The evolution of glacial lakes Barlow and Ojibway, Quebec and Ontario

Vincent, J S; Hardy, Liana

doi:10.4095/106036

Cited by 44 publications

(88 citation statements)

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“…Specifically, these are the presence of an actively erupting volcano within the reservoir and the fact that the reservoir could be rapidly overfilled because the lake level was not subject to a topographic control. At the time of the final flood from Lake Agassiz, the lake level is thought to have been controlled by a spillway that routed water through the valley of the Kinoje´vis River to the valley of the Ottawa River (Vincent and Hardy, 1979;Veillette, 1994;Leverington et al, 2002). We estimated the height of this spillway as 230 m above sea level at that time.…”

Section: Sheet-like Outbursts From Contemporary Reservoirsmentioning

confidence: 99%

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Clarke

Leverington

Teller

et al. 2005

Quaternary Science Reviews

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Section: Sheet-like Outbursts From Contemporary Reservoirsmentioning

confidence: 99%

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Clarke

Leverington

Teller

et al. 2005

Quaternary Science Reviews

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“…Lake Agassiz-Ojibway drained through the Kinojévis outlet to the Ottawa River Valley until the LIS no longer provided a barrier to northward outflow into the Tyrrell Sea (Vincent and Hardy, 1979). Catastrophic northward drainage into the Tyrrell Sea, possibly initiated in the region north of modern James Bay, is believed to have followed the collapse of the confining ice margin at about 7700 14 C yr B.P.…”

Section: Figmentioning

confidence: 99%

“…The form of the rebound curve used to reconstruct lake bathymetry at the Kinojévis stage was based on that for the Ponton stage (Thorleifson, 1996), with the trends of associated isobases modified in the east so that the 300-m isobase approximately intersects the Kinojévis outlet (see Vincent and Hardy, 1979, their fig. 3-I).…”

Section: Rebound Surfacesmentioning

confidence: 99%

“…2f), a possible final lake stage, is given here only for regions west of the Cochrane II ice advance (this advance is described by Vincent andHardy, 1979, andVeillette, 1994). The level of the Fidler stage is based on Klassen's (1983) identification of a beach along a moraine in northern Manitoba, which today lies about 80 m below the Ponton beach.…”

Section: Area Volume and Bathymetrymentioning

confidence: 99%

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Changes in the Bathymetry and Volume of Glacial Lake Agassiz Between 11,000 and 9300 ¹⁴C yr B.P.

2000

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Computer reconstructions of the bathymetry of the lake were used to quantify variations in the size and form of Lake Agassiz during its final two phases (the Nipigon and Ojibway phases), between about 9200 and 7700 14 C yr B.P. (ca. 10,300-8400 cal yr B.P.). New bathymetric models for four Nipigon Phase stages (corresponding to the McCauleyville, Hillsboro, Burnside, and The Pas strandlines) indicate that Lake Agassiz ranged between about 19,200 and 4600 km 3 in volume and 254,000 and 151,000 km 2 in areal extent at those times. A bathymetric model of the last (Ponton) stage of the lake, corresponding to the period in which Lake Agassiz was combined with glacial Lake Ojbway to the east, shows that Lake AgassizOjibway was about 163,000 km 3 in volume and 841,000 km 2 in areal extent prior to the final release of lake waters into the Tyrrell Sea. During the Nipigon Phase, a number of catastrophic releases of water from Lake Agassiz occurred as more northerly (lower) outlets were made available by the retreating southern margin of the Laurentide Ice Sheet; we estimate that each of the four newly investigated Nipigon Phase releases involved water volumes of between 1600 and 2300 km 3 . The final release of Lake Agassiz waters into the Tyrrell Sea at about 7700 14 C yr B.P. is estimated to have been about 163,000 km 3 in volume. C 2002 University of Washington.

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“…The paleogeography of individual basins and of the entire Great Lakes watershed may likewise be reconstructed for any desired age. Applications of the isostatic response surface and the exponential model of uplift are illustrated for: (1) digital reconstruction of Great Lakes Clayton, 1983;Teller and Thorleifson, 1983;Teller, 1985;Thorleifson, 1996 Vincent andHardy, 1979;Veillette, 1994;Dyke, 1996Calkin, 1970Barnett, 1979;Calkin andFeenstra, 1985 Goldthwait, 1910;Stanley, 1936Stanley, , 1937Stanley, , 1938aDeane, 1950;Chapman, 1975;Karrow et al, 1975;Karrow 1980;Chapman and Putnam, 1984;Eschman and Karrow, 1985;Kaszycki, 1985;Karrow, 1986Karrow, , 1987Lewis and Anderson, 1989;Lewis et al 1994Goldthwait, 1907Leverett and Taylor, 1915;Stanley, 1938b;Evenson, 1973;Futyma, 1981;Hansel et al, 1985;Taylor, 1990;Kehew, 1993;Colman et al 1994aColeman, 1937Muller and Prest, 1985;Pair et al, 1988;Rodrigues, 1993 Harrison, 1972;Chapman, 1975;Vincent and Hardy, 1979;Barnett, 1988;…”

Section: Introductionmentioning

confidence: 99%

Glacial Isostatic Adjustment of the Laurentian Great Lakes Basin: Using the Empirical Record of Strandline Deformation for Reconstruction of Early Holocene Paleo-Lakes and Discovery of a Hydrologically Closed Phase*

Lewis

Blasco

Gareau³

2007

gpq

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In the Great Lakes region, the vertical motion of crustal rebound since the last glaciation has decelerated with time, and is described by exponential decay constrained by observed warping of strandlines of former lakes. A composite isostatic response surface relative to an area southwest of Lake Michigan beyond the limit of the last glacial maximum was prepared for the complete Great Lakes watershed at 10.6 ka BP (12.6 cal ka BP). Uplift of sites computed using values from the response surface facilitated the transformation of a digital elevation model of the present Great Lakes basins to represent the paleogeography of the watershed at selected times. Similarly, the original elevations of radiocarbon-dated geomorphic and stratigraphic indicators of former lake levels were reconstructed and plotted against age to define lake level history. A comparison with the independently computed basin outlet paleo-elevations reveals a phase of severely reduced water levels and hydrologically-closed lakes below overflow outlets between 7.9 and 7.0 ka BP (8.7 and 7.8 cal ka BP) in the Huron-Michigan basin. Severe evaporative draw-down is postulated to result from the early Holocene dry climate when inflows of meltwater from the upstream Agassiz basin began to bypass the upper Great Lakes basin.Dans la région des Grands Lacs, le soulèvement isostatique lié à la dernière glaciation a ralenti selon une courbe de décroissance exponentielle établie à partir du gauchissement observé dans les anciennes lignes de rivage lacustres. Une surface de référence composite de la réponse isostatique datant de 10,6 ka BP (12,6 cal ka BP) a été préparée pour l’ensemble du bassin-versant des Grands Lacs, par rapport à une région au sud-ouest du lac Michigan située au-delà de la limite du dernier maximum glaciaire. Le calcul du soulèvement des sites en fonction des altitudes de la surface de référence a facilité la conversion d’un modèle altimétrique de terrain du bassin actuel des Grands Lacs en des cartes paléo-géographiques pour différents âges choisis. De plus, afin de définir l’évolution des niveaux lacustres, les altitudes initiales des indicateurs géomorphologiques et stratigraphiques des paléo-niveaux lacustres, datés au 14C, ont été reconstituées puis reportées en fonction de l’âge. La comparaison de cette courbe à celles des paléo-altitudes des exutoires lacustres, calculée indépendamment, révèle, entre 7,9 et 7 ka BP (8,7 et 7,8 cal ka BP), une phase d’abaissement majeur des niveaux lacustres au-dessous de ceux des exutoires et la fermeture hydrologique des lacs dans le bassin des lacs Huron-Michigan. La forte évaporation nécessaire à l’abaissement du niveau d’eau est attribuée à un climat sec peu après le début de l’Holocène, dans un contexte de détournement progressif hors des Grands Lacs des eaux de fonte du lac Agassiz

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The evolution of glacial lakes Barlow and Ojibway, Quebec and Ontario

Cited by 44 publications

References 0 publications

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Changes in the Bathymetry and Volume of Glacial Lake Agassiz Between 11,000 and 9300 ¹⁴C yr B.P.

Glacial Isostatic Adjustment of the Laurentian Great Lakes Basin: Using the Empirical Record of Strandline Deformation for Reconstruction of Early Holocene Paleo-Lakes and Discovery of a Hydrologically Closed Phase*

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The evolution of glacial lakes Barlow and Ojibway, Quebec and Ontario

Cited by 44 publications

References 0 publications

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Fresh arguments against the Shaw megaflood hypothesis. A reply to comments by David Sharpe on “Paleohydraulics of the last outburst flood from glacial Lake Agassiz and the 8200 BP cold event”

Changes in the Bathymetry and Volume of Glacial Lake Agassiz Between 11,000 and 9300 14C yr B.P.

Glacial Isostatic Adjustment of the Laurentian Great Lakes Basin: Using the Empirical Record of Strandline Deformation for Reconstruction of Early Holocene Paleo-Lakes and Discovery of a Hydrologically Closed Phase*

Contact Info

Product

Resources

About

Changes in the Bathymetry and Volume of Glacial Lake Agassiz Between 11,000 and 9300 ¹⁴C yr B.P.