Per,son(il (inti tScieiih'JJc jretn<. 199 
tlie coast uf Liihrailur is oliiiiaclerizt'd by llit- uracet'Lil tlowiiij:' contour 
whicli is produci'd bv the horizontal I'l-osioii of ice rallier tliaii of suli- 
aerial agtMicii'S. Tliis is in slrii<in;i' contrast to the- border of western 
Greenland, sviiicli was seen by Prof. Wri*riit last summer, in llie ('ook 
Arctic Expedition, for a distance of i!U,(i miles. In both cases t lie rocks 
ure Laurentian iiiieiss, which would weather into the same shapes if 
subjected to the same conditions. The mountainous border of western 
Greenland has never been entirely covered by jzlacial ice. but has been 
subjected for an indefinite time to subaerial erosion, producing the 
innumerable sharp needle-like peaks. The e\idences, however, of a 
former great extension of the inland ice-sheet of Greenland are every- 
where visible: but these peaks (from 2,000 to 4,000 feet in higlU) wer<- 
Always nunataks, and the ice probably never reached as far out inl.> 
Davis strait as it did from Labrador toward the .southeast. 
A striking fact, noted in both eoutliern Greenland and Labrador, is 
the small amount of glacial drift still remaining on the land now free 
from ice. There is scarcely any till in either region, and even boulders 
are few as compared with tracts near the border of the glacial drift 
in the central i)arts of the United States. The explanation is, doubt- 
less, that the present (ireenland and Labrador coasts were so far within 
the areas of Pleistocene ghiciation that the loose material was nearly 
all remoNed and depositeil in the sea. 
Professor AVright spent scmie lime on a projection of the inland ice. 
three miles wide, which comes down into Ikamiut fjord about fifteen 
miles from the open sea, near Sukkertoppen, in latitude 05° 50'. The 
ice there scarcely differs from that of the Muir glacier in Alaska. It 
has vast moraines on its surface, but little or no englacial material. 
The scratches on the marginsof this ijovcl present instructive complica- 
tions. Wh>'n the ici- tilled the fjord to the higlit of about 2.000 feet, 
the scratches Avere in the direction of its axis: but, now that it lias 
retreated, local glaciers are j)rodMcing stria' at right angles to these, 
and in some cases even in an ojjposite direction. (This paper is pub- 
lished in the American Journal of Science for February, 1895.) 
Jligldand Level Oraveh in northern JVeir England. }\y C. H. Hitch- 
cock. At the .south end of lake Mem]^hremagog terraces of sand and 
gravel, regarded as deltas of a glacial lake held by the barrier of the 
departing ice-sheet, occur at liights of 575 feet and especially at 250 to 
275 feet above the lake, wliich is (305 feet above the sea. These terraces 
are best developed near the mouths of Barton and Black rivers, and 
they extend nearly horizontal up the valleys of these streams,which flow 
into the lake from the south. Other terraces, having bights of LlOO 
feet or more above the sea. are known north of lake Memphremagog: 
and they occur at similar altitudes in northern Maine. Their greatest 
hight is in the White mt)untains of New Hampshire, where, near the 
Twin Mountain House, a very remarkable delta-like deposit of sand and 
gravel is found \,r>(K) feet above the sea level. 
Referring to the opinion of Chalmers and others of the Canadian (ie- 
ological Survey, that the glaciation of New England and New Bruns- 
wick may have radiated outward in all directions from their mountain- 
ous central region. Prof. Hitchcock thought this ^ iew disproved by the 
transportation of Ixiulders from the north side of the St. Lawrence to its 
southern watershed in ^Liine, and by the southeastward glacial stria* 
and drift transportation on Mt. Katahdin and Mt. AVashington. During 
the closing stage of the tilacial period, however, local glaciers or rem- 
nants of the continental ice-sheet flowed outward perhaps from all sides 
of the mountain region, and some of the valley moraines have been ob- 
served by Agassiz, Stone, and the author. This Late Glacial stage 
probably comprised the northward movement of boulders noted in som,. 
parts of noi't lu-rn New Eni:lan<l and theejistern iiro\inces of Canada. 
