100 GLACIAL GEAYELS OF MAINE. 



ice might for a time continue to flow across the valley until checked by the 

 hills of Springfield and Lee, and the remarkable mounds of till may par- 

 take of the nature of a terminal moraine. The mound of glacial gravel 

 lying near the osar-plain may date from this period. I could find no 

 signs of a glacial stream, a lateral tributary of the main river, reaching 

 farther north than this mound. The very large size of the bowlders of the 

 mound indicates that it was formed subglacially and makes it probable that 

 the deposit is partly or wholly a water-washed terminal moraine. The 

 region deserves more careful study than I have been able to give it. 

 Apparently the upper ice-bearing granite bowlders from the north contin- 

 ued to flow over the lower ice after the latter was partially embayed. The 

 osar-plain soon crosses a low divide at an elevation near 200 feet above 

 Kingman, and then follows the valley of the Passadumkeag River to Nick- 

 atoiTS Stream, where it tmnis from its southwestward course to south. It 

 here takes the form of a two-sided ridge 80 feet high (at an elevation above 

 the sea of 380 feet, as determmed by spirit level by D. F. Maxwell, C. E.), 

 and continues as a prominent ridge for several miles southward. It then 

 turns more nearly southeastward and follows the Narraguagus Valley for 

 many miles, most of the way lying one-fom-th of a mile or more to the 

 west of the river. Part of the way it takes the form of a single two-sided 

 ridge; at other places it is an osar-plain one-eighth of a mile or more in 

 breadth, and occasionally it expands into narrow plains of reticulated ridges. 

 North of Lead Mountain, in Beddingtou, an osar-ridge composed almost 

 wholly of bowlderets and bowlders is found oh the eastern border of the 

 gravel, while to the west extends a plain of sand and gravel 1 to 3 miles 

 wide. The western portion of these plains shows some low sand dunes. 

 But for the wind, the plains would probably now be quite level on top. The 

 material plainly becomes finer as we go westward. The plain was a delta 

 deposited in a glacial lake or in the sea. Its elevation, by aneroid, is more 

 than 300 feet above sea level. 



Just south of Lead Mountain there is another gravel plain of rounded 

 shape, about three-fourths of a mile in diameter. It ends in a steep bank 

 do%vnward both on the west and south, beyond which is till, not a plain of 

 •clay. It is gently rolling on the top, yet shows finer sediments on the west 

 and south, and must have been deposited in an open body of water. The 



