of this moraine from Cape Cod to the Canadian boundary in Da¬ 
kota, and Dr. Dawson has identified it for 400 miles beyond. This 
later moraine crosses the Northern States of the Union in twelve 
great loops, each of which embraces a distinct valley ; and these 
loops are believed to have been formed by lobes of ice advancing 
through the valleys from the front of the ice sheet. 
In the West the limit of glaciation extends for hundreds of 
miles beyond this moraine; but in the East the Champlain-Hud- 
son River lobe is believed to have formed the Cape Cod-Long 
Island moraine. In other words, while in the West the glacier 
of the second epoch was not so extensive as that of the first epoch, 
at the East its frontal edge reached the same or possibly a lower 
latitude. The second moraine is much more massive than the 
first, and the country back of it gives evidence of much more 
thorough glaciation than does that lying between this moraine 
and the limit of drift. 
At the time that the moraine was being formed on Long Island, 
New England was completely buried under an ice blanket which 
must have been fully a mile thick in Northern New Hampshire. 
So far as recorded the summits of all the New England moun¬ 
tains are glaciated. And it is readily seen that this would neces¬ 
sarily have been the case if the upper surface of the ice was (as 
it is supposed to have been) a plane with a gradually upward 
slope from the sea at Cape Cod to a point somewhere above the 
summit of Mount Washington. 
The Adirondacks, like the White Mountains, were completely 
covered with ice ; but the summits of the Catskills above about 
the 3000-foot contour are not glaciated. Some points in the New 
Jersey highlands a short distance north of the moraine rose, also, 
above the ice. These data, together with the position of the 
terminal moraine at tide water at Perth Amboy, have furnished 
Prof. Smock with the means of estimating the grade of the gla¬ 
cier’s surface. Between New Jersey and the Catskills the aver¬ 
age upward rise was thirty feet per mile. These figures, though 
indicating a grade very much less than that of any alpine glacier, 
accord well, not only with Geikie’s estimate of the grade of the 
surface of the Scotland glacier, but also with Nordenskiold’s fig¬ 
ures of the rise of the surface of the ice towards the interior of 
Greenland. 
