Age of Licking N arroius 
183 
carved by the glacial waters. (Channels N and P, fig. i.) Chan- 
nel N presents a profile as shown in the diagram, fig. 4. Its 
floor is continuous with the terrace on the adjacent valley slope 
and is covered with a thin deposit of sand and gravels, much water- 
I' worn, and underlain by the rock in place. That the tributary in 
valley C flowed through this channel at the time of the formation 
of the persistent terrace is quite evident. Since Pleistocene times 
it has reverted to its pre-glacial channel where it now flows on 
gravels ten feet below the level of the bed-rock in the old channel. 
Channel P, across the Licking, shows similar structure and 
history; the origin of the two channels must have been the same. 
The only explanation that satisfactorily accounts for the carving 
out of these channels on the slopes of hills is that the ice-front 
abutted against them and served as one of the valley walls until 
the stream was well established in its new course. 
The frontal limit of the ice sheet is, then, definitely located in 
these four places by the channels which resulted from its position. 
It is necessary, therefore, for us to postulate a valley dependency 
similar to, though smaller than, the one in the old Newark valley^ 
extending, as shown in fig. i, down the Licking valley until it 
was stopped by the steep slopes at the points M, JSf andP. Glacial 
bowlders have been found near the top of the hill just south of 
Claylick; this fact, combined with the small amount of cutting 
necessary to carve the bench at P, leads one to suppose that the 
I latter was covered by the advance of the ice and was formed dur- 
I ing a retreatal pause of the ice-front. 
The capture of the Licking. The hypothesis has been published 
that after the retreat of the ice the Licking Basin was closed and 
! as the waters rose in Lake Licking they reached a low col in the 
j divide a little south of Hanover. The position of this col is rep- 
resented by the present Licking “Narrows.^’ ^ If this were the case 
I terraces would be found in all four tributary vallevs at the same 
i elevation, for they would all be parts of the same lake. As stated 
I above there is a marked discrepancy between the elevations of 
those in valleys B and C, while no terrace, or signs of a glacial 
I lake, is found in valley D. The phenomena of the region do not, 
f therefore, coincide with this hypothesis. 
I 
* Carney: loc. cit.^ p. 149. 
' Tight : loc. cit.y p. 49. 
