362 APPENDIX TO PARTS I AND II. 



Kennebago lake. Very few ledges are seen. The boulders, however, are large and 

 numerous. But what is most important, it is undoubtedly the rock the metamor- 

 phisJii of which has produced the serpentine, which is also abundant here. The boul- 

 ders of serpentine are first found in great numbers about ten miles north of Kennebago 

 lake. They are enormous in size, sometimes 30 or 40 feet in length ; and with these 

 are boulders of diorite of nearly the same dimensions ; but where the ledges appear, 

 the diorite evidently passes into serpentine. 



Aj-gillitic Mica Schist with Statu'olite. West of the gneiss containing limestone, in 

 Phillips, we have a mica schist which, westward in Madrid, becomes quite argillaceous, 

 and then again, in the south-west corner of Madrid and in Sandy River Plantation, 

 and west as far as Rangeley lake, this rock has more the characteristics of a typical 

 mica schist. The strata are everywhere vertical, or nearly so ; and often there are 

 beautiful crystals of staurolite. One of the finest outcrops with these crystals is at a 

 school-house north of Sandy river, three and a half miles west of Madrid village. In the 

 river, below the dam at Madrid village, there is a fine-grained, thickly-bedded mica 

 schist, which contains concretionary nodules of granite from three inches to a foot in 

 length, and from two to eight inches in width. In the larger ones the proportional 

 width is much less than in the smaller ones. Five rods below the dam, the fissile ad- 

 dalusite schist has essentially the same strike and dip as the compact mica schist above. 

 North-west of Madrid village there is a large area of ferruginous schists that probably 

 belong to a different series of rocks from those we are considering. In the west part 

 of Sandy River Plantation, and in the east part of Rangeley, we have mica schist with 

 staurolite. This schist is extensively developed on Saddle-back stream, which flows 

 near the Greenvale house. Following up this stream, we find, for nearly half a mile, 

 both the schist and the conglomerate ; and there is such an intermingling of the two, 

 that, unless there have been great changes in the rocks since they were uplifted to 

 their present position, they must belong to the same series of rocks. When the stream 

 turns and comes more from the east, we leave the conglomerate. Above, a deep gorge 

 has been cut in the schist along the strike. On the hill south-east of the Greenvale 

 house, where the steep ascent begins, there is a mica schist with staurolite, and the dip 

 is S. 20° E. 82°. There is a conglomerate included in this, and unconformable with 

 it. On the face of the cliff it was not more than 120 feet in width, but it becomes wider 

 as we ascend the hill. It dips N. 30° W. 75°, and stands on the upturned edges of the 

 staurolite schist: so it is clear that we have two bands of conglomerate. Just south of 

 the inlet of the lake, the schist and conglomerate have the same relations that they do 

 on Saddle-back stream. This schist is more extensively developed in this section of 

 Maine than any other rock, for, with some of the White Mountain gneisses and schists, 

 it occupies the whole country to the north-east as far as Dead river in Flagstaff. 



Rangeley Conglomerate. This conglomerate has given rise to much discussion, on 

 account of the flattening and distortion of some of the pebbles of which it is composed, 

 but its stratigraphical relations have received very little attention. This conglomerate 

 is confined to a limited area, extending N. 30° E. and S. 30° W. from the inlet of 



