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F7-ank Carney 
place. The variation of valleys from transverse or from longi- 
tudinal positions is attended by a corresponding variation in 
erosion. The Moravia quadrangle has several valleys maintain- 
ing various attitudes between the transverse and longitudinal 
positions. Remembering that the ice in this area did not have a 
meridional motion, we understand the unequal erosive effects 
in these valleys. For example, a valley extending southeastward 
from Freeville bears quite a transverse relationship to ice-motion, 
whereas certain segments of the more longitudinal valleys (fig. 4) 
are quite in line with the deployment of the moving ice. The 
valleys that approach a transverse position suffer modification 
largely through partial burial. This is particularly the case when 
they happen to coincide with ice halts. 
The development offextended and fairly steep valley Walls is not 
normal to regions having slight vertical variation in stratigraphy. 
The development of drainage lines, and the resulting disintegra- 
tion of terranes, produce side walls more or less irregular in 
reference to the axis of the valley. In a longitudinal view this 
condition gives the effect of over-lapping spurs. 
From Locke northward the Owasco inlet, as already stated, 
especially on its western side has an oversteepened valley slope 
such as would not normally be developed in the stratigraphy. 
On the eastern side from Moravia northward the same condition 
exists; the exact nature of the valley wall on this side, southward 
from Moravia, is partially masked by drift accumulations. But 
this segment of the Freeville-Moravia valley does not have over- 
lapping spurs, a consequence of the active ice-erosion in this 
longitudinal valley. There is conclusive evidence that the north- 
ern half of the Freeville-Moravia valley is genetically due to the 
same direction of stream flow that the valley now has. This being 
the case the rock floor had a general northward gradient, and 
accordingly offered the moving ice the condition of obstruction 
conducive to a great amount of erosion. 
The same principles of ice-erosion in longitudinal valleys is 
illustrated by the steep rock slope extending from Morse Mill 
southeastward to the vicinity of Lake Como. Again, in the valley 
of Skaneateles inlet We have these oversteepened slopes on both 
sides, so far as this sheet is concerned (fig. 5), due to ice erosion. 
When glacial-deposition does not later take place in localities 
of active glacial-denudation we find barren farms as on the steep 
