Mastella L., Konon A., Dwornik M., Ludwiniak M., Rybak-Ostrowska B. and Śmigielski M. (2013) Tec ton ics of the Chęciny Anticline (Holy Cross Mts., cen tral Po land) in the light of new car to graphic data and cal cite vein anal y sis (dis cus sion). Geolog i cal Quar terly, 57 (1): 175-180, doi: 10.7306/gq.1070 Jurewicz and Stępień (2012) dis cussed the geo met ric recon struc tion of the Chęciny Anticline based on new map data. The two, newly found ex po sures of Cam brian rocks, not reported pre vi ously from the south ern limb of the fold, and fracture anal y sis based on data from Rzepka Quarry, en abled these au thors to pro pose dif fer ent in ter pre ta tions of struc tures mapped ear lier by Czarnocki (1938, 1948), Filonowicz (1967 and Hakenberg (1973). More over, Jurewicz and Stępień (2012) pro vided new in ter pre ta tions of the evo lu tion of the Chęciny Anticline, on as so ci ated trans verse faults and extensional fractures, as well as pro vid ing an es ti mate of the strain ra tio in the Kielce fold zone.Sev eral of their in ter pre ta tions are chal lenged in this dis cussion. Par tic u larly, we con sider that some of their ar gu ments, i.e. con cern ing the pres ence of Cam brian rocks at the lo ca tions shown by the au thors and re gard ing the ge om e try and for mation of folds, com po nents of move ment across the fault planes, their model of de vel op ment of the extensional frac tures, the tim ing of the struc ture's for ma tion, as well as their ter mi nol ogy are mis lead ing and are in need of amend ment.Jurewicz and Stępień (2012) de scribed "two new Cam brian out crops" lo cated near Chęciny: one lo cated to the west, and the sec ond to the east of Rzepka Hill. We have con ducted geolog i cal map ping in both ar eas. At the first lo ca tion, be low a thin clay layer with frag ments of quartzitic sand stone of prob a ble Cam brian age, we have found red ferruginous and si li ceous quartz sand stones rep re sent ing the Buntsandstein fa cies re ferable to the Lower Tri as sic, as well as Mid dle De vo nian dolomites (Fig. 1). At the sec ond lo ca tion, no frag ments of quartzitic sand stones that could be as signed to the Cam brian have been found. Only regolith was found there, with frag ments of white and yel low quartz sand stone, poorly ce mented and free of iron ox ides. The sand stone most prob a bly be longs to the Lower Tri as sic Buntsandstein fa cies.Based on data from those two out crops, Jurewicz and Stępień (2012) dis cussed the ge om e try of the fold pro file of the Chęciny Anticline in the Holy Cross Moun tains fold belt. They con sid ered that it formed due to diapiric-like move ments, with a lo cal de tach ment formed at the bound ary of com pe tent and incom pe tent rocks, and they have mis in ter preted Konon (2006) in sup port of their in ter pre ta tion. Konon (2006) merely sug gested that de tach ment ho ri zons played a sig nif i cant role in the de forma tion, al though not dur ing the "Al pine oro gen esis" as in dicated by Jurewicz and Stępień, but dur i...

1 Uni ver sity of War saw, Fac ulty of Ge ol ogy, ¯wirki i Wigury 93, 02-089 Warszawa, Po land £oziñski, M., Wysocka, A., Ludwiniak, M., 2015. Neo gene ter res trial sed i men tary en vi ron ments of the Orava-Nowy Targ Basin: a case study of the Oravica River sec tion near Èimhová, Slovakia. Geo log i cal Quar terly, 59 (1): 21-34, doi: 10.7306/gq.1209The Orava-Nowy Targ Ba sin is an intramontane de pres sion lo cated at the bor der of the In ner and Outer Carpathians. It is filled mostly with fine-grained ter res trial and fresh-wa ter de pos its of Neo gene and Qua ter nary age, which re cord the structural evo lu tion and de nu da tion pro cesses of the sur round ing re gions: Orava, Podhale, and the Tatra Mts. The Orava-Nowy Targ Ba sin fill was stud ied in the Oravica River sec tion, which re veals 90 m thick Neo gene de pos its and al lows ob ser va tion of their lat eral di ver sity. Fif teen lithofacies and seven fa cies as so ci a tions dis tin guished here doc u ment the depositional evolu tion of the ba sin fill, start ing from hill-slope de bris flow through silt turbidite-bear ing lake, to flood-dom i nated flu vial plain, swamp and al lu vial fan de pos its, as well as a pyroclastic event. The palaeorelief was low dur ing de po si tion and the Orava-Nowy Targ Ba sin could have spread sig nif i cantly more to the south.

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ABSTRACT:Konon, A., Ostrowski, S., Rybak-Ostrowska, B., Ludwiniak, M., Śmigielski, M., Wyglądała, M., Uroda, J., Kowalczyk, S., Mieszkowski, R. and Kłopotowska, A. 2016. Mnin restraining stepover -evidence of significant Cretaceous-Cenozoic dextral strike-slip faulting along the Teisseyre-Tornquist Zone? Acta Geologica Polonica, 66 (3), 429-449. Warszawa.A newly recognized Mnin restraining stepover is identified in the Permo-Mesozoic cover of the western part of the Late Palaeozoic Holy Cross Mountains Fold Belt (Poland), within a fault pattern consisting of dextral strikeslip faults. The formation of a large contractional structure at the Late Cretaceous -Cenozoic transition displays the significant role of strike-slip faulting along the western border of the Teisseyre-Tornquist Zone, in the foreland of the Polish part of the Carpathian Orogen. Theoretical relationships between the maximum fault offsets/mean step length, as well as between the maximum fault offsets/mean step width allowed the estimation of the values of possible offsets along the Snochowice and Mieczyn faults forming the Mnin stepover. The estimated values suggest displacements of as much as several tens of kilometres. The observed offset along the Tokarnia Fault and theoretical calculations suggest that the strike-slip faults west of the Late Palaeozoic Holy Cross Mountains Fold Belt belong to a large strike-slip fault system.We postulate that the observed significant refraction of the faults forming the anastomosing fault pattern is related also to the interaction of the NW-SE-striking faults formed along the western border of the TeisseyreTornquist Zone and the reactivated WNW-ESE-striking faults belonging to the fault systems of the northern margin of the Tethys Ocean.

A geological structural study has been conducted along the tectonic contact zone of the Central Carpathian Paleogene Basin (CCPB) and Pieniny Klippen Belt (PKB) in the eastern Podhale and western Spišska Magura areas. It concerned mostly the Central Carpathian Paleogene flysch strata and, to a lesser degree, the Upper Cretaceous rocks of the PKB. Tectonic deformation structures genetically related to the important tectonic boundary in question occur within a c. 1.5-2 km-wide strip of the Paleogene flysch rocks adjacent from the south to the PKB. Two parallel structural domains have been distinguished within this strip: the contact zone proper in the north and the peri-Pieniny monocline in the south. Most of the minor faults documented in the Paleogene flysch bear a record of dextral motion parallel to the contact zone. Some dextral-reverse oblique slip faults of NE-SW and WE trends have also been recognized. Discrepancies in the orientation and sense of movement on strike-slip faults in the Paleogene flysch rocks and those in marlstones of the "klippen envelope" of the PKB were encountered. They probably reflect differences in the structural history of both the adjacent rock complexes, as the Upper Cretaceous deposits of the PKB must have experienced more deformation events and, in general, were affected by much more intense strain than those of the CCPB. Contractional structures, such as south-vergent reverse faults and recumbent folds which point to ca N-S tectonic shortening, have also been found in the Paleogene rocks. The entirety of the structural features found in the CCPB is characteristic of a transpressional regime. The regionally consistent coexistence of structures resulting from strike-slip movements and tectonic shortening, as well as features pointing directly to a transpressional regime, prove the transpressional dextral nature of the contact between the CCPB and PKB.