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1

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

Uścinowicz Szymon, Adamiec Grzegorz, Bluszcz Andrzej, Jegliński Wojciech, Jurys Leszek, Miotk-Szpiganowicz Grażyna, Moska Piotr, Pączek Urszula, Piotrowska Natalia, Poręba Grzegorz, Przezdziecki Piotr, Uścinowicz Grzegorz

Geological Quarterly

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2019

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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.

2

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

Alexanderson H., Fabel D.

Geochronometria

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2015

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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.

3

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

Saarse L., Heinsalu A., Veski S.

Geological Quarterly

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2012

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Vol. 56, No 2

353-362

EN

Accelerator mass spectrometry (AMS) 14

4

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

Pochocka-Szwarc K.

Przegląd Geologiczny

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2010

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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).

5

Glacial Terminations II and I as recorded in NE Iceland

Vliet-Lanoë Brigitte, Guðmundsson Agust, Guillou Hervé, Guégan Soléne, Loon A. J. (Tom), Vleeschouwer François

Geologos

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2010

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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.

6

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

Kłapyta P.

Landform Analysis

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2009

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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.

7

Zagadka zaniku jeziora skaliskiego w Krainie Wielkich Jezior Mazurskich

Pochocka-Szwarc K.

Przegląd Geologiczny

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2005

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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.

8

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

Klajnert Z.

Landform Analysis

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2002

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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.

9

Procesy deglacjacji na obszarze SSSI No. 8 i ich uwarunkowania klimatyczne oraz hydrologiczne (Zatoka Admiracji, Wyspa Króla Jerzego, Szetlandy Południowe)

Battke Z., Marsz A. A., Pudełko R.

Problemy Klimatologii Polarnej

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2001

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nr 11

121-135

EN

This work deals with the processes of deglaciation occurring in the region of SSSI No 8 (Site of Special Scientific Interests No 8) located on the western coast of the in the vicinity of Polish H. Arctowski Station over the period 1979-1999. The location of the SSSI is shown in Fig. 1. The basis of this work is comparison between the category of the surface of the area on the charts from 1979 (Furmańczyk & Marsz, 1980) and on the chart from 1986 (Battke, 1990) and the ground measurements carried out in that area in 1999 (Battke & Pudełko, unpubl.). The categories of area were computed on maps with the help of a planimeter: - glaciated areas, - non-glaciated areas (formed by mineral grounds), - sea areas. The accuracy of total measurements of the area is not lower than about 0.2 km2. The results of cartometric measurements are given in Table 1. Over the period 1979-1999 the area of SSSI decreased by 0.86 km2 as an effect of regression of icy cliffs both of Ecology and Baranowski Glaciers and due to accompanied abrasion process. At the same time the glaciated area within the borders of SSSI decreased by 6.93 km2 and the ice free area increased by 6.08 km2. In this way the mean rate of deglaciation of the 21-year period reaches about 0.33 km2 per year. Over the 21-year period the ice free area within the borders of SSSI incresed three times (from 2.98 km2 to 9.06 km2) which results in various consequences on the physico-geographical and biological prosesses in the region of the Admiralty Bay. In the period 1978-1986 the processes of deglaciation observed north of SSSI in the region of Ecology Glacier were faster than in other regions. Over the period 1986-1999 much faster decrease in the glaciated area was noted in the south of the area, in the region of Baranowski Glacier and Tower Glacier spatial changes are presented in Fig. 2. The analysis of reasons having influence on so advance processes of deglaciation indicated to two factors i.e. climatic and hydrological that are both responsible for the process. Over the period 1978-1998 in region of the Admiralty Bay the increase in air temperature during the Antarctic summer (period December - February; trend +0.022°C/year, statistically not significant) was noted. At the same time the period in which ablation was observed (warmer November and March) was longer. The annual sums of precipitation in the same period indicate to the presence of statistically significant negative trend (-5.7 mm/year, p < 0.005). This resulted in the change in the glacier mass balance at the level 2 m. above sea level: from -115 g/cm2/year in 1979 to -146 g/cm2/year in 1998 (Fig. 3). The evaluated trend of change in mass balance is -1.56 g/cm2/year and is not statistically significant. The period during which sea ice cover is not observed also lasts longer and the ice conditions there became visibly milder. This enables the thermal abrasion to last longer and causes more active regression of ice cliffs. On the shore of the Bransfield Strait, between the Admiralty Bay and the Maxwell Bay entrance a deep cove was formed in the ice coast over the period 1985-1988. This resulted in the increase in inclination of the southern slopes of ice forming the Warszawa Ice cap and forced the volume of ice flowing towards the Bransfield Strait to increase. In this way the volume of ice flowing down the Warszawa Ice Cap eastward, to SSSI No. 8 area, decreased. The explanation of reasons responsible for the ice conditions becoming milder can be found in large scale changes in sea surface temperature of the Southern Ocean of the sea area located West of the Antarctic Peninsula (a strong positive trend SST is marked in the period from October to January; in December +0.058°C/year) and in changes in atmospheric circulation. Both these factors, i.e. the increase in the negative values of the ice masses balance and the decrease in the volume of ice flowing down on the SSSI No. 8 area act in the same direction, causing that the deglaciation process in that region occurs in an exceptionally intensive way. Due to such great intensity of the deglaciation processes occurring on the surface of SSSI in that area, this area can be regarded as a unique object of ecological and environmental research.

10

Southern Baltic area during the last deglaciation

Uścinowicz S.

Kwartalnik Geologiczny

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1999

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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.

11

Scandinavian eskers, global climatic relationships, and solar forcing

Lundqvist J.

Kwartalnik Geologiczny

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1999

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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

Maksymalny zasięg lądolodu stadiału Warty w lobie Prosny

Haisig J., Wilanowski S.

Biuletyn Państwowego Instytutu Geologicznego

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1998

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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.