riod i cally open fault fis sure along which Cam brian could have flowed to the sur face both in the past and at pres ent. It may have pierced thin Buntsandstein de pos its. In 2008 we were lucky enough to find ex actly the place where this Cam brian emerges at the sur face. We are con scious that we have no fi nal proof, but we do have a con sis tent hy poth e sis.The an swers to the re main ing ob jec tions ar tic u lated in Mastella et al. (2013) have been or ga nized by themes.

The Pieniny Klippen Belt (PKB) is a narrow structure delineating the boundary between the Central and Outer Carpathians. It is built of nappes stacked during the Cretaceous and Paleocene and then re-folded in the Miocene during the formation of the Outer Carpathian overthrusts. The internal structure of the PKB at the Polish/Slovakian border first formed during northward nappe thrusting processes, which were most intense at the turn of the Cretaceous to the Paleocene. A secondary factor is the change in strike of the PKB turning from W-E to WNW-

Abstract:The Pieniny Klippen Belt is a narrow, complex structure stretching along a tectonic boundary between the Central and Outer Carpathians. Its formation involved two main evolutionary stages, the first, related to Late Cretaceous-Paleocene folding and thrusting, and the second, associated with Miocene orogenic events in the Outer Carpathians. Interactions between the Pieniny Klippen Belt and Outer Carpathians during both the sedimentation and deformation stages have resulted in the establishment of a peri-klippen transitional zone (named the Šariš Transitional Zone), in which the tectonic deformation effects gradually decrease towards the north. The stratigraphy and tectonic position of this zone have been controversial for decades. The key stratigraphic problems concern 1) the lithologic identity and position of the Szlachtowa ("black flysch"), Opaleniec and Pieniny formations and 2) the relation of the Jarmuta Formation, associated mainly with the Šariš Transitional Zone, to the Szczawnica and Zarzecze formations of the Magura Nappe. We provide an early Paleogene dinoflagellate cyst stratigraphic record of deposits that, according to some recent reinterpretations, represent the Neogene "Kremna Formation". The legitimacy of new lithostratigraphic assignments of the "Kremna Formation" at Jaworki is put into question upon the basis of the primacy of units introduced for the same strata earlier.

63 Abstract Dąbrowska, M. and Jurewicz, E. 2013. Character and structural evolution of the Mała Łąka Fault in the Tatra Mts., Carpathians, Poland. Acta Geologica Polonica, (1), 137-151. Warszawa. The Mała Łąka Fault in the Tatra Mts. is a synsedimentary normal fault responsible for the variable thickness of Eocene deposits in the area. Its main activity took place in the interval from the sedimentation of red conglomerates to the appearance of nummulitic limestones. The estimated throw is up to 350 m. Near the northern margin of the Tatra Mts., the trend of the fault changes from N-S to NE-SW. This part of the fault could have been activated during the Neogene uplift of the Tatra Mts. and rejuvenated as a sinistral fault. In the upper reach of the Mała Łąka Stream, the fault trend does not follow the course of the Mała Łąka Valley. Here, the flowing stream waters used extensional fractures within a damage zone associated with the Mała Łąka Fault rather than the lithological boundary at the tectonic contact between the Triassic dolomites and the Eocene conglomerates. The fault has a hingelike character; its hinge was located in the present-day Kościeliska Valley, c. 2.5 km west of the Mała Łąka Valley.