Wyniki wyszukiwania - Biblioteka Nauki

1

The distinctive shapes of some kame ridges in the Łódź region of Central Poland

100%

Klajnert Z.

|

tom Vol. 3

63--75

EN

In the central part of the Rawka lobe of the Warta stage ice sheet of the Middle Polish glaciation (Saalian), areal déglaciation took place in the vicinity of Łódź. This is indicated by the numerous kames here, among which ridge forms are conspicuous. Some of the ridges which are situated on the slopes of river valleys and on the slopes terrain depression possess unusual shapes which resemble „tongues" and „paws". These forms merge gently with the adjacent elevated upland, whereas their distal parts are sharply defined and may lie as much as several decametres above their bases. „Kame tongues" and „karne paws" are built from paraglaciolacustrine and glaciofluvial deposits which accumulated in water bodies between dead ice blocks during the final phases of the ice sheet downwasting. The distinctive shapes of the landforms result from the varying thickness of the dead ice masses: thinner on the elevations and significantly thicker in terrain depressions (mainly in large, subglacial pre-Wartian valleys). These characteristic kame ridges demonstrate that the more elevated parts of the subglacial surface had been ice free for a long time before the dead ice blocks eventually disappeared from the terrain depressions.

2

Deglaciation chronology of the Pandivere and Palivere ice-marginal zones in Estonia

88%

Saarse L. , Heinsalu A. , Veski S.

|

2012

|

tom Vol. 56, No 2

353-362

EN

Accelerator mass spectrometry (AMS) 14

3

Glacial and periglacial relief on the southern slopes of the Western Tatra Mts. (Slovakia) - the results of the first detailed geomorphological mapping of the Žiarska, Jamnicka, Račkova and Bystra Valleys

88%

Kłapyta P.

|

2009

|

tom Vol. 10

50-57

EN

The article presents the results of the first detailed geomorphological mapping of the Žiarska, Jamnicka, Raekova, and Bystra Valleys, situated on the southern slope of the Western Tatra Mountains. The field work was supplemented by digital topographic as well as statistical analysis of rock glaciers distribution. The author focused on the distribution and morphological features of moraines and rock glaciers. Variability of both sets of deposits strongly reflects topographic influences on debris and snow accumulation. The main factor controlling the geometry of landforms was solar irradiance modified by the influence of the local cirque topography. Two generations of the rock glaciers indicate distinct phases of periglacial conditions during the Late Glacial period.

4

Chronology of the last ice sheet decay on the southern Baltic area based on dating of glaciofluvial and ice-dammed lake deposits

88%

Uścinowicz S. , Adamiec G. , Bluszcz A. , Jegliński W. , Jurys L. , Miotk-Szpiganowicz G. , Moska P. , Pączek U. , Piotrowska N. , Poręba G. , Przezdziecki P. , Uścinowicz G.

Geological Quarterly

|

2019

|

tom Vol. 63, No. 1

193--208

EN

The paper presents the results of the first OSL dating of glaciofluvial and ice-marginal lake sediments which occur between end moraines of the Słupsk Bank and the Polish coast. The sand and gravel of glaciofluvial deltas on the Słupsk Bank were deposited most likely during a period from 14.3 ±1.2 to 16.6 ±1.4 ka ago. The deposition of silty-sandy sediments of the ice-marginal lake is dated at 14.51 ±0.81 and 14.6 ±1.4 ka years. Likewise, dates ranging from 13.74 ±0.84 to 16.70 ±1.1 ka obtained from low sandy ridges, related to the southern range of the ice-marginal lake in the Gardno-Łeba Lowland, indicate the most likely timing of their deposition. It can be concluded that a short stop of the ice sheet on the Słupsk Bank took place approximately 15.2 ka ago, which could be correlated with the position of the ice sheet front in central Skåne and in northern Lithuania at that time. Older and younger results were also obtained, except the dates mentioned above. The older ages show little sunlight exposure of sediments during their deposition. The younger dates indicate a marine origin of the sediments and show that some parts of glaciofluvial sediments were redeposited and exposed to sunlight at a later stage, most probably when dead-ice blocks were melting.

5

Holocene Chronology of the Brattforsheden Delta and Inland Dune Field, SW Sweden

75%

Alexanderson H. , Fabel D.

|

tom Vol. 42, no.1

1--16

EN

Brattforsheden is a large glacifluvial deposit in southwestern Sweden and associated with it is one of Sweden’s largest inland dune fields. Although the relative ages of the Brattforsheden deposits are well known, absolute ages from the area are few. In this study we have used optically stimulated luminescence (OSL), surface exposure (10Be) and radiocarbon (14C) dating to provide an absolute chronology for the deglaciation and for the Holocene development of the aeolian dunes. Our data show that the deglaciation took place just before 11 ka (11.5 ± 0.6 ka OSL, 11.3 ± 0.8 ka 10Be), in line with the 14C-based regional deglaciation age. Aeolian dunes started forming immediately after deglaciation and were active for at least 2000 years, well after vegetation had established. Renewed aeolian activity occurred 270–180 years ago, resulting in the deposition of sand sheets. Comparison between dating methods and studies of OSL dose distributions show that glacial, glacifluvial and littoral sediments suffer from incomplete bleaching and thus that mean OSL ages from such deposits overestimate the true depositional age. By using small aliquots and statistical age models, this effect can partly be countered. Also, some of the 10Be ages appear too old, which may be due to previous exposure.

6

Maksymalny zasięg lądolodu stadiału Warty w lobie Prosny

75%

Haisig J. , Wilanowski S.

Biuletyn Państwowego Instytutu Geologicznego

|

1998

|

tom nr 385

105-111

PL

Badania prowadzone w rejonie lobu Prosny wykazały dalszy ku południowi (miejscami do 10 km) zasięg strefy marginalnej maksymalnego zasięgu stadiału Warty, wyznaczony głównie na podstawie przebiegu wzgórz moren czołowych oraz występowania poziomu glin lodowcowych. Gliny lodowcowe występujące w lobie Prosny mają cechy litologiczne podobne do glin lodowcowych z tego samego wieku, obserwowanych w dorzeczu Widawki oraz na Wale Śląskim. Na północ od strefy maksymalnego zasięgu lądolodu stadiału Warty zaznaczają się dwie strefy moren recesyjnych.

EN

Current investigations have documented that the maximum extent of the Wartanian ice sheet in the Prosna lobe lies more southwards than hitherto assumed. It occurs in places about 10 km to the south, especially in the central part of the lobe. The ice sheet extent is usually marked by distinct end moraines, but in places only by the till. The Wartanian till in the region investigated has similar mineralogical and petrological features as Wartanian tills in surrounding regions. Northwards the maximum ice sheet extent, there are other end moraine hills, which represent recessional phases, as well as several kames and one esker. South of the terminal moraines, the ice marginal valleys filled with glaciofluvial sands occur extensively.

7

Symptoms of the permafrost presence in Middle Poland during the last 150 000 years

75%

Klatkowa H.

Biuletyn Peryglacjalny

|

1996

|

tom 35

8

Ice dynamics during the deglaciation of SW Skane, South Sweden

75%

Lagerlund E.

|

tom 04

9

Glacial Terminations II and I as recorded in NE Iceland

63%

Vliet-Lanoë B. , Guðmundsson A. , Guillou H. , Guégan S. , Loon A. J. T. , Vleeschouwer F.

Geologos

|

2010

|

tom Vol. 16, No. 4

201--222

EN

Volcanism in eastern Iceland has controlled the changes in glacier- and river-drainage patterns and the sedimentary budget, particularly during the Middle and Late Pleistocene. The glacial extent in NE Iceland appears to be related to the impact of volcanic activity, not only on the ice-stream dynamics, but also on the sedimentary successions. Analysis of the Jökuldalur and Jökulsa á Brù records results in a new interpretation of the changes in ice extent and flow direction for at least the last two glaciations. From MIS 8 onward, the development of the Snæfell volcano apparently forced the ice stream that derived from the Vatnajökull ice cap to take another course; it also affected the offshore sedimentary budgets at the new outlet at Vopnafjördur. The MIS 6 ice sheet was thick and extensive, and associated with an ice-stream diversion to the North. The thick sedimentary complex of palaeolake Halslón was formed close to an outlet of the Vatnajökull, the Brùarjökull, during Termination II and a part of the MIS 5e interglacial. The deposits formed during MIS 5e record two climate optima interrupted by two successive glacial advances correlated with the mid-Eemian cooling. The deposits of the Weichselian deglaciation (Termination I) are much more limited in thickness. During the Last Glacial Maximum and the Late Glacial, glaciers also seem to have been restricted in the Jökulsa á Brù area. Valley glaciers issued from the Brùarjökull re-advanced several times in the Jökuldalur only during at least the Older Dryas, the Younger Dryas and the Preboreal. NE Iceland has undergone considerable deglaciation since the Bølling. In contrast to the conclusions of previous studies, the results presented here are consistent with data on the glaciations in other Nordic regions and can increase the understanding of the mid-Eemian cooling.

10

Zapis glacilimnicznej sedymentacji w basenie Niecki Skaliskiej - północna część Pojezierza Mazurskiego

63%

Pochocka-Szwarc K.

Przegląd Geologiczny

|

2010

|

tom Vol. 58, nr 10

1014-1022

EN

The investigation area is situated in the north part of Mazurian Lakeland in NE from Węgorzewo in the borderland between Poland and Russia. It was covered with the ice sheet during the upper stage of the Vistulian Glaciation. During the recession of the maximum range of the ice-sheet (Pomeranian Phases) the 6 ice-sheet retreated were left. Skaliska Basin this is end depression, between two end moraine zones. The glaciolacustrine and lacustrine sediments was recorded late glacial and postglacial history. The results of the multidisciplinary investigations including cartographical, sedymentological methods indicate that in the ice-dammed lake in Skaliska Basin was existed in front of the ice. The outflow from Skaliska ice-dammed was connected with the ice sheet retreat (behind the Pregoła Valley) and development of the new erosion base level (like Pregoła Valley).

11

Scandinavian eskers, global climatic relationships, and solar forcing

63%

Lundqvist J.

|

tom Vol. 43, Nr 2

149-152

EN

The morphology of a number of eskers in Sweden formed during the down-wasting of the last Scandinavian ice sheet about 11,000 to 10,000 calendar years ago shows a subdivision into centres representing periods of 1, 3-6 and 10-11 years. It is proposed that these periods correspond to the summer/winter seasons, the El Nińo - Southern Ocean (ENSO) cycle, and the sunspot cycle, respectively. If this is correct, the implication is a more global climatic relationship than earlier realised.

PL

W morfologii wielu ozów szwedzkich, powstałych podczas zaniku ostatniego lądolodu skandynawskiego 11-10 tysięcy lat temu, zaczynają się kulminacje reprezentujące okresy jednoroczne oraz 3-6 i 10-11 letnie. Przypuszczalnie okresy te są spowodowane odpowiednio przez sezonowość letnio-zimową, cykliczność zjawiska El Nińio oraz zmieniającą się intensywność plam słonecznych. Jeśli takie powiązania okazałyby się prawdziwe, to mielibyśmy znacznie więcej globalnych zależności klimatycznych niż przypuszczano dotychczas.

12

Southern Baltic area during the last deglaciation

63%

Uścinowicz S.

|

tom Vol. 43, Nr 2

137-148

EN

In the Polish economical zone of the Baltic Sea there are boulder fields (residuum of end moraines), remnants of end moraines, glaciofluvial deltas, eskers, and ice-dam lake deposits formed during a decay of the last Scandinavian ice sheet. Landforms and deposits of three ice marginal zones were distinguished in the Southern Baltic. The Gardno Phase probably corresponds to the Halland-West Skane Phase, dated at ca. 14 ka BP, and to the Middle Lithuanian Phase. The Słupsk Bank Phase is marked at a bottom of the Baltic Sea by boulder fields on the Słupsk Bank and by remnants of end moraines in the southern Bornholm Basin and the western Gdańsk Basin. It is to be correlated with the ice limit in Skane, dated at 13.5 ka BP, and with the North Lithuanian Phase at ca. 13.2 ka BP. The Southern Middle Bank Phase, marked by glaciofluvial deltas on this bank and by end moraines in the central Bornholm Basin, most probably corresponds to the ice margin in Skane, dated at 13.0-12.9 ka BP, and to the Otepää Phase in the east.

PL

W czasie prac kartograficznych prowadzonych w latach 1977-1990 przez Oddział Geologii Morza Państwowego Instytutu Geologicznego w obszarze polskiej strefy ekonomicznej Morza Bałtyckiego rozpoznano szereg form i osadów związanych z zanikiem ostatniego lądolodu skandynawskiego. Opisano i przedstawiono na mapie rozmieszczenie głazów i głazowisk stanowiących rezyduum osadów morenowych, ostańców ciągów moren czołowych częściowo pogrzebanych pod młodszymi osadami, delt glacitluwialnych, ozów i osadów zastoiskowych. Na dnie południowego Bałtyku wyróżniono formy i osady trzech stref maginalnych: fazy Gardna, Ławicy Słupskiej i Południowej Ławicy Środkowej. Podjęto próbę korelacji przestrzennej i czasowej form zachowanych na dnie Bałtyku z cięgami marginalnymi występującymi po obu stronach Bałtyku. Faza Gardna, której wiek w strefie polskiego wybrzeża wyznaczają daty radiowęglowe torfów z Niziny Gardzieńsko-Łebskiej (K. Rotnicki, K. Borówka, 1995a, b) i Zatoki Pomorskiej (R. Kramarska, Z. Jurowska, 1991; R. Kramarska,1998), odpowiada najprawdopodobniej fazie Halland-West Skane, wyróżnionej i datowanej na ok. 14 ka BP przez E. Lagerlunda i M. Houmark-Nielsena (1993), jak również fazie środkowolitewskiej na wschodzie (A. Raukas i in., 1995; R. Pirrus, A. Raukas, 1996). Faza Ławicy Słupskiej, zaznaczająca się na dnie Bałtyku głazowiskami na Ławicy Słupskiej oraz ostańcami cięgów moren czołowych w południowej części Basenu Bornholmskiego i w zachodniej części Basenu Gdańskiego, może być korelowana z linią postoju krawędzi lądolodu w Skanii, datowaną na 13,5 ka BP (J. Lundqvist, 1994) i fazą północnolitewskŕ (Ługa), której wiek określa się na ok.13,2 ka BP (A. Raukas i in.,1995; R. Pirrus, A. Raukas, 1996). Faza Południowej Ławicy Środkowej, zaznaczona głównie przez delty glacifluwialne występujące na tej ławicy i moreny czołowe w środkowej części Basenu Bornholmskiego, odpowiada najprawdopodobniej strefie marginalnej w Skanii datowanej na 13.0-12.9 ka BP (J. Lundqvist, 1994), a na wschodzie fazie Otepaa (A. Raukas i in.,1995), nazywanej też fazą północnołotewską (V. K. Gudelis, E. Emelyanov, 1976). Recesja lądolodu z obszaru Południowej Ławicy Środkowej kończy deglacjację obszaru południowego Bałtyku. Około 12,7-12,6 ka BP na skutek wytapiania się martwych lodów w Rynnie Słupskiej przy podnoszeniu się poziomu wody, następuje połączenie zastoisk Basenów Gdańskiego i Bornholmskiego dając początek bałtyckiemu jezioru lodowemu-pierwszej fazie rozwojowej Morza Bałtyckiego.

13

Cechy rozwoju i zaniku lądolodu warciańskiego w środkowej Polsce

63%

Krzemiński T. , Uniwersytet Łódzki I. G. F. i. K. Ś.

Acta Universitatis Lodziensis. Folia Geographica Physica

|

1997

|

tom 1

EN

The South Great Poland ice-sheet lobe representing the Warta Glaciation stretched from the Warsaw-Berlin pradolina that runs along the S2nd parallel (100 m above sea level) to the Wieluń Upland (272 m above sea level) in south (SI°N). The lobe was halted by topographic barriers of the Ostrzeszów Hills (284 m) and of the Łódź Upland (284 m) and left some signs of push moraines there. In central Poland the Wartanian ice-sheet spread southwards utilising the river valleys of the Prosna, Warta and Widawka (Fig. 1). The ice conserved the valleys, which is evidenced by 2-4 m thick till well preserved on the slopes of buried valleys older than of Wartanian age (Fig. 2). The southern portion (51O5O'N) of the South Great Poland lobe diverged into lower order lobes of Widawka, Warta and Prosna. The Widawka lobe, developed in the east, flew over the elevation of the Bełchatów Upland (200-220 m) and left signs of diffluence in the Piotrków Plain (Fig. 3). The Warta lobe crept up onto the northern edge of the Wieluń Upland (200-250 m) where the ice-sheet dissipated. The Prosna lobe reached the Wieruszów Upthrust at a similar altitude. Climatically induced process of the ice-sheet degradation began with the development of crevasses and cracks in the places of irregularities in the topography of the sub-Quaternary bedrock. This led to the formation of marginal zone delineated by the maximum extend of the ice-sheet and by its extent during the main stagnation phase, when the contact with the active ice mass was retained. Inside this zone the landforms associated with stagnant ice downwasting are found. These include kames, karne terraces, karne plateaux, kettles, post-glacial depressions, small outwash plains, latent fragments of pradolinas. Topographic watersheds separate former inward and outward meltwater flow directions. Four subsequent phases of the ice-sheet degradation and the corresponding zones: I - Dzialoszyn, II - Sieradz, III - Niemysłów and Kalisz zones comprise a similar range of landforms and the pattern of flow directions inherited from the areał deglaciation (Fig. 3 and 4). The formation of the zones can be related to the elevations of the sub-Wartanian base, mainly of Mesozoic and Neogene age. Groups of kames (Fig. 1 and 5) are also the evidence of the areal deglaciation. On elevations of the substratum elongated crevasses developed in the downwasting ice. They were then filled with gravel and sand - mainly of inglacial or supraglacial origin. The areas situated between subsequent deglaciation zones and the groups of karnes are usually build of till that forms low relief of undulating ground moraine.

PL

Proces rozprzestrzeniania lądolodu warciańskiego w środkowej Polsce postępował ku południowi dolinami Prosny, Warty i Widawki. Udokumentowane jest to gliną zwałową, dobrze zachowaną na stokach dolin kopalnych starszych od zlodowacenia warciańskiego. W części południowej lobu południowowielkopolskiego (5I,30aN) wyodrębniły się loby niższego rzędu Prosny, Warty i Widawki. Klimatycznie uwarunkowany proces zanikania lądolodu rozpoczyna się przetainami i spękaniami na elewacjach podłoża podwarciańskiego. Prowadzi to do powstania stref brzeżnych ograniczonych każdorazowo linią maksymalnego zasięgu lądolodu i linią głównego etapu postojowego, zachowującego więź z żywym lądolodem. Kolejne etapy zanikania lądolodu warciańskiego w strefach: I działoszyńskiej, II sieradzkiej, III niemysłowskiej i kaliskiej mają podobny inwentarz form rzeźby i układ odpływu wód odziedziczony z deglacjacji arealnej (rys. l, 3 i 4). Obszary leżące pomiędzy kolejnymi strefami brzeżnymi zbudowane są przeważnie z glin zwałowych moreny dennej, która miejscami powleczona jest utworami pokrywowymi.

14

Contemporary glaciation of the Petuniabukta area against the background of Late-Vistulian and Holocene deglaciation [Western Olav V Land, Spitsbergen]

63%

Karczewski A.

|

tom 04

15

Post-'Little Ice Age' retreat rates of glaciers around Billefjorden in Central Spitsbergen, Svalbard

63%

Rachlewicz G. , Szczucinski W. , Ewertowski M.

|

2007

|

tom 28

|

nr 3

EN

Twelve glaciers, representing various types, were investigated between 2000 and 2005, in a region adjacent to the northern reaches of Billefjorden, central Spitsbergen (Svalbard). On the basis of measurements taken using reference points, DGPS and GPS systems, analyses of aerial photographs and satellite images, geomorphological indicators and archival data their rates of deglaciation following the "Little Ice Age" (LIA) maximum were calculated variously on centennial, decadal and annual time scales. As most Svalbard glaciers have debris-covered snouts, a clean ice margin was measured in the absence of debris-free ice front. The retreat rates for both types of ice fronts were very similar. All studied glaciers have been retreating since the termination of the Little Ice Age at the end of 19th century. The fastest retreat rate was observed in the case of the Nordenskioldbreen tidewater glacier (mean average linear retreat rate 35 m a-1). For land-terminating glaciers the rates were in range of 5 to 15 m a-1. Presumably owing to climate warming, most of the glacier retreat rates have increased several fold in recent decades. The secondary factors influencing the retreat rates have been identified as: water depth at the grounding line in the case of tidewater glaciers, surging history, altitude, shape and aspect of glacier margin, and bedrock relief. The retreat rates are similar to glaciers from other parts of Spitsbergen. Analyses of available data on glacier retreat rates in Svalbard have allowed us to distinguish four major types: very dynamic, surging tidewater glaciers with post-LIA retreat rates of between 100 and 220 ma-1, other tidewater glaciers receding of a rate of 15 to 70 m a-1, land terminating valley polythermal glaciers with an average retreat of 10 to 20 m a-1 and small, usually cold, glaciers with the retreat rates below 10 m a-1.

16

An outline of the evolution of the Southern Baltic area at the end of the last glaciation and beginning of the Holocene

63%

Mojski J. E.

|

1995

|

tom 34

17

The periglacial impact on the deglaciated area of Northern Poland after 20 KYR BP

63%

Kozarski S.

|

1995

|

tom 34

18

The evolution of a marginal form and of kames in the region of Bielsk Podlaski. Sedimentological analysis of deposit

63%

Mycielska-Dowgiallo E. , Pekalska A. , Woronko B.

|

tom 04

19

Deglaciation of the Northern foot-hills in the East Kunlun Mts.

63%

Drozdowski E.

|

tom 60

20

Zagadka zaniku jeziora skaliskiego w Krainie Wielkich Jezior Mazurskich

51%

Pochocka-Szwarc K.

Przegląd Geologiczny

|

2005

|

tom Vol. 53, nr 10/1

873-878

EN

In the northern part of the Great Mazurian Lakes there is a post-lacustrine plain extending over 90 km 2 . This depression, called Skaliska Basin (Kondracki, 1998), is situated NE of Węgorzewo, overlapping the state boundary between Poland and Russian Kaliningrd Region (thus the northernmost part of the structure was not accessible for study). A glaciolacustrine lake existed there during Late Pleistocene (Pochocka-Szwarc & Lisicki 2001a, 2003). Defining the exact extent and direction of outflow from the Skaliska Lake are most important aims for palaeogeographic investigation of the area. For paleogeomorphological analyses of the Skaliska Basin, the following methods were used: Digital Terrain Model (1 : 200,000 scale), Landsat TM satellite images, archival cartographic materials, and results of geological investigations accompanying compilation of sheets Budry (Pochocka-Szwarc, Lisicki 2001a) and Banie Mazurskie (Pochocka-Szwarc 2003) of the Detailed Geological Map of Poland (1 : 50,000). The study allowed to recognize the lateral extension of the paleolake, and reconstruct the sequence of events that led to catastrophic out flow towards the NW.