| Summary: | Pleistocene of the North-western margin of the Holy Cross Mts No pre-Pleistocene deposits or sediments corresponding to Podlasie Glaciation (Günz) or Przasnysz Interglacial (Cromer) were found in the area of north-western margin of the Holy Cross Mts. During the Cracovian Glaciation (Mindel) this whole region was covered with ice-sheet. Deposits of this Glaciation are preserved only in relics (fig. 1) and represented by separated ratches of boulder clay and fluvioglacial deposits, (I. Jurkiewiczowa and K. Mamakowa, 1960, C. Radłowska, 1963, H. Ruszczyńska-Szenajch, 1966). These deposits correspond to the lower glacial series of the Cracovian Glaciation. Preservation of deposits of the Cracovian Glaciation only in scarce remains indicates considerable erosion and denudation processes during the preoptimal part of the Great Interglaciai (Holstein) (S. Z. Różycki 1964a, L. Lindner 1970a, b). The depth of river valleys in that times was from 20 to 50 m. and their bottoms occur 25—85 m below the present surface. During the postoptimal period of Interglaaial (S. Z. Różycki 1964 a, K. Grzybowski 1966) these valleys have been filled with alluvial deposits (Fig. 1). The Middle Polish Glaciation (Riss) in the area under examination is represented by three distinct glacial series and by fluvioglacial deposits connected with subsequent transgressions and recession's of the ice-sheet of the Radomka glacistadial (Drenthe). Because of their climate-stratigraphic significance (S. Z. Różycki 1964 b), the series of glacial accumulation correspond to the three glaciphase oscillations of the ice-sheet front (Fig. 1). During the maximal extension of this glaciation the base of ice front was reaching in the Przysucha region 300—330 m. a.s.l. and in the Końskie region 275—285 m a.s.l. Retreat of the ice-sheet of the maximal glaciphase proceeded simultaneously in these both regions. Four glacioscilations were traced, separated by melting periods during interglacistages (L. Lindner , 1970 a, b, c). Considerable lowering of the local erosion base level during the Pilica Interglacistage (Ohe) resulted in the formation of erosion-and-aocumulation surface (terrace III) ¡n the Czama river-basin. The Eemian interglacial period was marked by further intensification of erosion processes and organogenic accumulation (E. Passendorfer, 1931, A. Środoń and M. Gołąbowa , 1956) and by the development of soil-forming processes (L. Lindner , 1970a). Three horizons of younger loesses were accumulated during the older (steppe-tundra) part of Würm whereas in it younger part congeliffluction, formation of the terrace II and dune-forming processes took place.
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