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The Pattern of Glaciation on the Avalon Peninsula of Newfoundland L’Histoire De La Glaciation De La Presqu’Île D’Avalon, À Terre-Neuve

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The Pattern of Glaciation on the Avalon Peninsula of Newfoundland L’Histoire De La Glaciation De La Presqu’Île D’Avalon, À Terre-Neuve Document généré le 26 sept. 2021 05:31 Géographie physique et Quaternaire The pattern of glaciation on the Avalon Peninsula of Newfoundland L’histoire de la glaciation de la presqu’île d’Avalon, à Terre-Neuve. Das Schema der Vereisung auf der Avalon-Halbinsel in Neufundland. Norm R. Catto Volume 52, numéro 1, 1998 Résumé de l'article L'histoire de la glaciation de la presqu'île d'Avalon a été établie à partir de URI : https://id.erudit.org/iderudit/004778ar l'étude des caractéristiques géomorphologiques, des stries et de la provenance DOI : https://doi.org/10.7202/004778ar des blocs erratiques. On distingue trois phases dans un continuum de glaciation. Pendant la première phase, il y a eu accumulation et dispersion de Aller au sommaire du numéro 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 Éditeur(s) 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 Les Presses de l'Université de Montréal 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 ISSN 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 0705-7199 (imprimé) commencé avant 10 100 ± 250 BP. L'évolution des calottes glaciaires de la 1492-143X (numérique) presqu'île d'Avalon a été déterminée par des événements régionaux et hémisphériques et par la réponse des glaciers laurentidiens. Découvrir la revue Citer cet article Catto, N. R. (1998). The pattern of glaciation on the Avalon Peninsula of Newfoundland. Géographie physique et Quaternaire, 52(1), 23–45. https://doi.org/10.7202/004778ar Tous droits réservés © Les Presses de l'Université de Montréal,1998 Ce document est protégé par la loi sur le droit d’auteur. L’utilisation des services d’Érudit (y compris la reproduction) est assujettie à sa politique d’utilisation que vous pouvez consulter en ligne. https://apropos.erudit.org/fr/usagers/politique-dutilisation/ Cet article est diffusé et préservé par Érudit. Érudit est un consortium interuniversitaire sans but lucratif composé de l’Université de Montréal, l’Université Laval et l’Université du Québec à Montréal. Il a pour mission la promotion et la valorisation de la recherche. https://www.erudit.org/fr/ Géographie physique et Quaternaire, 1998, vol. 52, n° 1, p. 1- 24, 16 fig. THE PATTERN OF GLACIATION ON THE AVALON PENINSULA OF NEWFOUNDLAND Norm R. CATTO, Department of Geography, Memorial University of Newfoundland, St. John's, Newfoundland, A1B 3X9, [email protected]. Manuscrit reçu le 21 mars 1996 ; manuscrit révisé et accepté le 22 août 1997 ABSTRACT,,16fig.N. 19952(1 R. 8, ),CATTO vol. 1998 52, n° 1 The pattern of glaciation on the RÉSUMÉ L‘histoire de la glaciation de la ZUSAMMENFASSUNG Das Schema der Avalon Peninsula has been established presqu'île d'Avalon, à Terre-Neuve.L'histoi- Vereisung auf der Avalon-Halbinsel in Neu- through study of geomorphic features, stria- re de la glaciation de la presqu'île d'Avalon a fundland. Das Schema der Vereisung auf tions, and erratic provenance. Three phases été établie à partir de l'étude des caractéris- der Avalon-Halbinsel wurde mittels des Stu- in a continuum of glaciation are recognized. tiques géomorphologiques, des stries et de diums der geomorphologischen Merkmale, The initial phase involved the expansion of la provenance des blocs erratiques. On dis- der Schrammen und der Herkunft der errati- ice from several centres. Ice thickness and tingue trois phases dans un continuum de schen Blöcke nachgezeichnet. In der An- extent reached a maximum during the sub- glaciation. Pendant la première phase, il y a fangsphase dehnte sich das Eis ausgehend sequent Phase 2 event, correlated with the eu accumulation et dispersion de la glace à von mehreren Zentren aus. Das Eis erreich- Late Wisconsinan. Lowered sea level per- partir de plusieurs centres. Au cours de la te ein Maximum an Dicke und Ausdehnung mitted the development of the St. Mary's Bay deuxième période, qui correspond au Wis- in der folgenden 2. Phase, die dem späten ice centre. Ice from the Newfoundland main- consinien supérieur, les glaciers ont atteint Wisconsin entspricht. Der niedrigere Mee- land coalesced with Avalon Peninsula ice in un maximum en étendue et en épaisseur. Le resspiegel ermöglichte die Entwicklung des Placentia Bay, on the Isthmus, and in Trinity niveau marin abaissé a permis la formation Eiszentrums der St. Mary's -Bai. Das Eis Bay. Rising sea level, triggered by the retreat d'un centre glaciaire à l'emplacement de la vom Festland Neufundlands vereinigte sich of Laurentide ice in Labrador, resulted in de- baie St. Mary. Le glacier en provenance de mit dem Eis der Avalon-Halbinsel in der Pla- stabilization of the St. Mary's Bay ice cap, la partie continentale de Terre-Neuve a fu- centia-Bai, auf dem Isthmus und in der Trini- marking Phase 3. Final deglaciation of the sionné avec celui de la presqu'île d'Avalon ty-Bai. In Phase 3 führte ein ansteigender Avalon Peninsula began before 10,100 ± dans la baie de Plaisance, sur l'isthme et Meeresspiegel, ausgelöst durch den Rück- 250 BP. The Avalon Peninsula ice caps were dans la baie de la Trinité. La troisième pha- zug des laurentischen Eises in Labrador, zur controlled by regional and hemispheric se, caractérisée par la remontée du niveau Destabilisierung der Eiskappe der St. Ma- events, and by the response of the Lauren- marin et déclenchée par le recul de l'Inland- ry's-Bai. Die endgültige Enteisung der Ava- tide glaciers. sis laurentidien au Labrador, a déséquilibré lon-Halbinsel begann vor 10 100 ± 250 la calotte glaciaire de St. Mary. La déglacia- v.u.Z. tion finale de la presqu'île d'Avalon a com- mencé avant 10 100 ± 250 BP. L'évolution des calottes glaciaires de la presqu'île d'Avalon a été déterminée par des événe- ments régionaux et hémisphériques et par la réponse des glaciers laurentidiens. 2 N. R. CATTO INTRODUCTION west. Heights of land follow the axes of the sub-peninsulas, with maximum elevations in excess of 330 m. Most of the Investigation and assessment of ice-flow directions in area is below 150 m a.s.l. regions marked by limited sedimentary deposition repre- The heights of land throughout the Avalon Peninsula fol- sents a complex but persistent problem in Quaternary stud- low the axes of the major sub-peninsulas, resulting in the ies. Although recognition of the occurrence of glaciation is development of drainage systems marked by short, steep generally a straightforward matter, more precise understand- gradient streams with small catchment areas. The bays ing of the patterns of glacial movement is required for geo- between the sub-peninsulas vary in depth. The maximum technical or resource management purposes. In addition, depths in Conception Bay (in excess of 280 m), Placentia construction of glaciological or glacio-climatic models Bay (in excess of 300 m), and Trinity Bay (in excess of 580 requires information concerning glacial extents, volumes, m) follow the structural trends. In contrast, St. Mary's Bay is and accumulation areas. The more recent of these models relatively shallow, with a maximum depth of 210 m and a attempt to incorporate data from localized glacial sources modal depth of 120 m south of Great Colinet Island. Sea- surrounding the North Atlantic, as well as that related to the ward access to the bay is further impaired by the shallow St. Laurentide and Fennoscandian glaciers (e.g. Velichko et al., Mary's Bank, with a maximum depth of 65 m, extending 1997). across the mouth of the bay from St. Shotts to Point Lance. Throughout Atlantic Canada, the hypothesis of multiple glacial ice caps independent of the Laurentide Ice Sheet PREVIOUS WORK complex has gained support through numerous investiga- tions (e.g. Chalmers, 1895; Jenness, 1960; Prest, 1973; After erratic boulders and glacial features on the Avalon Grant, 1974, 1977, 1989; Brookes, 1982, 1989; Seaman et Peninsula were recognized (Jukes, 1842, 1843; Kerr, 1870; al. ,1991; Stea et al. ,1992; Stea, 1995). Assessment of the Milne, 1874, 1876, 1877; Packard, 1876), debate centred directions of ice movement necessary to support these upon the origin of the glacial features. Several authors, hypotheses has necessitated careful examination of all gla- including Murray (1883), Flint (1940), Twenhofel and Mac- cigenic depositional and erosional features, with heavy reli- Clintock (1940), and Tanner (1944), advanced the view that ance on geomorphic forms and the distribution of glacially the Avalon Peninsula was glaciated by ice originating to the transported erratics, and with the realization that these indi- northwest, either from the main part of Newfoundland or cators may produce results that initially seem incompatible from the Laurentide complex based in western Labrador. In (cf. Schau, 1981). contrast, Chamberlin (1895) suggested that the Avalon Pen- insula had been covered by an independent, radially-flowing The Avalon Peninsula is one region in Atlantic Canada ice cap. The ice cap hypothesis was supported subsequently that has been postulated to have supported one or more by Coleman (1926) and Summers (1949), based primarily on independent ice caps. Investigation of the Avalon Peninsula, the absence of granitic erratics in the central part of the Ava- therefore, serves as an illustration of the applicability of lon Peninsula.
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