Wyniki wyszukiwania - BazTech

1

Erosion and accumulation phases during the last glacial-interglacial cycle : a case study of the terrace system of the Odra and Osobłoga rivers (southern Poland)

Wójcicki Krzysztof Jan, Pawelec Halina, Malik Ireneusz, Woskowicz-Ślęzak Beata, Moska Piotr

Geological Quarterly

|

2020

|

Vol. 64, No. 1

104--119

EN

In the Odra and Osobłoga River valleys in the vicinity of the town of Krapkowice, a system of morphological levels is present which is exceptionally extensive compared to other such systems in southern Poland. The extent, origins and chronology of these levels have been the subject of many controversies. In the light of current research, the terraces, which are situated on average 14.5-13, 12-10, 8-6, 6-4 and 3-1 metres above the river level, were formed in the post-Wartanian interval. The main factor driving their development was erosion, which compensated for the effects of large-scale aggradation that had occurred during the anaglacial phase of the Odranian Glaciation (MIS 8) dated to 261 ±15 ka. The impact of climatic conditions on the trends towards fluvial erosion or accumulation was only of secondary importance. According to OSL dating, successive phases of vertical stabilisation of the valley floor occurred ~118.8 ±8.3, 87.7 ±5.7 and 42.0 ±2.0 ka. In the meantime, erosion intensified, which resulted in the formation of lower terrace levels. During the climatic minimum of the Upper Plenivistulian (21.5 ±1.5 ka), under conditions of the delivery of sheet-wash-generated sediment, the aggradation of distal reaches of the Odra River valley was locally marked. During the Late Vistulian and Holocene, erosive tendencies continued, which were reflected by the fact that the surfaces of subsequent inset alluvial fills were situated ever lower. In the light of dating results, it can be concluded that during the colder periods correlated with the Rederstall Stadial (MIS 5b) and with the Hasselo Stadial (MIS 3), a braided river was present in the river valleys examined, which was most probably accompanied by permafrost. During the Eemian Interglacial (MIS 5e), during the Late Vistulian Interstadials and in the Holocene, it was a meandering river.

2

Terasy Wetliny w Bieszczadach (Karpaty Wschodnie) : próba porównania ich hipsometrii, budowy i wieku z doliną górnego Sanu

Kukulak J.

Landform Analysis

|

2015

|

Vol. 28

29--44

PL

W górskiej dolinie rzeki Wetlina (Bieszczady Wysokie) znajduje się schodowy system sześciu teras rzecznych (T1–T6). Wszystkie terasy mają wysokie cokoły skalne i żwirowe pokrywy akumulacyjne. Przetrwały w tej dolinie także residua żwirów staroglacjalnych. Dowiązanie wieku teras do reperu datowanych szczątków drewna i torfu na jednej z teras Wetliny (Ralska-Jasiewiczowa 1969, 1980) pozwala na wydzielenie w badanej dolinie 2–3 teras niskich (dennych) holoceńskich i 3 teras wysokich (zboczowych) plejstoceńskich. Z hipsometrycznej korelacji teras Wetliny z terasami pobliskiego Sanu wynika, że w dolinie Wetliny terasy są znacznie wyższe i mają bardziej zaburzone profile podłużne. Lokalne zmiany wysokości teras Wetliny i miąższości ich pokryw akumulacyjnych nie wykazują korelacji ze wskaźnikiem krętości koryta rzeki. Są one uwarunkowane względnie dużą podatnością skał strefy przeddukielskiej i ich silną fragmentaryzacją tektoniczną na erozyjne pogłębianie koryta rzeki.

EN

A stair-case system of six river terraces (T1–T6) with accumulation covers and bedrock toe occurs in the valley of the Wetlina River. Residual deposits of earlier glaciations are also present in this valley. Correlation of the age of the terraces with the dated organic material (wood and peat) on one of the terraces (Ralska-Jasiewiczowa 1969, 1980) allows delimitation of the levels of Pleistocene terraces: 2–3 within the valley floor (low terraces) and 3 within the slopes (high terraces). Hypsometric correlation of the terraces of the Wetlina and the nearby San River indicates that the terraces of the Wetlina are considerably higher and their longitudinal profiles are more distorted. Local variability in the elevation of the Wetlina terraces and in the thickness of their alluvial covers is not correlated with channel sinuosity and may have resulted from the complex tectonic structure and relatively low resistance of the bedrock of the Fore-Dukla Zone to the erosion of the river bed.

3

Chronostratigraphy of alluvia and age of fluvial landforms in the Carpathian Foreland during the Vistulian

Gębica P.

Studia Quaternaria

|

2013

|

Vol. 30, Nr 1

19--27

EN

A development of opinions on stratigraphy of alluvia and age of the Vistulian terraces in the valleys of the Carpathian foreland is presented, based mainly on publications of Professor Leszek Starkel. Studies of age of fluvial landforms and sediments of the Last Cold Stage in the Carpathian foreland have been started more than 100 years ago. Before them modern sedimentological methods and radiocarbon dating were introduced, pioneer studies of Pleistocene river terraces and sediments in the Carpathians were performed by Mieczysław Klimaszewski, and subsequently, by his student Leszek Starkel who mapped in 1950s a margin of the Carpathian Foothills as well as alluvial fans of Wisłoka, Wisłok and San rivers in the Carpathian foreland. In that time a stratigraphy of alluvial infillings in the marginal mountain zone was elaborated for the Late Vistulian and the Holocene. Starting from 1970s and basing on studies in key sites in the Wisłoka valley near Dębica, focused on palynological analyses and radiocarbon dating, general strati-graphical schemes of alluvial fills within the Vistulian terrace 15 m high and within the Holocene terrace 8-10 m high have been constructed. A comparison with the valleys in a periglacial area prowed that the Vistulian terrace 15 m high was incised before the maximum extension of the last Scandinavian ice sheet (i.e. before 20 ka BP) and the terrace 11-12 m high (with relics of braided river channels) was formed at the decline of the Plenivistulian. A final incision below the present river bed and aggradation occurred during the Late Vistulian (13-10 ka BP). The rivers changed their regime and their channel pattern from braided to large meanders-type as an effect of forest development and lower sediment load. The Younger Dryas cooling resulted in increased bedload and braiding.

4

Morfologia i budowa wewnętrzna terasy III (bifurkacyjnej) w Poznańskim Przełomie Warty

Antczak-Górka B.

Landform Analysis

|

2011

|

Vol. 16

194-196

EN

Results of a case study on the Warta River were presented which demonstrate climatically controlled valley floor evolution. The change in channel pattern meant also a change in valley floor development. Very flat and broad sandy-gravely bottoms formed by braided rivers were cut by better organised meandering rivers. The key profile at Żabinko shows sediments at the braided channel and organic deposits 14C dated. The dates point to bölling interstadial age. A clear differentiation in outflow direction has been fund in the vertical pattern of sedimentation from the western to northern sector. This analysis show that the bifurcation of waters ended at level of the bifurcation (III) terrace.

5

Palaeoslopes of Weichselian sand-bed braided rivers in the Toruń Basin (Poland): results of a palaeohydraulic analysis

Weckwerth Piotr

Geologos

|

2011

|

Vol. 17, No. 4

227--238

EN

Palaeoslopes of Weichselian sand-bed braided rivers have been reconstructed for two stages of fluvial development in the Toruń Basin. (1) The palaeoslope of the ‘fossil’ fluvial succession (buried under Weichselian tills) was calculated on the basis of the median grain size and the Shields parameter. The hydraulic gradient thus found is comparable with the hydraulic gradient of the present-day river. (2) The second developmental stage of the Toruń Basin (as a apart of the Noteć-Warta ice-marginal valley) took place after deglaciation. The slopes of river terraces are a few times lower than those calculated on the basis of the Shields parameter. The palaeoslope of the then river was estimated on the basis of a constant interdependency between the braidplain width, the channel geometry and the grain size. The river gradient that was thus calculated is similar to the measured terrace slope. Palaeoslope estimates in valleys similar to those in the Toruń Basin should consider the width of the braidplain.

6

Development of relief of the Velyky Lukavets River valley near Starunia palaeontological site (Carpathian region, Ukraine)

Sokołowski T.

Annales Societatis Geologorum Poloniae

|

2009

|

Vol. 79, No 3

243-254

EN

In Quaternary sediments filling the Velyky Lukavets River valley, at the abandoned ozokerite mine (= Ropyshche) in Starunia, perfectly preserved carcasses of large mammals were discovered in the first half of the 20th century. The study area includes a fragment of the valley between Molotkiv and Starunia, and its close vicinity. The area belongs to several morphostructural and geomorphic units of the Outer Eastern Carpathians and the Carpathian Foreland. The asymmetric, subsequent valley is a part of the Mizhbystrytska Upland, where flattened ridges and flat bulges represent fragments of planation surfaces: the upper (the Krasna level), elevated 170 m above the valley bottom and linked with the Late Pliocene, and the lower one (the Loyova level), rising at 100 m and linked with the Eopleistocene. Several flat surfaces are visible on valley slopes, probably representing river terraces formed before the Late Pleistocene. The valley attained its maximum depth during the Eemian Interglacial (OIS 5e). In the Ropyshche area, probably three terrace steps built of Weichselian and Holocene sediments (OIS 5d - 1) were developed, but their top surfaces are almost completely destroyed by mining operations. The recent, meandering river bed follows the zones of decreased cohesiveness of rocks resulting from mining activity and is becoming somewhat deepened during inundations. The transported material is mostly coarse-clastic one. The two latter factors may suggest that the river is underloaded due to declining agriculture and decreasing intensity of outwash. The top surface of the sub-Quaternary basement is deformed by subsidence and collapse of mine workings, but the relief of valley bottom allows for further exploration for remnants of large mammals not only in the Ropyscche area but along the whole studied segment of the valley, as well.

7

Późnoplejstoceński rozwój doliny Niemna w rejonie Grodna na Białorusi

Lindner L., Sańko A.

Przegląd Geologiczny

|

2008

|

Vol. 56, nr 1

73-80

EN

Based on geological and paleobotanic data, the oldest valley system of the Niemen River is linked in the study area with a river located southward of Grodno, within a parallel valley from the Alexandrian (Mazovian) Interglacial. The foundations of the present-day, almost meridian course of the Niemen River valley, are connected with a system of post-glacial lakes from the Sozhian (Wartanian) Stadial of the Pripethian (Odranian) Glaciation, later filled with organic deposits of the Muravian (Eemian) Interglacial. Analysis of six sites with these deposits (Pyszki, Rumlówka, Poniemuń, Żukiewicze, Bohatyrowicze and Kniażewodce) indicates that they represent three lakes located at different altitudes. During the maximal range of the Dvinian (Main) Stadial of the Poozerian (Vistulian) Glaciation, the lakes were beyond the range of the ice-sheet. At this time, the highest located deposits of the Poniemuń-Żukiewicze lake were covered by sander sediments, whereas the Bohatyrowicze-Kniażewodce and Pyszki-Rumlówka lakes that were located at lower levels, were covered by fluvio-periglacial deposits and varved clays of the Skidel ice-dammed lake. Retreat of the ice-sheet of the Dvinian Stadial, resulting in outflow of water from the Skidel ice-dammed lake through the area with the two lower interglacial lakes, triggered the formation of a system of the Niemen River supra-flood terraces above them. Accumulation of the highest of these terraces (VI), during the first phase of the Skidel lake outflow, marks the beginning of the present-day Niemen River valley formation that probably began in the younger phases of the Dvinian ice-sheet retreat. Further evolution of the valley is linked with the Late Glacial formation of the middle (III-V) supra-flood terraces and with the Holocene formation of the lower (II, I) supra-flood terraces.

8

Tarasy rzeczne Nysy Kłodzkiej oraz drobne plejstoceńskie struktury tektoniczne w strefie sudeckiego uskoku brzeżnego i przełomu bardzkiego w Janowcu

Badura J., Przybylski B., Tokarski A., Świerczewska A.

Przegląd Geologiczny

|

2007

|

Vol. 55, nr 3

228-228

EN

New research in the N part of the Bardo Gorge [close to the Sudetic Marginal Fault] evidenced the occurrence of two hitherto unknown Pleistocene river terraces. The terraces were interpreted basing on digital elevation model [DEM] 1;10,000 and radars sweeping of the Earth’s surfaces [DETM level 2]. Moreover, the results of petrographical analysis of deposits exposed in the 22 high river terrace show two-tier structure of the terrace. This suggest a polygenetic age of the terrace. Within the last terrace fractured clasts and small-scale faults were observed. Fractured clasts were studied in the bottom part of the 22-m-high river terrace where numerous fractured clasts occur. This part of the terrace is composed of gravels containing clasts up to 80 cm across. The matrix is sandy-clayey. The fractures are usually restricted to particular clasts. The fractures compose two sets striking NW-SE and N-S. Gravels exposed in the uppermost part of the terrace are cut by few strike-slip, N-S striking, sub-vertical faults which can be traced along a vertical distance up to 50 cm. These faults cut the gravel matrix but omit clasts. Fractures cutting the clasts do show a well organized architecture which is independent of orientation of a-b surfaces of the host clasts. These features indicate that the fractures were formed in situ within the studied gravels. Furthermore, for the majority of fractures, the angle between the fracture and the a-b surface of the host clast is less than 80, confirming the in situ origin of fractures. The fractures of one set are parallel to the strike of the Sudetic Marginal Fault. This suggests that the origin of the fractures is related to that of the fault. The fractures of the second set may represent Riedel shears associated with the activity of the Sudetic Marginal Fault. The orientations of minor faults confirm this supposition. Summing up, we believe that during the Pleistocene, the Sudetic Marginal Fault was a dextral strike-slip fault, at least in the discussed area.

9

Litostratygrafia plejstoceńskiego tarasu wysokiego doliny Łagowicy w rejonie Masłowca (SE część Gór Świętokrzyskich)

Ludwikowska-Kędzia M., Wiatrak M., Olszak I., Bluszcz A.

Przegląd Geologiczny

|

2006

|

Vol. 54, nr 11

953-962

EN

The lithostratigraphy of the Pleistocene high meadow terrace deposits in the Łagowica Valley near Masłowiec, southeastern part of the Holy Cross Mountains, central Poland, is presented against the background of geological features and relief of the valley in the Łagów–Ruda segment. The lithostratigraphic divisions for the Holy Cross Mountains assume Middle- Polish Glaciation age for high terraces in valleys. Hypsometry of terraces often served to estimate their age. Detailed sedimentological analysis of deposits forming the terrace of the Łagowica Valley near Masłowiec (textural and structural features, TL and OSL datings) have indicatived a complex fluvial-deluvial origin of the deposits and their Plenivistulian, not Middle Polish Glaciation age. The actual aggradation of the valley bottom has been partly masked by slope processes, which due to local lithostructural conditions, significantly participated in the Łagowica Valley bed aggradation. This problem is well-known in other upland regions of Poland and has been only briefly noted in the Holy Cross Mountains. The research methods and results can be useful in establishing the origins of deposits building meadow terraces, also then when only borecore material is available. The methods can also faciltate stratigraphic interpretation of deposits dated with TL and OSL methods

10

Sediments of the Pleistocene terraces of the Bug and Huczwa Rivers in the vicinity of Hrubieszów

Dolecki L.

Kwartalnik Geologiczny

|

1999

|

Vol. 43, Nr 1

27-38

EN

Geologic structure of the Pleistocene terraces of the Bug River within the Horodło Hills and the southern Dubienka Basin, and of the Bug and Huczwa Rivers in the Hrubieszów Basin, are described. There are three overbank terraces, two of them with a loess cover from the Upper Pleniglacial of the Vistulian Glaciation. The highest terrace was formed in the Wartanian Glaciation, the higher overbank terrace in the Lower Pleniglacial and the lower overbank terrace in the Upper Pleniglacial of the Vistulian Glaciation

PL

Teren badań stanowiły tarasy Bugu i Huczwy w obszarze przygranicznym Polski i Ukrainy, w bezpośrednim sąsiedztwie Grzędy Horodelskiej w okolicach Hrubieszowa. Rozpatrywano budowę tarasów nadzalewowych Bugu przed i za przełomem tej rzeki przez Grzędę Horodelską oraz tarasy nadzalewowe dolnego odcinka Huczwy w obrębie Kotliny Hrubieszowskiej. Podłoże czwartorzędu stanowią skały górnokredowe. Wyżej leżą zróżnicowane litologicznie i genetycznie osady eo- i mezoplejstoceńskie, tworzące w wielu miejscach powierzchnię bazalną tarasów neoplejstoceńskich. Najwyższy taras nadzalewowy (III) stwierdzony został pod przykryciem lessów z ostatniego zlodowacenia. Jest to taras ze zlodowacenia warty, o czym świadczą daty TL, a także wykształcony w stropie osadów tarasowych kompleks glebowy interglacjału eemskiego i wczesnej części zlodowacenia wisły. Łącznie z przykryciem młodszego lessu (4-12 m) taras ma wysokość względną rzędu 23 m. Taras nadzalewowy wyższy (IIb), erozyjno-akumulacyjny, zbudowany jest z osadów aluwialnych starszej części zlodowacenia wisły, z nadbudową w obrębie Grzędy Horodelskiej lessów młodszych górnego pleniglacjału tego zlodowacenia, natomiast utworów lessopodobnych i piasków poza Grzędą Horodelską. Wysokość względna tarasu nadzalewowego wyższego jest rzędu 7-12 m, w zależności od istnienia pokrywy lessu subaeralnego. Wysokość bezwzględna wynosi 190-197 m n.p.m. Powierzchnię bazalną tarasu stanowią głównie utwory plejstocenu, ale miejscami także kreda. Powszechnie utwory tarasu włożone są w różnogenetyczne osady zlodowacenia warty. Taras nadzalewowy niższy (IIa), erozyjno-akumulacyjny, powstał w wyniku erozji w interpleniglacjale podczas zlodowacenia wisły, a osady akumulowane w obrębie tarasu pochodzą głównie z górnego pleniglacjału tego zlodowacenia. Wysokość względna tarasu jest zróżnicowana w obrębie Grzędy Horodelskiej oraz jej sąsiedztwie, zwykle waha się w zakresie 5-6 m w stosunku do poziomu wody w rzece. Wysokości bezwzględne sę rzędu 180-l85 m n.p.m. Powierzchnię bazalną tarasu stanowią utwory aluwialne dolnego pleniglacjału zlodowacenia wisły lub starsze osady plejstoceński

11

Late Quaternary evolution of the Nysa Kłodzka river valley in the Sudetic Foreland, southwestern Poland

Przybylski B.

Geologia Sudetica

|

1998

|

Vol. 31, nr 2

197-211

EN

The late Quaternary Nysa Kłodzka river terrace system has developed since the retreat of the Early Saalian (Odranian) ice sheet, which entirely covered the Sudetic Foreland and partly the Sudetes Mts. There are four terraces in the river valley, where the oldest one, the Upper Terrace, developed during and immediately after the ice sheet retreat, other terraces were deposited during the subsequent cold and warm stages, Wartanian, Weichselian and the Holocene. At the initial stage, the present river valley formed at the margin of retreating ice sheet. Later, the valley developed due to several erosion and sedimentation phases. The Nysa Kłodzka river flows through a zone of moderate to distinct tectonic activity, which is confirmed by seismic activity and recent crustal movements in the eastern part of the Sudetic Foreland. The neotectonic movements influenced much the evolution of morphology of this zone throughout the Quaternary and led to the shaping of the valley into its current form. During the late Quaternary, neotectonics could have been strenghten due to post-glacial isostatic rebound. These vertical movements disturbed the terrace system of the Nysa Kłodzka river valley, with the strongest terrace tilt in the Upper Terrace level, but less deflections visible even in the Holocene terrace levels.