Stratigraphy, paleoceanography, chronology, and environment during deglaciation of eastern Maine

Dorion, Christopher C.; Balco, G.; Kaplan, Michael R.; Kreutz, K. J.; Wright, James D.; Borns, Harold W.

doi:10.1130/0-8137-2351-5.215

Cited by 26 publications

(37 citation statements)

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“…See Vincent (1989) and Veillette (1996) for the other moraines. Areas in gray on the southern side of the Gulf of St. Lawrence are related to Younger Dryas local glaciers, from Richard et al (1997), Dorion et al (2001) and Stea and Mott (2005). Moraines, eskers et limites proposées du Dryas récent sur la marge sud-est de l'Inlandsis laurentidien, au Québec et au Labrador.…”

Section: Methodsunclassified

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The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

Occhietti

2010

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The Saint-Narcisse morainic complex extends over 750 km along the southern margin of the Laurentian Highlands in Québec, north of the St. Lawrence Valley, between the Ottawa and Saguenay Rivers. To the east, the Laurentide Ice Sheet margin was located in the present St. Lawrence Estuary. To the west, the morainic complex is extended 235 km west of the Ottawa River to the Algonquin Highlands, in Ontario. The general outline of the morainic complex comprises large lobes and reentrants, related to major topographic features. In the lower Saint-Maurice River area, the moraine is composed of reworked clay and till and proximal glaciomarine deposits (Yamachiche Diamicton) and melt-out till and ice-marginal outwash (Charette Drift). The Saint-Narcisse Event can be subdivided in several phases: local readvance in low areas, main phase at the origin of the Saint-Narcisse Moraine s.s., melting-out of the marginal ice with compressive structures and large proglacial outwash features, and slow retreat with secondary ridges. The accuracy of the chronological data is limited by several factors: and a floating chronology is proposed. Two landmarks constrain the age and range of duration of the main Saint-Narcisse phase. The main ridge deposition occured after the onset, ca. 12.9 cal ka, of Champlain Sea in the St. Lawrence Valley, and a rapid ice retreat on the southern edge of the Laurentians. It ended before the drawdowm, in the Lake Huron basin, of Glacial Lake Algonquin ca. 12.5 cal ka. The Saint-Narcisse Event is related to the early cold phase of Younger Dryas, as evidenced by other YD ice readvances in Maine, Nova Scotia, and ice cover on the Gaspé Peninsula. It corresponds to a positive change of the budget of the Laurentide Ice Sheet as a result of climate forcing. After a slow ice front retreat during about 900-700 yr, the final phase of YD is marked by the Mars-Batiscan Moraine, located 17 to 70 km north of the Saint-Narcisse Moraine.Le complexe morainique de Saint-Narcisse s’étend sur 750 km le long de la marge méridionale des Laurentides, au Québec, au nord de la vallée du Saint-Laurent, entre l’Outaouais et le Saguenay. Vers l’est, la marge glaciaire était située dans l’estuaire actuel du Saint-Laurent. Vers l’ouest, en Ontario, les formes associées sont suivies dans le massif Algonquin, jusqu’à 235 km de l’Outaouais. Le tracé général du complexe inclut de grands lobes et rentrants liés à la topographie. Dans la basse vallée du Saint-Maurice, la Moraine de Saint-Narcisse est composée de dépôts glaciomarins proximaux, de till et d’argile marine remaniée (Diamicton de Yamachiche) et de till de fusion sur place et de dépôts fluvioglaciaires et juxtaglaciaires (Dépôts de Charette). L’Épisode de Saint-Narcisse est subdivisé en plusieurs phases non nécessairement synchrones sur toute la marge glaciaire: réavancée locale dans les dépressions importantes, phase majeure de stabilisation à l’origine de la Moraine de Saint-Narcisse, fonte sur place indiquée par des structures imbriquées et épandages proglaciaires, puis retra...

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Section: Methodsunclassified

“…Voir Vincent (1989) et Veillette (1996 pour les autres moraines. Les surfaces en gris au sud du Golfe du Saint-Laurent correspondent aux glaciers locaux du Dryas récent, d'après Richard et al (1997), Dorion et al (2001) et Stea et Mott (2005).…”

Section: Methodsunclassified

The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

Occhietti

2010

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“…As the marine ice margin retreated inland, vigorous streams emerged from beneath the ice and built submarine fans along the margin (Ashley et al, 1991;Borns et al, 2004;Dorion et al, 2001;Hooke and Fastook, 2007;Hunter et al, 1996). Where the margin was stable for a sufficiently long period of time, the fans reached sea level and became deltas.…”

Section: Deglaciation and Eskersmentioning

confidence: 99%

“…Two 14 C dates (Dorion et al, 2001) on marine shells interbedded with diamicton on the ice-distal side of the Pond Ridge moraine at Turner Brook (Figure 1) yield a calibrated mean age of 16.0 ± 0.2 ka. Consistent with this age are (1) a minimum age of 15.5 ± 0.2 ka from glaciomarine facies overlying the moraine at Sprague Neck, 5 km west of Turner Brook (Dorion et al, 2001) and (2) a maximum age of 16.4 ± 0.1 ka from laminated silt underlying diamicton at Dennison Point, 3 km outside the moraine (Kaplan, 1999).…”

Section: Dating the Retreatmentioning

confidence: 99%

Late glacial and Holocene history of the Penobscot River in the Penobscot Lowland, Maine

et al. 2016

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When the Laurentide ice sheet retreated rapidly (~150 m/a) across the Penobscot Lowland between ~16 and ~15 ka, the area was isostatically depressed and became inundated by the sea. Silt and clay were deposited, but no significant moraines or deltas were formed. The Penobscot River was reborn at ~14 ka when ice retreated onto land in the upper reaches of the river’s East Branch. As isostatic rebound exceeded sea level rise from melting ice, the river extended itself southward. Between ~13.4 and 12.8 ka, it established a course across marine clay and underlying glacial till in the Lowland. Its gradient was low as differential rebound had not begun. Discharge, however, was higher and the river transported and deposited outwash gravel. During the cold, dry Younger Dryas, ~11 ka, eolian sand began to accumulate in dunes in the Lowland. Some of this sand, along with fluvial sediment from the headwaters, was redistributed into terraces along gentler stretches of the river and into a paleodelta in Penobscot Bay. Eolian activity continued to ~8 ka and aggradation in terraces until ~6 ka. The climate became wetter and warmer after ~6 ka, the dunes were stabilized by vegetation, the river began to downcut, and braiding became less intense. Pauses in the downcutting are reflected in discontinuous strath terraces. In due course, the river re-encountered the old outwash gravels, marine clay, glacial till, and, in a few places, bedrock. Its profile is now stepped, with gentle, gravel-bedded reaches between bedrock ribs that form rapids.

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“…Late Wisconsinan glaciers retreated from the Maine coast between 15 and 13 ka (Dorion et al 2001), leaving heterogeneous deposits of till, glacial outwash, and glacialmarine mud across the present seafloor (Belknap and Shipp 1991). Glacial-marine (GM) muddy sediments commonly cover rock and till seaward of the late Pleistocene marine limit (Thompson and Borns 1985).…”

Section: Physical Settingmentioning

confidence: 99%

More than a century of bathymetric observations and present-day shallow sediment characterization in Belfast Bay, Maine, USA: implications for pockmark field longevity

et al. 2011

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Mechanisms and timescales responsible for pockmark formation and maintenance remain uncertain, especially in areas lacking extensive thermogenic fluid deposits (e.g., previously glaciated estuaries). This study characterizes seafloor activity in the Belfast Bay, Maine nearshore pockmark field using (1) three swath bathymetry datasets collected between 1999 and 2008, complemented by analyses of shallow box-core samples for radionuclide activity and undrained shear strength, and (2) historical bathymetric data (report and smooth sheets from 1872, 1947, 1948). In addition, because repeat swath bathymetry surveys are an emerging data source, we present a selected literature review of recent studies using such datasets for seafloor change analysis. This study is the first to apply the method to a pockmark field, and characterizes macro-scale (>5 m) evolution of tens of square kilometers of highly irregular seafloor. Presence/absence analysis yielded no change in pockmark frequency or distribution over a 9-year period (1999)(2000)(2001)(2002)(2003)(2004)(2005)(2006)(2007)(2008). In that time pockmarks did not detectably enlarge, truncate, elongate, or combine. Historical data indicate that pockmark chains already existed in the 19th century. Despite the lack of macroscopic changes in the field, near-bed undrained shear-strength values of less than 7 kPa and scattered downcore 137 Cs signatures indicate a highly disturbed setting. Integrating these findings with independent geophysical and geochemical observations made in the pockmark field, it can be concluded that (1) large-scale sediment resuspension and dispersion related to pockmark formation and failure do not occur frequently within this field, and (2) pockmarks can persevere in a dynamic estuarine setting that exhibits minimal modern fluid venting. Although pockmarks are conventionally thought to be long-lived features maintained by a combination of fluid venting and minimal sediment accumulation, this suggests that other mechanisms may be equally active in maintaining such irregular seafloor morphology. One such mechanism could be upwelling within pockmarks induced by near-bed currents.

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Stratigraphy, paleoceanography, chronology, and environment during deglaciation of eastern Maine

Cited by 26 publications

References 0 publications

The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

Late glacial and Holocene history of the Penobscot River in the Penobscot Lowland, Maine

More than a century of bathymetric observations and present-day shallow sediment characterization in Belfast Bay, Maine, USA: implications for pockmark field longevity

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