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Scattered glacial erratics in northeastern Kentucky and southern Ohio [5] are pre-Kansan in age. Only the Nebraskan is recognized as earlier than Kansan; these have been designated as remnants of deposits left by the Nebraskan glacier. [6] The ice sheet overrode the preglacial Teays creating ponds or glacial lakes.
Glaciation changed the course of the Ohio River, in the vicinity of Louisville and Cincinnati where glacial melt waters filled the valley with sand and gravel. Lake bottom sediments deposited locally where the Kentucky, Green, Licking and Salt rivers were temporarily impounded by glacial debris. [2]
The unglaciated plateau extends southwestward into eastern Kentucky and Tennessee, where it is called the Cumberland Plateau. Canisteo River Valley from Pinnacle State Park . Glaciation in this area of the plateau removed the sharp relief that is seen in unglaciated areas of the plateau.
The river's path traveled through modern-day West Virginia, Kentucky, Ohio, Indiana, and Illinois, finally emptying into the Gulf of Mexico, which at the time extended to southern Illinois. The glaciers of the Ice Age soon began to block the Teays, effectively damming the river and forming Lake Tight, near what is now Chillicothe, Ohio.
The Allegheny Plateau (/ ˌ æ l ɪ ˈ ɡ eɪ n i / AL-ig-AY-nee) is a large dissected plateau area of the Appalachian Mountains in western and central New York, northern and western Pennsylvania, northern and western West Virginia, and eastern Ohio. It is divided into the unglaciated Allegheny Plateau and the glaciated Allegheny Plateau.
Since glacial till is highly fertile soil, agriculture on the glacial till plains is very productive. The region has gently rolling moraine hills left over from the retreating glaciers, as well as small sandy ridges , which were formed as coastal dunes during periods in which Lake Erie was higher than it is today (14,000-12,000 years ago).
[1] Marine (1997) found five terrace levels along the rivers, but he had to conclude that the lake deposits found on them resulted from only two episodes of glacial damming. Deposits on the fifth and fourth terrace levels represent damming during a pre-Illinoian glaciation, whereas the third- and second-terrace-level deposits represent damming ...
In northern Ohio, the thickness of the Bedford is irregular due to erosion prior to the deposit of the Berea Sandstone, and due to recent glacial and stream erosion. The Bedford thins toward the south; near Columbus in central Ohio it is 95 feet (29 m) thick, and 85 feet (26 m) near Chillicothe 45 miles (72 km) to the south. [28]