|Location||Manitoba, Ontario, and Saskatchewan in Canada; Minnesota and North Dakota in the U.S.|
|Lake type||proglacial lake|
|Primary inflows||Laurentide Ice Sheet|
|Primary outflows||Glacial River Warren, the Vermilion River, the Wanapitei River and the Montreal River valley |
|Basin countries||Canada, United States|
|First flooded||12,875 years before present|
|Max. length||475 miles (764 km)|
|Max. width||296 miles (476 km)|
|Surface area||300,000 km2 (115,831 sq mi) |
|Surface elevation||335 metres (1,099 ft),|
258 metres (846 ft),
|References||Coleman, Arthur Philemon, (1909) "Lake Ojibway; Last of the Great Glacial Lakes". Ontario Bureau of Mines. Report 18 (4): 284–293. Retrieved 30 October 2015.|
Lake Agassiz was a large glacial lake in central North America. Fed by glacial meltwater at the end of the last glacial period, its area was larger than all of the modern Great Lakes combined, although its mean depth was not as great as that of many major lakes today.
During the last Ice Age, northern North America was covered by an ice sheet, which alternately advanced and retreated with variations in the climate. This continental ice sheet formed during the period now known as the Wisconsin glaciation, and covered much of central North America between 30,000 and 10,000 years ago. As the ice sheet disintegrated, its meltwaters created an immense proglacial lake.
Around 13,000 years ago, this lake came to cover much of what are now Manitoba, northwestern Ontario, northern Minnesota, eastern North Dakota, and Saskatchewan. At its greatest extent, it may have covered as much as 440,000 km2 (170,000 sq mi), larger than any currently existing lake in the world (including the Caspian Sea) and approximately the area of the Black Sea.
At times the lake drained south through the Traverse Gap into Glacial River Warren (parent to the Minnesota River, a tributary of the Mississippi River), east through Lake Kelvin (modern Lake Nipigon) to what is now Lake Superior, and northwest through the Clearwater Spillway to the Mackenzie River System and the Arctic Ocean about 13,000 years ago.
The ice returned to the south for a time, but as it again retreated north of the present Canada–United States border around 10,000 years ago, Lake Agassiz refilled. The last major shift in drainage occurred around 8,200 years ago. The melting of remaining Hudson Bay ice caused Lake Agassiz to drain nearly completely. This final drainage of Lake Agassiz has been associated with an estimated 0.8 to 2.8 m (2.6 to 9.2 ft) rise in global sea levels.
Lake Agassiz's major drainage reorganization events were of such magnitudes that they had significant impact on climate, sea level and possibly early human civilization. The lake's enormous freshwater release into the Arctic Ocean has been postulated to have disrupted oceanic circulation and caused temporary cooling. The draining of 13,000 years ago may be the cause of the Younger Dryas stadial. Although disputed, the draining at 9,900–10,000 years ago may be the cause of the 8,200 yr climate event. A recent study by Turney and Brown links the 8,500-years ago drainage to the expansion of agriculture from east to west across Europe; they suggest that this may also account for various flood myths of prehistoric cultures, including the Biblical flood narrative.
Glacial River Warren outlet
The lowest point between the drainage of Hudson Bay and the Gulf of Mexico is in the Traverse Gap between the U.S. states of Minnesota and South Dakota. It lies between Lake Traverse and Big Stone Lake. This continental divide is about 300 metres (980 ft) above sea level. When Lake Agassiz existed, the gap was the outlet of River Warren. The outflow from the melting glaciers filled Lake Agassiz and then drained through the gap to the Gulf of Mexico. This mass of moving water eroded a valley about 2–5 kilometres (1.2–3.1 mi) wide and from 100 feet (30 m) to 125 feet (38 m) deep. Today, this valley contains the Minnesota River, joined by the Upper Mississippi River at Fort Snelling, Minnesota. The northern part of the former lakebed is the valley of the Red River of the North, which flows northward to Lake Winnipeg.
In this section, YBP denotes years before present.
Lockhart Phase: 12,875–12,560 YBP
During the Lockhart Phase, water accumulated in the Red River valley of North Dakota and Minnesota. As the water reached to the top of the divide to the south, the water drained into the ancestral Minnesota and Mississippi River system. This occurred while the Laurentian Ice Sheet was at or below the current Canada–US border. As the ice sheet melted northward, an early Lake Agassiz covered southern Manitoba, the Minnesota and Ontario boundary country, and along the Red River south of Fargo, North Dakota. The Lockhart phase is associated with the Herman lake stage (335 metres (1,099 ft)), the highest shoreline of Lake Agassiz. The Big Stone Moraine formed the southern boundary of the lake. During the Lockhart Phase the lake is estimated to have been 231 metres (758 ft) deep, with greater depths near the glacier.
Moorhead Phase: 12,560–11,690 YBP
As the ice sheet melted northward, Lake Agassiz found a lower outlet through the Kaministikwia route along the modern Minnesota–Ontario border. This moved water to Lake Duluth, a proglacial lake in the Lake Superior basin. From there the water drained south via an ancestral St. Croix and Mississippi River system. The lake drained below the Herman lake beaches until isostatic rebound and glacial advances closed the Kaministikwia route. This stabilized the lake at the Norcross lake stage (325 metres (1,066 ft)). The average depth of Lake Agassiz during the late Moorhead Phase was 258 metres (846 ft). Drainage from Lake Agassiz continued to flow southward out of the ancient Minnesota and Mississippi River systems into the Gulf of Mexico.
Emerson Phase: 11,690–10,630 YBP
During the Emerson Phase, lake levels and drainage patterns continually fluctuated. The lake switched from a southward outlet to a northwestern outlet, and may have been static without a significant outlet during this phase. Isostatic rebound changed the altitude of the land, and this, combined with changes in the volume of meltwater from the ice margin and the closure of the Kaministikwia outlet in the east increased the size of the northern end of the lake. One hypothesis postulates that the lake was a ‘terminal lake’ with water inflows and evapotranspiration being equal. Dating of the glacial moraines shows that the Clearwater and Athabasca River system and Lake Nipigon and Minong basin were still ice-covered. A period of precipitation and meltwater input balance with the rate of evapotranspiration may have existed for a short period of time. During this phase, the Clearwater and Athabasca River system outlet opened. Isostatic rebound opened the southern outlet for a time, creating the Norcross (325 metres (1,066 ft)), Tintah (310 metres (1,020 ft)), and Upper Campbell (299 metres (981 ft)) beaches. The south outlet was permanently closed at the end of Emerson Phase.
Nipigon Phase: 10,630–9,160 YBP
The opening of the Kaministiquia outlet to the east initiated the onset of the Nipigon Phase. The lower lake level ended the southern outlet through the ancestral Minnesota and Mississippi River system. The ice sheets advanced and blocked the northwestern outlet through the Clearwater and Athabasca system. There were several other low level outlets into the Lake Minong basin, including the Kaministiquia and the Lake Nipigon outlet. These allowed large amounts of water to flow from Lake Agassiz into Lake Minong. A series of ice advances and retreats between 10,500 and 9,500 YBP blocked the Lake Nipigon outlet and the other low level outlets, creating intermittent catastrophic outbursts of water into the Lake Minong basin.
These large inflows of water raised Lake Minong lake levels and flowed into Lake Algonquin in the Lake Michigan/Huron basin. These outbursts refilled the Lake Michigan and Huron basins, which are extreme low water levels of the Lake Chippewa (Lake Michigan basin) and Lake Stanley (Lake Huron basin). This was due to isostatic rebound of the northern shorelines combined with the opening of the North Bay outlet of the Lake Huron basin. These repetitive outbursts from Lake Agassiz flooded the Lake Minong basin, then flowed over into the Lake Stanley basin, and then flowed through the North Bay drainage route into the Champlain Sea (present day St. Lawrence lowland). The shifting ice sheet created fluctuating drainage channels into the Lake Nipigon and Superior basin. A dozen beaches were created during short periods of stability. Towards the end of the Nipigon Phase, Lake Agassiz reached its largest geographical size as it joined with Lake Ojibway in the east.
Ojibway Phase: 9,160–8,480 YBP
The Ojibway Phase is named for the glacial lake along the ice front in northern Ontario. Lake Ojibway merged with Lake Agassiz at this time. Isostatic rebound of glaciated lands that were south of the ice sheet created a long linear lake from the Saskatchewan–Manitoba border to Quebec. This long lake drained through the eastern outlet at Kinojevis River, into the Ottawa River valley. Lake Agassiz-Ojibway drainage raised sea levels. The results can be seen in Nova Scotia, New Brunswick, and eastern Maine. Marine records from the North Atlantic have identified two separate episodes, linked to northern hemisphere cooling in 8,490 YBP and 8,340–8,180 YBP. These may be linked with the Ojibway Phase of Lake Agassiz and may indicate large amounts of drainage from the Ottawa River valley and the Tyrrell Sea (ancestral Hudson Bay).
The Laurentide Ice Sheet continued to recede. Continued warming shrank the ice front towards present day Hudson Bay. Here, the Lake Agassiz northward outlet drained into the Tyrrell Sea. This breach dropped the water level below the eastern Kinojevis outlet. The drainage was followed by the disintegration of the adjacent ice front at about 8,480 YBP. This brought on the end of Lake Agassiz. The ice sheet continued its northward retreat to Baffin Island, leaving the North American mainland around 5,000 YBP.
Lakes of the Lake Agassiz basin
Numerous lakes have formed in this glacial lake basin. The best known are the Great Lakes of Manitoba; Lake Winnipeg, Lake Manitoba, and Lake Winnipegosis. A cluster of smaller lakes surround these, including: Cedar Lake, through which the Saskatchewan River flows; Lake Dauphin, south of Lake Winnipegosis and tributary to it; and Lake St. Martin, on the Fairford or Little Saskatchewan River, the outlet of Lakes Manitoba and Winnipegosis. In northern Minnesota, there are Roseau, Thief, Mud, and Maple lakes, besides three large lakes of that state, Rainy Lake, the Lake of the Woods, and Red Lake.
|Lake Winnipeg||250 miles (400 km)||The southern area is 25 miles (40 km) wide. The northern area is 60 miles (97 km) wide.||9,465 square miles (24,510 km2)||85 miles to a strait 2 miles (3 km) to 4 miles (6 km) wide, which extends 12 miles (19 km) to Cape Dog. The narrowest is about 1 mile (1.6 km) wide with five-sixths of the lake north of the cape, and one-sixth south.||710 feet above sea level.||Max. depth < 65 feet (20 m). Much is 6–7 feet deep||Nelson River|
|Lake Manitoba||120 miles||28 miles (south end)||1,785 square miles (4,623 km²)||Narrows to a strait of 2 miles width, becoming irregular to the north.||809 feet||23 feet||Fairford River to Lake Winnipeg|
|Lake Winnipegosis||150 miles with the northern portion bent towards the west.||5 to 15 miles||2,070 square miles (5,361 km²)||Lies in the same valley as Lake Manitoba, parallel to Lake Winnipeg.||833 feet||39 feet||Water Hen River and Lake to Lake Manitoba|
|Rainy Lake||50 miles, with the northern portion bent towards the west.||5 miles||360 square miles (932 km²)||Numerous bays, narrows and islands.||1117 feet||110 feet||Rainy River to Lake of the Woods|
|Lake of the Woods||60 miles, with the northern portion bent towards the west.||60 miles||1,679 square miles (4,349 km²)||Irregularly shaped with a substantial peninsula on the west side.||1060 feet||84 feet||Winnipeg River to Lake Winnipeg|
|Red Lake||20 miles for each lobe with a total of 30 miles across both.||10 miles for each lobe.||427 square miles (1,106 km²)||Divided into two equal areas by a strait 3/4 of a mile wide.||1172 feet||84 feet||Red Lake River to the Red River of the North and Lake Winnipeg.|
Glacial lakes draining into Lake Agassiz
Glacial Lake Souris formed along the Manitoba and North Dakota border, forming a crescent around the west side of the Turtle Mountains. Lake Souris had three successive outlets: the Sheyenne River, the Pembina River, and finally the Assiniboine River. Initially, Lake Souris' southern bay drained into the Sheyenne River, a tributary of the Red River, which in turn flowed into Lake Agassiz. However, after the ice sheet had retreated enough to uncover Turtle Mountain, the northern bay of Lake Souris found an outlet at the "elbow" of the modern Souris River; the elbow is about 18 miles (29 km) southwest of the present mouth of the Souris River.: 57 From this elbow, the lake's waters flowed southeast and entered the Pembina River, now a tributary of the Red River,: 57–58, 268 and the Pembina, in turn, entered Lake Agassiz at its Assiniboine embayment. When the ice sheet retreated north of the Assiniboine River, Lake Souris drained via that river into Lake Agassiz. (Pelican Lake in Langs Valley of Manitoba occupies what was once the northern shore of Lake Souris.)
The lower part of the Saskatchewan River basin near the river's mouth at Cedar Lake was clear of the ice-sheet before Lake Agassiz began to drain to northeast. Lake Saskatchewan existed on about 135 miles (217 km) of the North Saskatchewan River between Saskatoon and Prince Albert, Saskatchewan. A few miles east of Lake Saskatchewan's outlet, near the modern junction of the north and south branches, it entered Lake Agassiz. This Saskatchewan embayment extended for 400 miles (640 km) along the modern Saskatchewan River route.
Formation of beaches
Raised beaches, many kilometers from any water, mark the former boundaries of the lake. While the Red River gradually descends from south to north, these old strandlines ascend as one goes north, due to isostatic rebound since glaciation.
When Lake Agassiz outflowed to the south
The highest shore of Lake Agassiz is called the Herman Beach. It is named for Herman, Minnesota, in Grant County. The Herman Beach is the highest shoreline and can be traced from the historic outlet at Lake Traverse on the border of Minnesota and South Dakota. The beach fluctuates between 973 feet (297 m) and 976 feet (297 m) above sea level. The altitude of Lake Traverse at 971 feet (296 m) above sea level at the Traverse Gap at Brown's Valley is at 980 feet (300 m). This was the south outlet of Lake Agassiz.
The Herman Beach displays numerous deltas from the major rivers that entered Lake Agassiz. In Minnesota and North Dakota, these include the Buffalo River Delta, Sand Hill River Delta, Sheyenne River Delta, Elk Valley Delta, and the Pembina River Delta. In Manitoba, there is the Assiniboine River Delta.
- Beaches of the Norcross stages: The Norcross shoreline lies near the Herman shore on the slope of eroded till.
- Beaches of the Tintah stage: The Tintah beaches are 1,040 feet (320 m) to 1,055 feet (322 m) above sea level.
- Beaches of the Campbell stage: These have a well developed profile and are useful in establishing the boundary of the lake when it ceased to flow south into the River Warren.
- Beaches of the McCauleyville stage: The channel of the River Warren, flowing out of Lake Agassiz, eroded the channel below the level of Traverse Lake and Big Stone Lake, down to 935 feet (285 m), the deepest part of Lake Traverse. The southern portions of the McCauleyville shoreline coincides with the levels of high and low water in Lake Traverse, which are approximately 976 feet (297 m) to 970 feet (300 m) above sea level.
When Lake Agassiz outflowed to the northeast
Fourteen shorelines of Lake Agassiz have been identified, which lie below the McCauleyville beaches. These formed when the River Warren could no longer receive the outflow of the lake. This occurred when a lower outlet was found and the lake shrank with the release of the lakes waters. The three highest shorelines are named the Blanchard beaches, and the next five in descending order are the Hillsboro, the two Emerado, and the two Ojata beaches, from towns on or near their course in North Dakota.
- Beaches of the Blanchard Stage (Hillsboro Beach): Three successive levels of the lake pass near Blanchard, North Dakota. They are indicated by sand and gravel deposits 5 miles (8.0 km) to 7 miles (11 km) southeast of Euclid, Minnesota., and near Midway station, Manitoba The next lower beach is called the Hillsboro beach and is visible near Glyndon, Minnesota, and 5 miles (8.0 km) to 15 miles (24 km) north of Crookston, Minnesota.
- Beaches of the Emerado Stage: The Emerado shoreline, is approximately 885 feet (270 m) above sea level. Its southern tip is across the Red River between Kragnes, Minnesota, and Harwood, North Dakota. This single shoreline, clearly shows that it belongs to a period when the lake flowed northeastward to its outlet. Crustal rebound was greater to the north, where the Emerado beach, in Manitoba is 10 feet (3.0 m) to 20 feet (6.1 m) higher.
- Beaches of the Ojata stage: The upper Ojata shoreline is between 870 feet (270 m) to 875 feet (267 m) above sea level near Perley, Minnesota, and Noble, North Dakota. In Minnesota it is 2 miles (3.2 km) to 6 miles (9.7 km) east of the Red River. Some of the shore is marked by a beach ridge, especially to the north, where the surface is till.
- Gladstone beach: The southern tip of Lake Agassiz when Gladstone beach formed is near Belmont, North Dakota, 20 metres (0.020 km) south of Grand Forks it lies 845 feet (258 m) above sea level. It runs northward about 10 miles (16 km) east of the Red River.
- Burnside beach: The Burnside beach crosses the Red River at Grand Forks, North Dakota and to the northeast, then north, paralleling the Red River 10 metres (0.010 km) to 13 metres (0.013 km) to the east. This beach is indistinct south of the international border. The beach lies 835 feet (255 m) to 840 feet (260 m) above sea level.
- Ossowa beach: The Ossowa beach lies only a few miles south of the International boundary. The beach lies 815 feet (248 m) to 820 feet (250 m) above sea level.
- Stonewall beach: In Stonewall, Manitoba there is a conspicuous beach ridge 0.33 miles (0.53 km) or more. Its crest is 820 feet (250 m) to 825 feet (251 m) above sea level and about 10 feet (3.0 m) deep. Beach deposits belonging to this stage were not observed elsewhere in southern Manitoba. It is believed that they are buried for most of their length from the U.S. side of the border, north to Winnipeg
- Beaches of the Niverville stage: About 0.5 miles (0.8 km) southeast of Niverville the road crosses this beach. Its crest is 777 feet (237 m) to 778 feet (237 m) above sea level. It stands 4 feet (1.2 m) above the surrounding surface. Beginning near Niverville station, it extends southeasterly at least a mile. About 0.33 miles (0.53 km) south, a similar beach ridge crest is at 780 feet (240 m) above sea level. It rises 2 feet (0.61 m) to 4 feet (1.2 m) above the land. Much of it sloughs, with water throughout the year, the elevation of the beach crest is 782 feet (238 m) to 784 feet (239 m) above sea level.
- Examining the progression and termination of Lake Agassiz; Michael J. Michalek; April 23, 2013
- Perkins S (2002). "Once Upon a Lake". Science News. 162 (18): 283–284. doi:10.2307/4014064. JSTOR 4014064. Archived from the original on 28 February 2009. Retrieved 29 September 2012.
- Keating, William H. (1824). Narrative of an Expedition to the Source of St. Peter's River, Lake Winnepeek, Lake of the Woods, …. vol. 2. Philadelphia, Pennsylvania, U.S.A.: H.C. Cary & I. Lea. p. 7.
|volume=has extra text (help) From p. 7: "In some places pebbles were as abundant as if we had been travelling upon the bed of some former river or lake; the mind endeavours in vain to establish limits to the vast expanse of water which certainly at some former day overflowed the whole of that country."
- Upham, Warren (1880). The Geology of Central and Western Minnesota. A Preliminary Report. [From the General Report of Progress for the Year 1879.]. St. Paul, Minnesota, U.S.A.: The Pioneer Press Co. p. 18. From p. 18: "Because of its relation to the retreating continental ice-sheet it is proposed to call this Lake Agassiz, in memory of the first prominent advocate of the theory that the drift was produced by land-ice."
- The "retreat" of glacial margins is not caused by a reversal of the glacier's flow, but rather from melting of the ice sheet.
- Ojakangas RW, Matsch CL (1982). Minnesota's Geology. Minnesota: University of Minnesota Press. pp. 106–110. ISBN 978-0816609536.
- Fisher, Timothy G.; Smith, Derald G.; Andrews, John T. (2002). "Preboreal oscillation caused by a glacial Lake Agassiz flood" (PDF). Quaternary Science Reviews. 21 (2002): 873–78. Bibcode:2002QSRv...21..873F. doi:10.1016/S0277-3791(01)00148-2. Archived from the original (PDF) on 22 February 2014. Retrieved 7 April 2018., at page 874. This is the extreme figure of the ranges cited there.
- Fisher, Timothy G. (March 2003). "Chronology of glacial Lake Agassiz meltwater routed to the Gulf of Mexico" (PDF). Quaternary Research. 59 (2): 271–76. Bibcode:2003QuRes..59..271F. doi:10.1016/S0033-5894(03)00011-5. S2CID 130223046. Archived from the original (PDF) on 10 September 2008. Retrieved 14 May 2014.
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- Schiermeier, Quirin (31 March 2010). "River reveals chilling tracks of ancient flood". Nature. 464 (7289): 657. doi:10.1038/464657a. PMID 20360702.
- Brown, Michael (5 August 2021). "Massive ancient lake across Prairies emptied quickly enough to set off an ice age, study suggests". Folio. University of Alberta. Retrieved 3 September 2021.
- Lia, Yong-Xiang; Torbjörn E. Törnqvist; Johanna M. Nevitta; Barry Kohla (January 2012). "Synchronizing a sea-level jump, final Lake Agassiz drainage, and abrupt cooling 8200 years ago". Earth and Planetary Science Letters. 315–316: 41–50. Bibcode:2012E&PSL.315...41L. doi:10.1016/j.epsl.2011.05.034.
- Broecker, Wallace S. (26 May 2006). "Was the Younger Dryas Triggered by a Flood?". Science. 312 (5777): 1146–1148. doi:10.1126/science.1123253. PMID 16728622. S2CID 39544213.
- Fisher, Timothy G.; Smith, Derald G.; Andrews, John T. (2002). "Preboreal oscillation caused by a glacial Lake Agassiz flood" (PDF). Quaternary Science Reviews. 21 (2002): 873–78. Bibcode:2002QSRv...21..873F. doi:10.1016/S0277-3791(01)00148-2. Archived from the original (PDF) on 22 February 2014. Retrieved 28 September 2012.
- Dominique Forget (12 May 2008). "Polémique scientifique sur la disparition du lac Agassiz" (PDF). Journal L'UQAM. pp. 3–4.
- Turney CS, Brown H (2007). "Catastrophic early Holocene sea level rise, human migration and the Neolithic transition in Europe". Quaternary Science Reviews. 26 (17–18): 2036–2041. Bibcode:2007QSRv...26.2036T. doi:10.1016/j.quascirev.2007.07.003.
- Sansome, Constance Jefferson (1983). Minnesota Underfoot: A Field Guide to the State's Outstanding Geologic Features. Stillwater, MN: Voyageur Press. pp. 174–79. ISBN 978-0-89658-036-7.
- Spading, Kenton (23 August 2001). "Memorandum for Record: Interbasin Flow, Browns Valley Dike, Browns Valley, Minnesota, 2001 Flood and Historical Information" (PDF). Memorandum for Record. U.S. Army Corps of Engineers. Archived from the original (PDF) on 11 August 2011. Retrieved 15 May 2014. A sign at the dike however gives the elevation of the continental divide as 977 feet (297.8 m).
- The Glacial Lake Agassiz, Monographs of the United States Geological Survey, Volume XXV; Warren Upham; Government Printing Office, Washington; 1895; Chapter II
- (Thorleifson, 1996).
- (Upham, 1895), pp. 267; 270–272.
- The land around former Lake Souris inclines downhill along a northeast direction; thus, as the ice sheet retreated northwards, it exposed outlets of successively lower elevation. (Upham, 1895), pp. 270–272.
- (Upham, 1895), p. 268.
- (Upham, 1895), Plate IX (following p. 36).
- (Upham, 1895), pp. 271–272; see also Plate XXI (following p. 268).
- (Upham, 1895), see Plate XXI (following p. 268).
- The Glacial Lake Agassiz;, Monographs of the United States Geological Survey, Volume XXV; Warren Upham; Government Printing Office, Washington; 1895; Chapter VII
- The Glacial Lake Agassiz;, Monographs of the United States Geological Survey, Volume XXV; Warren Upham; Government Printing Office, Washington; 1895; Chapter VI
- The Glacial Lake Agassiz;, Monographs of the United States Geological Survey, Volume XXV; Warren Upham; Government Printing Office, Washington; 1895; Chapter VIII
- Sansome, Constance Jefferson (1983). Minnesota Underfoot: A Field Guide to the State's Outstanding Geologic Features. Stillwater, MN: Voyageur Press. pp. 174–181. ISBN 978-0-89658-036-7.
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- Thorleifson, L.H. (1996). "Review of Lake Agassiz History", Sedimentology, Geomorphology, and History of the Central Lake Agassiz Basin, Geological Association of Canada Field Trip Guidebook for GAC/MAC Joint Annual Meeting, pp. 55–84.
- Upham, Warren (1895). "The Glacial Lake Agassiz". Monographs of the United States Geological Survey. XXV. Retrieved 16 April 2009. Archived at: Wayback Machine
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- "Lake Agassiz Bathymetric Maps: Herman and Upper Campbell". Retrieved 2 November 2009.
- Thor K. Bergh, "Minnesota’s Sandy Soils", The Conservation Volunteer, Minnesota Department of Conservation. September October 1944. pp. 29–33.