Unexpected ice flow directions during the Late Weichselian deglaciation of the south Baltic area indicated by a new lithostratigraphy in NW Poland and NE Germany

Lagerlund, Erik; Persson, Kärstin Malmberg; Krzyszkowski, Dariusz; Johansson, Per; Dobracka, E.; Dobracki, Ryszard; Panzig, Wolf-Albrecht

doi:10.1016/1040-6182(95)00028-h

Cited by 24 publications

(25 citation statements)

References 14 publications

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“…The Big Stony Ridge centre also was the source area for inland flow of glacial ice, towards the centre of the Trepassey sub-peninsula, and is the only Phase 3 centre surrounding St. Mary's Bay associated with flow away from the embayment. Lagerlund et al (1995) recognized a similar pattern of seaward glacial flow surrounding the western margins of the Baltic Sea, attributed to the accumulation of 'marginal domes' in the latter stages of glaciation. The absence of landward flow indicators associated with the Branch, Little Salmonier, Salmonier Nature Reserve, and Little Harbour River centres suggests that the ice in these areas was not sufficiently active or thick to form radially-flowing domes.…”

Section: Maintenance and Collapse Of The St Mary's Bay Ice Centrementioning

confidence: 94%

“…The absence of landward flow indicators associated with the Branch, Little Salmonier, Salmonier Nature Reserve, and Little Harbour River centres suggests that the ice in these areas was not sufficiently active or thick to form radially-flowing domes. The Big Stony Ridge ice, although it is associated with weak inland flow, is much smaller than the marginal domes of Lagerlund et al (1995). It was influenced primarily by drawdown effects, rather than acting as a truly independent, radially-flowing marginal ice dome.…”

Section: Maintenance and Collapse Of The St Mary's Bay Ice Centrementioning

confidence: 98%

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The pattern of glaciation on the Avalon Peninsula of Newfoundland

Catto¹

2002

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The pattern of glaciation on the Avalon Peninsula has been established through study of geomorphic features, striations, and erratic provenance. Three phases in a continuum of glaciation are recognized. The initial phase involved the expansion of ice from several centres. Ice thickness and extent reached a maximum during the subsequent Phase 2 event, correlated with the Late Wisconsinan. Lowered sea level permitted the development of the St. Mary's Bay ice centre. Ice from the Newfoundland mainland coalesced with Avalon Peninsula ice inPlacentia Bay, on the Isthmus, and in Trinity Bay. Rising sea level, triggered by the retreat of Laurentide ice in Labrador, resulted in destabilization of the St. Mary's Bay ice cap, marking Phase 3. Final deglaciation of theAvalon Peninsula began before 10,100 ± 250 BP. The Avalon Peninsula ice caps were controlled by regional and hemispheric events, and by the response of the Lauren- tide glaciers.L'histoire de la glaciation de la presqu'île d'Avalon a été établie à partir de l'étude des caractéristiques géomorphologiques, des stries et de la provenance des blocs erratiques. On distingue trois phases dans un continuum de glaciation. Pendant la première phase, il y a eu accumulation et dispersion de la glace à partir de plusieurs centres. Au cours de la deuxième période, qui correspond au Wisconsinien supérieur, les glaciers ont atteint un maximum en étendue et en épaisseur. Le niveau marin abaissé a permis la formation d'un centre glaciaire à l'emplacement de la baie St. Mary. Le glacier en provenance de la partie continentale de Terre-Neuve a fusionné avec celui de la presqu'île d'Avalon dans la baie de Plaisance, sur l'isthme et dans la baie de la Trinité. La troisième phase, caractérisée par la remontée du niveau marin et déclenchée par le recul de l'Inlandsis laurentidien au Labrador, a déséquilibré la calotte glaciaire de St. Mary. La déglaciation finale de la presqu'île d'Avalon a commencé avant 10 100 ± 250 BP. L'évolution des calottes glaciaires de la presqu'île d'Avalon a été déterminée par des événements régionaux et hémisphériques et par la réponse des glaciers laurentidiens.Das Schema der Vereisung auf der Avalon-Halbinsel wurde mittels des Studiums der geomorphologischen Merkmale, der Schrammen und der Herkunft der erratischen Blöcke nachgezeichnet. In der Anfangsphase dehnte sich das Eis ausgehend von mehreren Zentren aus. Das Eis erreichte ein Maximum an Dicke und Ausdehnung in der folgenden 2. Phase, die dem späten Wisconsin entspricht. Der niedrigere Meeresspiegel ermöglichte die Entwicklung des Eiszentrums der St. Mary's -Bai. Das Eis vom Festland Neufundlands vereinigte sich mit dem Eis der Avalon-Halbinsel in der Placentia-Bai, auf dem Isthmus und in der Trinity-Bai. In Phase 3 führte ein ansteigender Meeresspiegel, ausgelöst durch den Rückzug des laurentischen Eises in Labrador, zur Destabilisierung der Eiskappe der St. Mary's-Bai. Die endgültige Enteisung der Avalon-Halbinsel begann vor 10 100 ± 250 v.u.Z

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Section: Maintenance and Collapse Of The St Mary's Bay Ice Centrementioning

confidence: 94%

Section: Maintenance and Collapse Of The St Mary's Bay Ice Centrementioning

confidence: 98%

The pattern of glaciation on the Avalon Peninsula of Newfoundland

Catto¹

2002

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“…Each of the sites is downslope of a highland area. (cf., Lagerlund et al, 1995;Catto, 1998a). All late-glacial readvances in the Humber River basin remain undated.…”

Section: Glaciation Of Coastal Highlandsmentioning

confidence: 99%

Topographically-controlled Deglacial History of the Humber River Basin, Western Newfoundland

Batterson

Catto

2003

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AbstractThe Humber River in western Newfoundland flows through a large interior basin, that influenced Late Wisconsinan ice flow from major dispersal centres to the north, in the Long Range Mountains, and to the east in The Topsails. An early southward ice flow from a source to the north covered coastal areas in the western part of the basin. Subsequent regional ice flow was southwestward to northwestward from The Topsails, while south to southwestward flowing ice from the Long Range Mountains occupied the upper Humber River valley. This flow was confluent with ice from The Topsails and moved northwestward toward Bonne Bay. Regional deglaciation began about 13 ka from the inner coast. Ice occupying the Deer Lake valley dammed glacial Lake Howley in the adjacent Grand Lake and Sandy Lake basins to an elevation up to 85 m above present lake levels, which were controlled by drainage through a western outlet feeding into St. George’s Bay. The lake was lowered by exposure of the South Brook valley outlet, and finally drained catastrophically through a spillway at Junction Brook. Marine limit at the coast was 60 m asl. Inland deltas at the head of Deer Lake and fine-grained sediment exposed in the Deer Lake valley show inundation below 45 m present elevation. This produced a narrow embayment extending at least 50 km inland from the modern coast and is named here as ‘Jukes Arm’. Dated marine macrofossils in the Humber Arm and lower Humber River valley, indicate the deltas at the head of Deer Lake formed about 12.5 ka.

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“…The general knowledge about the Baltic Sea evolution is fairly profound but many problems still remain unresolved, particularly those related to the age and character of changes during the transition periods. The Baltic Ice Lake, the oldest stage of the Baltic Sea evolution began at 17 000 cal BP after deglaciation of the ice sheet (Björck 1995, Lagerlund et al 1995 and existed until the final drainage of the Baltic Ice Lake into the North Atlantic at 11 600 cal BP (Kortekaas et al 2007). The Baltic Ice Lake high stands at around 20 m b.s.l.…”

Section: Introductionmentioning

confidence: 99%

Stages of the Baltic Sea evolution in the geochemical record and radiocarbon dating of sediment cores from the Arkona Basin

Kostecki

2014

Oceanological and Hydrobiological Studies

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Four sediment cores from the southern part of the Arkona Basin were analyzed in terms of their geochemical composition, age and stratigraphy. The main stages of the Baltic Sea: the Baltic Ice Lake, the Ancylus Lake and the Littorina Sea were identified in all the analyzed cores. The data confirmed the high water fluctuation and significant environmental changes during the Baltic Sea evolution in the Late-Glacial and the Holocene. The signs of the second regression of the Baltic Ice Lake, dated at around 11 000 cal BP, were identified at a depth of 24 m b.s.l. Regression of the Ancylus Lake, dated at 9300 cal BP, was identified at a depth of 23 m b.s.l. The most pronounced period was the transition stage between the Ancylus Lake and the Littorina Sea. The record of the Littorina Sea onset in the sediments of the Arkona Basin is marked as a sudden increase in loss on ignition, biogenic silica, magnesium, calcium, iron and strontium. The age of the Littorina Sea in the Arkona Basin was estimated as younger than 8200 cal BP.

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Unexpected ice flow directions during the Late Weichselian deglaciation of the south Baltic area indicated by a new lithostratigraphy in NW Poland and NE Germany

Cited by 24 publications

References 14 publications

The pattern of glaciation on the Avalon Peninsula of Newfoundland

The pattern of glaciation on the Avalon Peninsula of Newfoundland

Topographically-controlled Deglacial History of the Humber River Basin, Western Newfoundland

Stages of the Baltic Sea evolution in the geochemical record and radiocarbon dating of sediment cores from the Arkona Basin

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