396 GLACIAL FORMATIONS OF ERIE AND OHIO BASINS. 



advantage along the direct road from Newark to Wilkins Run, and tlience to 

 St. Louisville, and in the district southeast along the road from Newark 

 to Linnville, and thence west along the National road to the valley of South 

 Fork. There is a lowland tract, lying northeast of Newark, with a general 

 elevation about 100 feet above the Licking River, which Wright refers to 

 in his paper on the glacial boundary (p. 53) as a terrace. It is, however, 

 dotted by drift knolls 10 to 20 feet in height, among which shallow basins 

 are inclosed, the whole aspect being morainic. In structure also it resembles 

 a moraine rather than a river terrace, since it contains mucli till and its 

 assorted material is frequently disposed in arching or inclined attitudes. On 

 the north side of the Licking Valley, just east of Newark, is a less elevated 

 lowland than that just described, standing about 40 feet above the river. 

 It has slight surface inequalities, but they are perhaps attributable to fluvial 

 action, and being made up almost entirely of gravel, the name terrace is 

 probably applicable. There are also in this portion of the valley two smooth- 

 surfaced gravel terraces, standing about 30 feet and 20 feet above the river, 

 the lower one constituting the plain upon which the business portion of 

 Newark is built. On each of the several forks of the Licking, which unite 

 at Newark, terraces occur at heights of 40 feet or less above the streams. 

 On the South Fork the head of the upper terrace is about 3 miles south- 

 west of Newark, where the valley is crossed in a north-iaorthwest to south- 

 southeast course by a moraine. On the Middle and North forks the terraces 

 are well displayed for a few miles above Newark, but were not traced to 

 their heads. A low gravel plain several miles in extent lies in the angle 

 between the tlu'ee forks of Licking River west of Newark, and carries occa- 

 sional low di'ift knolls. These knolls were apparently formed at the time 

 the gravel plain was being built up, and are thought to indicate that the 

 head of the gravel plain was built up as a submarginal deposit to about its 

 present height before tlie ice sheet had withdi'awn from over it. 



The morainic system is, on the whole, stronger northward than it is 

 southward from Newark. Not onl}'- are the belts broader, but the knolls 

 and ridges are sharper. South from the latitude of Newark the western or 

 main member is only 3 to 5 miles in width, and with the excejjtion of an 

 occasional large gravelly knoll, the height of its swells and ridges falls below 

 25 feet. They are, howevei-, closely aggregated, rendering the belt readilj^ 

 distinguishable from bordering plains. The eastern portion of the morainic 



