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„Middle Polish fluvial high terrace” in the river valleys of the Kielce - Łagów Depression (Holy Cross Mountains, Poland) – fact or myth?

Ludwikowska-Kędzia Małgorzata

Studia Geomorphologica Carpatho-Balcanica

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2021

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Vol. 55

129--152

EN

The article is a commentary on the current state of knowledge of the formation conditions, origin and stratigraphic position of the „Middle Polish fluvial, fluvioperiglacial high terraces” being relief elements of the river valleys of the Kielce– Łagów Depression (KŁD) in the southern part of the Holy Cross Mountains (HCM), i.e. the Belnianka, Lubrzanka and Łagowica river valleys. The former conception and criteria of distinguishing them are no longer fully valid. The “high terraces” were formed in the studied valleys in periglacial conditions of the Vistulian Glaciation and not, as it was previously considered, during the “Middle Polish Glaciation”. They are entirely or partially composed of slope deposits or formed within the cover of glacial and / or slope deposits (toe-cut terraces) of different ages (including derived from the Odra Glaciation). Their hypsometric position is determined by the features of structural relief and the possibility of deposition of slope sediments on the alluvial series. The formation and structure of these terraces are the outcome of the location and pattern of river valleys in relation to the morphostructural elements of the KŁD as well as the changes of climate and environmental conditions in the Quaternary. The presented results were obtained owing to the fact that the investigations were conducted both in the profiles of hillslopes (slope environment) and river valleys (fluvial environment) as well as in the bottom of the KŁD (glacial environment). Only such an integrated approach gives an opportunity to find the relationship between the elements of the local litho- and morphogenetic system of the HCM: hillslopes ↔ river valleys ↔ bottoms of structural depressions.

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Terraces of the Bystrzyca river valley, Middle Sudetes, and their deformation along the Sudetic Marginal Fault

Krzyszkowski D., Biernat J.

Geologia Sudetica

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1998

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Vol. 31, nr 2

241-258

EN

There are three stages in the evolution of the Bystrzyca river valley, dated to the Pliocene, the Early to late Middle Pleistocene, and the late Middle Pleistocene to recent. The Pliocene landscape was flat to hilly, with a weakly developed margin of the mountains. The valleys were shallow and wide, most probably with sinuous rivers, and are today represented by the 100-120 m high terrace. The scarp of the Sudetic Marginal Fault and the mountain landscape with deeply incised valleys were not formed until the Early Pleistocene tectonic phase, during which the uplift was about 60-70 m. The late Middle to Late Pleistocene stage of the valley development may be subdivided into several sub-stages, during each of which, one of three morphogenetic factors, namely fluvial activity, glacial erosion and sedimentation and tectonic uplift, prevailed. Five fluvial terraces have been found, one formed before glaciation and the other four during the post-glacial times. The valley was glaciated only once, during the early Saalian (Odranian) stage. The total postglacial uplift was about 40-50 m and fluvial activity that time was influenced by varying uplift rates. At first, erosion prevailed due to strong glacio-isostatic uplift. Then, it diminished quickly and was replaced by more localised tectonic uplift, which decreased with time. As a result, fluvial activity in the mountains and in the foreland became different, as is highlighted by the increased thickness of fluvial deposits in the foremoutain zone, the rapid change of terrace height, formation of a distinct, 25-30 m high, fault scarp along the Sudetic Marginal Fault, and the increased erodibility along the fault lines.

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Late Cainozoic evolution of the Nysa Kłodzka river system between Kłodzko and Kamieniec Ząbkowicki, Sudetes Mts, southwestern Poland

Krzyszkowski D., Przybylski B., Badura J.

Geologia Sudetica

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1998

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Vol. 31, nr 2

133-155

EN

The Nysa Kłodzka river drainge basin in the Sudetes Mts, SW Poland, preserves a complex late Cainozoic sequence that includes eight fluvial series/terraces and deposits from two glacial episodes as well as locally volcanic rocks, slope covers and loess. Sedimentation took place during the late Pliocene and since early Middle Pleistocene (Cromerian), with a long erosion phase (hiatus) during the Early Pleistocene. Fluvial series occur in the late Pliocene, Cromerian, Holsteinian, late Saalian/Eemian, Weichselian and the Holocene. Glacial deposits are represented in the early Elsterian and early Saalian stages. The main tectonic uplift and strong erosion was during the Early Pleistocene, with displacement about 60-70 m. Tectonic uplift was documented also for the post-Elsterian and the post-early Saalian time, and these uplift phases are most probably due to glacio-isostatic rebound. The Quaternary terrace sequence has been formed due to base level changes, epigenetic erosion after glaciations and neotectonic movements. The Cromerian fluvial deposits/terraces do not reveal any tectonic influence. However, all other Quaternary terraces indicate clear divergence, and the post-early Saalian terraces also offset by fault scarps. The total Late Pleistocene displacement along the fault scarps is about 25 m. The fluvial pattern is stable, once formed during the Pliocene, it continued in the same place until recently, with only minor changes along the uplifted block surrounding the Bardo gorge which infers the antecedent origin of the Bardo gorge. During the post-glacial times, epigenetic incisions have only slightly modified the valley.

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Geomorphic evolution of the mountain front of the Sudetes between Dobromierz and Paszowice and adjacent areas, with particular reference to the fluvial systems

Migoń P., Krzyszkowski D., Gogół K.

Geologia Sudetica

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1998

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Vol. 31, nr 2

289-305

EN

The morphology of the marginal part of the Sudetes between Dobromierz and Paszowice reflects above all lithological and structural differences within bedrock. Major landforms include watershed surfaces of low relief, monadnocks and intramontane basins. Drainage pattern changes were associated with the decay of the early Saalian (Odranian) ice-sheet, whilst stages of further development of fluvial systems are well documented by multiple terrace levels. The mountain front of the Sudetes, genetically related to the Sudetic Marginal Fault, is only up to 100 m high and overall strongly degraded. In contrast to southern sectors of the Sudetic mountain front, active Quaternary tectonics played minor part in the landscape development.