MERWIN: SHORE-LINES. oar 
—.— The Side Valleys. Fifteen miles east of Lake Champlain 
Brown’s River enters the Lamoille River from the south. In the east- 
ern junction angle between the streams, sand terraces reach an altitude 
of about 540 feet. Terraces are absent from the north side of the 
Lamoille River in this vicinity on account of the presence of ice there 
during the building of the terraces on the south side. Brown’s River 
had no part in this terrace building for it drains an unfilled basin of 
which the terrace deposits are the northern rim. The Brown’s River 
valley, during the Wood Creek stage of Lake Vermont, was submerged 
by an arm of the lake at least 100 feet. Into the north end of the 
valley at this time sediments collected from the ice and from the 
Lamoille River; into the south end the Winooski delta encroached; 
into the middle, only a little sediment from small side streams, and 
clay from the ice, found their way. Corresponding to this level of 
Lake Vermont, beaches were formed northeast of the northward 
bend of the river at an elevation of 510 feet, and 3 miles north 
on the east side of the valley, wave-washed slopes at about 515 feet. 
= When Lake Vermont began falling from its Wood Creek stage the 
Lamoille River still drained through the lake in the Brown’s River 
valley. Its old channel across the Winooski delta is at an altitude of 
490 feet. Very soon, however, the ice in the lower Lamoille valley 
gave way, allowing the Lamoille River to occupy its preglacial channel. 
‘The lake in the Brown’s River valley then began draining into the 
Lamoille River. 
From near Jeffersonville a longitudinal valley extends northward, 
joining the Lamoille valley and the Missisquoi valley. The swampy 
divide on the floor of the longitudinal valley attains an altitude of 
about 450 feet. South of the divide kames and outwash gravels rise 
to an elevation of 550 feet. Southwest of the divide laminated clays 
occur 30 feet above the divide. The clays are overlain by gravels 
which form an ice-block basin south of the cross-road leading to 
North Cambridge. Here the clays dip south. These relations are 
explainable on the hypothesis that the clays were laid down in a lake 
standing at an elevation of 580 feet or more, and that an advance of 
the ice over them left a stranded ice-block. 
Tue Missisquor Basin.— The Side Valleys. The northern part of 
the longitudinal valley just described, also contains glacial outwash 
gravel. At Sheldon the gravels attain a height of 450 feet above the 
sea, and at the divide between Sheldon Springs and Green’s Corners, 
a height of 460 feet. The latter deposit is irregularly cross-bedded 
and contains scattered boulders reaching four feet in diameter. 
