Раннее озеро Эри: История формирования и эволюции в плейстоцене и голоцене.

Early Lake Erie was a prehistoric proglacial lake that existed at the end of the last ice age approximately 13,000 years ago. The early Erie fed waters to Glacial Lake Iroquois. The ancient lake was similar in size to the current lake during glacial retreat, but for some period the eastern half of the lake was covered with ice. Early period Lake Erie was made up of smaller lakes (Lakes Warren, Wayne, Maumee and Lundy) with lower depths. Much of the ancient lake bed is now northern Ohio.

12,000 years before present (YBP) the Laurentian ice sheet had melted to the east, creating an outlet for the Lake Erie basin at the Niagara Escarpment. Simultaneously, the ice sheet had opened a drainage between Lake Algonquin and Lake Ontario through the Kirkfield Outlet. This ended the outflow from Lake Algonquin into the Lake Erie Basin. Holocene history of Lake Erie began with a flood of water over the Niagara Escarpment. The flood created a channel in the moraines and bedrock lower water level in the Erie basin. The Niagara River Outlet, was over lower than the present level of Lake Erie creating a non glacial lake, called Early Lake Erie. At this stage water elevation was above sea level. The lake consisted of two lobes, one in the eastern basin and a smaller lake in the central basin.

About 10,400 YBP the ice sheet advanced southward, blocking the Kirkfield Outlet. Once again, the Lake Erie basin received water from Lake Algonquin, through the Port Huron Outlet and the new St. Clair River Lake St. Clair Detroit River system. The additional water created a marshy swamp in the western basin, then it created a river system through the Pelee Passage. The shallow central basin overflowed the Norfolk Moraine creating the Pennsylvania Channel into the eastern basin. The deeper eastern basin overflowed Niagara Escarpment by the Niagara River for a brief time. There is still a division of ideas about whether Early Lake Erie overflowed the Niagara River at this time or remained without an overflow.

By 10,300 YBP the North Bay Outlet opened between Lake Algonquin and the St. Lawrence River. The level of Lake Algonquin dropped, ending the outflow through the Port Huron outlet. For several thousand years Early Lake Erie did not receive water from the upper basins. This low water stage lasted for 5,000 years. The lake lost over 90 percent of its inflow, becoming stagnant. The lake became eutrophic, acerbated by lower precipitation and increased evaporation. A closed or endorheic lake basin was created Bathymetric data compiled by National Geographic Data Center in 1998 located a former shoreline submerged below Lake Erie. The Buffalo Ridge shoreline in the eastern basin is below the current river outlet. It is believed that decreased precipitation and increased evaporation of set the changes created by the isostatic uplift.) This Xerothermic or Hypsithermal Interval existed for approximately 5,000 years (10,300 to 5,300 YBP). The increase in water, the growing humidity in the climate, and increased water levels created a large delta in western basin at the mouth of the ancestral Detroit River. The remaining depositional features in Lake Erie (i. e. the Buffalo Ridge, Norfolk Moraine, Conneaut Bank, and Presque Isle Bank) were flooded. These underwater obstacles altered water circulation patterns,

Shoreline features indicate Lake Erie rose to a highstand, above its present level about 4,700 YPB. The Niagara River Outlet eroded to its current level about 3,500 YBP. These drowned shores became the source of beach sand, forming the massive sand spits at Long Point and Presque Isle, and creating new spits at Point Pelee, Ontario, and Cedar Point, Ohio. At the same time barrier beaches were formed across the mouths of most of the estuarine tributaries.