382 GLACIAL GRAVELS OF MAINE. 



ends of bays or fiords considerably north of tlie general coast line. Thus 

 two systems end in Belfast Bay and one in the north end of Penobscot 

 Bay. The Clinton S3^stem ends very near the fiord known as Sheepscot 

 Eiver, and another comes almost to Cobscook Bay, in Pembroke, and 

 another near the sea at Waldoboro. Since the deposits become smaller 

 toward the south, it is possible that some of the systems really extend 

 farther than they seem, the small deposits of gravel which form their 

 southern ends being covered by the marine clays. But in many cases this 

 can not be admitted. Thus three systems seem to end near .the Head of 

 the Tide, Belfast. One of them, if extended, would be found beneath Bel- 

 fast Bay, but the two more westerly systems would cross the city of Belfast, 

 where excavations for wells, foundations, etc., are so numerous that the 

 gravels would certainly have been discovered. In these cases and in most 

 of the gravel systems the evidence that they really end before reaching the 

 sea is satisfactory. Another exception is found on the coast from Scarboro 

 for many miles southward. The shore is formed of marine-delta sand. It 

 is difficult to estimate how far the delta originally extended out into the 

 region at present covered by the ocean. In Jonesport a plain of glacial 

 sand reaches nearly to tide water. With the exceptions named the gravel 

 systems all end north of the present shore, and in most cases only 10 to 50 

 feet above sea level. 



LENTICULAR SHAPE OF THE COASTAL GRAVEL MASSES. 



At Winslows Mills a round-topped hummock of glacial gravel lies 

 directly beneath the more northern ridge of the Waldoboro moraine. It 

 was exposed by excavations made during the building of the dam and mills. 

 At the time of my visit the gravel had fallen into the excavation so as to 

 make it impossible to determine what was the original nature of the stratifi- 

 cation. Enough could be seen of the general shape of the mass of gravel 

 and cobbles to show that it does not materially differ in external form from 

 the other hillocks of the system of glacial gravel of which this forms a part. 

 This is a discontinuous system which extends from near the sea at Waldo- 

 boro northward along the valley of the Medomac to a point somewhat more 

 than a mile north of the moraine at Winslows. The moraine lies directly 

 on the gravel dome, without transition beds. I could discover no sign that 

 the glacial stream which deposited the gravel was flowing at the time the 



