18 The Americ((n Geologist. January, 1895 
This is twelve miles farther than the terrace on the south side 
of the river, which does not reach the Winnebago county line. 
This north side terrace in Winnebago county is a well-marked 
bench, 50 to 60 feet above the river, which has cut into it but 
hardly removed much of its bulk. Directly opposite, on the 
south side of the valley, instead of a similar terrace of 60 
feet thickness of loess, we find no loess whatever; onlj'' the 
sloping rock surface overlaid with thin drift of the newer 
sheet. It is hence evident that the loess on the north side 
was deposited before the drift sheet was formed on the south 
side of the valley, else this side would have received a heavy 
deposit of loess also. Having found that the epoch of loess 
deposition was not subsequent to that of the newer drift 
sheet, we will next look into the probability of its having pre- 
ceded it. The newer drift in this vicinity (we use the term 
■"newer drift" to distinguish this sheet from the very much 
older one to the west, and not as designating the latest formed 
drift sheet in America) was formed by a long and compara- 
tively narrow lobe of the ice which projected toward the west 
from the general front of the glacier. There is a ridged ac- 
cumulation of drift about its border, which is further distin- 
guished by a boulder belt. But the amount of material in 
this ridge, especiall}^ about its western end, is remarkably 
small, in comparison with the length of time it was occupied 
by the edge of the ice as indicated by other phenomena. Had 
a deposit of loess been found by the ice on the south side of 
the valley as great as now exists on the north side, and had 
it plowed up and entirely removed this loess as it must have 
done to produce the present configuration, the morainic ridge 
at its border, and especially at its westward end, should now 
be ten times as large as it really is. We naturally conclude 
that there never was any deposit of loess on the south side of 
the valley, and that the Valley loess and newer drift sheet in 
this vicinity were formed contemporaneously. This conclu- 
sion is further supported by internal discordance in the strat- 
ification of the loess of the terrace as though it were subject 
at times to external pressure from the direction of the ice. 
Moreover, while the main body of the ice lobe lay on the un- 
dulating country to the south of the river valley and the north 
edge of the ice rested in the valle}^ leaving a space between 
