GEOLOGICAL RELATIONS. 33 



long stretch of granite extending from the Bay of Chaleur to St. George, Me., if not 

 beneath the ocean to New Bedford, Mass. 



West of the granite there is a considerable quartzite, dipping south-easterly, and 

 then in the opposite direction, forming an anticlinal. Following it is an immense 

 Stretch of micaceous schists, showing at least two well marked axes, the first in Ken- 

 duskeag, the second in Charlestown. I have been informed that there are smaller 

 subordinate folds along this line not here represented. 



A broad band of clay slate succeeds the schists, and shows three axes, the first and 

 most marked being at the crossing of Piscataquis river. The rock is uniformly a clean, 

 soft clay slate, with very few dissimilar strata. A multitude of slate quarries are lo- 

 cated upon this band, furnishing the best quality of roofing shingles obtained in any 

 part of the country. There is a narrow band of a pretty conglomerate marking the 

 eastern edge of this formation. The last axis in the slate is on the south-west side of 

 Moosehead lake, near Greenville. Following the lake border, we find a considerable 

 mass of sienite. Squam mountain is mainly composed of slates, with corals on its 

 southern slope, as reported by J. T. Hodge. As far as to the hill opposite Mt. Kineo, 

 the rocks appear to be slaty, and the whole series is probably Silurian, and of more 

 modern date than the clay slates recently passed over. But scarcely anything is known 

 of them. Mt. Kineo is composed of a compact felsite or siliceous slate, whose struc- 

 ture it is not easy to determine. Viewed from the east it presents some resemblance 

 to a crushed anticlinal, and, as this structure is in accordance with the best suggestions 

 possible as to its age, we may accept it for the present as correct. The formation may 

 be Huronian, lying beneath the fossiliferous members on both sides of it. 



The rocks on Moosehead lake, beyond the felsite, are better understood, as they 

 contain, first, the peculiar fucoid of the Cauda-galli grit, and then marine forms charac- 

 teristic of the Oriskany sandstone. Our observations would give an anticlinal struc- 

 ture to this formation, which differs from that ascertained to characterize the same 

 band at Parlin pond. The occurrence of this well-established fossiliferous horizon in 

 the midst of the crystalline schists is of great importance, since it enables us to say 

 decidedly that the two classes of rocks are not interstratified with each other, and that 

 therefore the latter are older than Paleozoic* Beyond the lake, on the west branch of 

 the Penobscot, the rock verges into a slate, whose cleavage planes may obscure the 

 stratification. While these dip at an angle of 6o°-7o° north-westerly, it is very likely 

 the strata dip only io° or 12° in the same direction. It is not impossible that these 

 slates represent a different formation, the same which occurs farther on. First, how- 

 ever, our line passes over a few miles' width of the Huronian mica schists, with three 

 or more axes. The slates display, as a whole, the synclinal form, with a small anti- 

 clinal in the centre, at Lead-better falls. Other minor or local foldings were observed 

 in them. The formation may correspond with the Upper Silurian slates or Gaspe series 

 of Ouebec, as well as with the same range at the Moose River settlement on the Canada 



See paper on geology of the north-west part of Maine. Proc. Amcr. Ass. Adv. Set., 1873, p. 163. 

 VOL. II. 5 



