198 The American Geoloytst. March, 1895 
frontal glacier cliifs, and cvi-ii Iln'Sf> snow drifts are sutticienl in some 
places to cause the ice to How upward or to be laterally deflected. 
Til some cases the morainic hillocks, seen in process of formation 
beneath the steej) or vertical edge of the ice, have the outlines of min- 
iature drumlius, with the laminated glacier curving ujiward (luite con- 
formably over them. Xo eskers or kames were observed. The drain 
age from the glacial melting is mostly by subaerial lateral streams, 
along the inner side of the adjoiiiini.'' moraines: rarely it is by central 
subglacial streams. 
Only very scanty drift is spread over the country outside the ice- 
sheet and glaciers; and the largest glacio-tluvial delta fans are about a 
half mile in extent. Most of the glaciers havf been long stationary: a 
few are retreating: others are ad\ancing. 
Near the east side of J5owdoin bay a driftless area, having a diam- 
eter t)f three or four miles, shows deep decomposition of its rock, 
which is hornblendic gneiss. Its altitude is less than that of neigh- 
boring glaciers, and it is accepted, with the jagged and unglaciated 
outlines of the ui)per part of many of the coastal mountains from 
capes Farewell and Desolation north to Inglefield gulf (a distance of 
1,200 miles), as decisive evidence that there has never been a complete 
envelopment of the western border of (Jreenland by land ice. 
Dalrymi)le island, close to the Greenland coast, near long. 70° and 
lat. 7(V°30'. al.so consists of decomposing hornblendic gneiss, with no 
drift, and with mountain forms due solely to subaerial erosion. Fifty 
miles north wesi want, however, the ('arey islands, which are moun- 
tains rising from a large expanse of the surrounding northern part 
of BafHn bay, have been glaciated by an ice-sheet flowing over them 
from the north, that is, from Grinnell land and Smith sound. In the 
course of this ice-sheet, at a distance of fifty miles north of the Carey 
islands, the sea has a dei)th of 220 fathoms. 
Inquiring for the physical causes and exi)lanation of glacial motion. 
Prof. Chamberlin thinks the theory of Ilugi. (Jrad, Forel, and others, 
which refers the movement, under the influences of the solar heat 
and gravity, to the enl.argement and long persistence of the granules 
originating in the neve, to be more supported by his observations and 
studies than the now commonly accepted theory of J. L). Forbes, 
which regards the ice as a viscou.sly flowing, though brittle, solid. 
(These Greenland glacial studies, upon a wider range than could be 
noted in this address, are being i)resented very fully by Prof. Gham- 
berlin in a series (jf articles in the Journal of Geology, from the num- 
ber for Oct. -Nov.. 181)4. onward.) 
Nine other papers related to the Ice age and Pleistocene 
history, of which abstracts, witli notes of their disctission. fol- 
low : 
Obfierrafioiix ai) tin- (rhicidl i>hcn(>ini'nii of NcirfoiUKlhtiid, LubrtiOnf. mul 
southern (irecnhind. Hy (J. Fukdkhick Whioht. From glacial drift de- 
posits and strije it seems conclusive that the ice-sheet of Tjabrador ex- 
tended out ui)on the submerged plateau surrounding Newfoundlaiui so 
as completely to envelo|) the island; but probably the whole region was 
then elevated above its present level about 2.000 feet, in which case the 
ice-sheet also may have likewise enveloped the very large area of the 
now submerged Grand Hank, yet without then reaching to the sea level. 
The evidences for these conclusions are (1) that glacial scratches are 
found on the summits of all the. headlands oT Newfoundland \\\) to r).")0 
feet, pointing out to the open sea: (2) that the basins of some of the 
inland lakes of the island descend nearly 1,000 feet below the li-vel of 
the sea: and (:5) that the submerged plateau of the Fishing Hanks is 
intersected by a deep channel extending across the Gulf of St. T^aw- 
rence to the edge of the abvssal water of the Atlantic. Furthermore, 
