The Pleistocene of Newfoundland

Coleman, A. P.

doi:10.1086/623302

Cited by 16 publications

(9 citation statements)

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“…In contrast, Chamberlin (1895) suggested that the Avalon Peninsula had been covered by an independent, radially-flowing ice cap. The ice cap hypothesis was supported subsequently by Coleman (1926) and Summers (1949), based primarily on the absence of granitic erratics in the central part of the Avalon Peninsula. Summers (1949), however, noted granitic clasts derived from local Avalon sources, and reported ultramafic erratics of unknown provenance.…”

Section: Previous Workmentioning

confidence: 86%

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: Previous Workmentioning

confidence: 86%

The pattern of glaciation on the Avalon Peninsula of Newfoundland

Catto¹

2002

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“…He concluded that a noted tendency towards subspeciation was unlikely to have occurred in the short postglacial period; thus, adding further support to the idea of glacial refugia. Recent work by Ives (1975) Coleman (1926) probably misinterpreted intensive periglacial weathering of granite and granodiorite as being proof of ice-free areas during the Wisconsinan. It was commonly believed by his contemporaries that the Wisconsinan stage was an entity and not a series of retreats and advances as we now know.…”

Section: Discussionmentioning

confidence: 99%

“…In it, he proposed that the island had remained unglaciated during the Wisconsinan. His argument (1925) Coleman (1926) added further support to Fernald's hypothesis. He reported that he could find no evidence for glaciation of the southern part of the Long Range Mountains during the Pleistocene; further, ice that invaded the Northern Peninsula and the rest of the island was probably of Kansan or Jerseyan age.…”

Section: The Opposing Theoriesmentioning

confidence: 91%

“…It is hoped that a historic approach will shed light on how specific theories developed and were maintained, while at the same time re-emphasizing problems that still exist in determining the scope and sequence of Quaternary events. Many original ideas such as those of Murray (1864Murray ( , 1883, Fernald (1911Fernald ( , 1930, and Coleman (1926) have been obscured by more recent work, but in spite of improved logistics and research methods, several questions originally raised by the authors have yet to be resolved. Except for coastal events, the Quaternary of Newfoundland is, still, little understood.…”

Section: Introductionmentioning

confidence: 99%

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Quaternary Studies in Newfoundland: A Short Review

Tucker

1976

atgeol

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“…Fossiliferous sediment at 43 m asl between two units interpreted as tills was inferred by Coleman (1926) to represent an interglacial deposit near Corner Brook. MacClintock and Twenhofel (1940) considered this deposit, along with the large delta at the mouth of the Humber River at about 46-48 m asl, to be late-glacial.…”

Section: Marine Incursionmentioning

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 Pleistocene of Newfoundland

Cited by 16 publications

References 0 publications

The pattern of glaciation on the Avalon Peninsula of Newfoundland

The pattern of glaciation on the Avalon Peninsula of Newfoundland

Quaternary Studies in Newfoundland: A Short Review

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

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