Rhythmic Sedimentation in Glacial Lake Hitchcock, Massachusetts-Connecticut

Ashley, Gail M.

doi:10.2110/pec.75.23.0304

Cited by 133 publications

(105 citation statements)

References 17 publications

(17 reference statements)

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“…Varves consist of lamina couplets with a coarse-grained lower component associated According to the classification scheme of Ashley (1975), Green Lake varves are of Type II (clay cap thickness approximately equal to half the total varve thickness) and Type III (clay cap thickness less than half the total varve thickness), as shown in Figure 4. Type II varves, indicative of nearly equal classical 'summer' and 'winter' layers, are observed only in the distal basin.…”

Section: Varve Sequencesmentioning

confidence: 99%

Contemporary sedimentation rates and depositional structures in a montane lake basin, southern Coast Mountains, British Columbia, Canada

Schiefer

2006

Earth Surf Processes Landf

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Spatial variability of recent lacustrine sedimentary structures and sedimentation rates are examined for Green Lake, a morphologically complex lake basin of the southern Coast Mountains, British Columbia. A dense, 100 m grid sampling scheme was used for sediment coring within the 2 km 2 lake basin. Deltaic, massive, weakly laminated, and varved sediment sequences are identified within the sediment record. Spatial patterns among these sedimentary deposits are related to within-lake sediment transfer processes, morphometric controls, and the extent of post-depositional mixing by bioturbation. Unconformities, turbidites, and cohesive slump failure deposits, observed within the contemporary varve sequences, could all be correlated with major flooding events in the catchment area and direct anthropogenic disturbances along the shoreline. There is an overall, non-linear decrease in sedimentation rates with increasing distance from the lake inflows; however, this pattern is disrupted in deep water sites of intervening lake sub-basins where locally higher accumulation rates are observed. Spatial sedimentation patterns are quantitatively described by an empiricallyderived model. Systematic variations in the model parameters are observed for different lake sub-regions and are associated with changing sediment transfer dynamics between proximal and distal sub-basin settings.

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Section: Varve Sequencesmentioning

confidence: 99%

Contemporary sedimentation rates and depositional structures in a montane lake basin, southern Coast Mountains, British Columbia, Canada

Schiefer

2006

Earth Surf Processes Landf

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“…Partings of very fine sand are present within almost all summer layers; in two varves, these partings show distinct, NW-SE trending, parallel lineations that were presumably produced by turbidity currents. On the basis of examples given by Banerjee (1973) and Ashley (1975), these varves are interpreted as turbidites with (C)DE (t,h) -divisions (nomenclature of Walker, 1984). The attenuated covariation of winter and summer layer thicknesses in the entire varve series (Fig.…”

Section: Rivière Landry Sectionmentioning

confidence: 99%

Late Wisconsinan deglaciation and glacial lake development in the Appalachians of southeastern Québec

Parent¹,

Occhietti²

2002

gpq

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Late Wisconsinan deglaciation in southeastern Québec was preceded by a northward ice-flow reversal that was recorded in the northeastern part of the region. The reversal event was generated by flow convergence toward the St. Lawrence Ice Stream, a northeastward-flowing ice stream which formed in the St. Lawrence estuary prior to 13 000 years BP and lasted until at least 12 400 years BP. In the Bois-Francs uplands, the flow reversal event led to the formation of a semi-detached ice mass that underwent widespread stagnation and downwasting. In the southwestern region, northward retreat of the margin of the Laurentide Ice Sheet was marked by the formation of a series of discontinuous recessional moraines and by the development of ice-dammed lakes in the main valleys. The level of these lakes fell as progressively lower outlets became ice-free. The main episodes are (1) the Sherbrooke Phase of Glacial Lake Memphremagog, (2) an unnamed transitional lake and (3) Glacial Lake Candona, a large lake which had expanded northeastward from the deglaciated regions of the Upper St. Lawrence (Lake Iroquois) and Ottawa valleys to the Lake Champlain (Glacial Lake Vermont) basin. As recorded by the Danville Varves, Lake Candona lasted about 100 years following deposition of the Ulverton-Tingwick Moraine. Subsequent ice retreat along the Appalachian piedmont led to final drainage of Lake Candona and allowed Champlain Sea waters to invade much of these glaciolacustrine terrains about 12 000 years BP. On the basis of the Danville Varves record, a regional rate of ice retreat of about 200 m·a -1 is inferred. The age of the earliest moraine, the Frontier Moraine, is thus about 12 550 years BP, while the ages of the subsequent Dixville, Cherry River-East-Angus, Mont Ham and Ulverton-Tingwick moraines are estimated at 12 500, 12 325, 12 200 et 12 100 years BP, respectively.La déglaciation du Wisconsinien supérieur a été précédée d'une inversion d'écoulement glaciaire vers le nord. Cette inversion, enregistrée dans le nordest de la région, résulte de la convergence des glaces vers le Courant glaciaire du Saint-Laurent, lequel s'était formé dans l'estuaire du Saint-Lau- rent avant 13 000 ans BP et a duré au moins jusque vers 12 400 ans BP. Dans les hautes-terres des Bois-Francs, cette inversion d'écoulement a mené à l'isolement d'une masse glaciaire partiellement détachée et qui se dissipa tardivement. Dans le secteur sud-ouest, le retrait de l'Inlandsis est ponctué par la mise en place d'ensembles morainiques discontinus et par le développement de lacs proglaciaires barrés dans les vallées principales. Le niveau de ces lacs chutait à mesure que le retrait glaciaire libérait des cols de plus en plus bas. Les principaux épisodes sont : la Phase Sherbrooke du Lac glaciaire Memphrémagog ; un lac de transition ; le Lac glaciaire Candona, formé de la coalescence des lacs glaciaires endigués dans les vallées du haut Saint-Laurent, des Outaouais, du lac Champlain (Lac Vermont) et du Saint-François. Le Lac Candona a subsisté quelque ...

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“…Although referenced in the first of Flint's (1947) textbooks on glacial geology, his later two textbooks (Flint, 1957(Flint, , 1971, used by most students of glacial geology in North America for two decades, have no reference to Antevs' (1922Antevs' ( , 1928 work on varves in New England. More recent studies of varves in New England have focused on the sedimentology of the varve sequence, in particular depositional processes and facies changes associated with the varves, and have not addressed issues of chronology (Ashley, 1972(Ashley, , 1975Ashley et al, 1982). While most glacial geologists working in New England over the last half century have ignored varve chronology as a viable chronologic tool, many investigators (Lougee, 1935b;McNish and Johnson, 1938;Johnson et al, 1948;Verosub, 1979aVerosub, , 1979bThomas, 1984;Ridge and Larsen, 1990, Ridge et al, 1995, 1996Levy, 1998;T.…”

Section: Systematic Ice Recession In New Englandmentioning

confidence: 99%

Varve, paleomagnetic, and 14 C Chronologies for late Pleistocene events in New Hampshire and Vermont (U.S.A.)

Ridge¹,

Bensonen²,

Brochu³

et al. 2002

gpq

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A deglacial chronology for northern New England has been formulated using an atmospheric 14 C calibration of the New England Varve Chronology and paleomagnetic records. This 14 C chronology is based on 14 C ages from macrofossils of non-aquatic plants and is about 1 500 yr younger than existing chronologies that are based primarily on 14 C ages of bulk organic samples. The lower and upper Connecticut Valley varve sequences of Ernst Antevs (NE varves 2 701-6 352 and 6 601-8 500) overlap (lower 6 012 = upper 6 601) based on their crudely matching varve records and their similar paleomagnetic records. Three 14 C ages at Canoe Brook, Vermont (NE varve 6 150 = 12.3 14C ka) calibrate the lower Con necticut Valley sequence. New AMS and con ventional 14 C ages on woody twigs from Newbury, Vermont calibrate the upper se quence from 11.6-10.4 14 C ka (NE varves 7 440-8 660) and are consistent with the over lapping varve and paleomagnetic records, and the Canoe Brook 14 C ages. Deglaciation of the Connecticut Valley in southern Vermont began at 12.6 14 C ka (15.2 cal ka) and the Littleton-Bethlehem Readvance in northern New Hampshire and Vermont reached its maximum at11.9-11.8 14 C ka (14.0-13.9 cal ka) followed by recession of ice into Québec at about 11.5 14 C ka (13.4 cal ka). A lake persisted in the upper Connecticut Valley until at least 10.4 14 C ka (12.3 cal ka) and may have been seen by the first humans in the area.

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Rhythmic Sedimentation in Glacial Lake Hitchcock, Massachusetts-Connecticut

Cited by 133 publications

References 17 publications

Contemporary sedimentation rates and depositional structures in a montane lake basin, southern Coast Mountains, British Columbia, Canada

Contemporary sedimentation rates and depositional structures in a montane lake basin, southern Coast Mountains, British Columbia, Canada

Late Wisconsinan deglaciation and glacial lake development in the Appalachians of southeastern Québec

Varve, paleomagnetic, and 14 C Chronologies for late Pleistocene events in New Hampshire and Vermont (U.S.A.)

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