72 BULLETIN OF THE 
to the strike of the sandstones be so considered; the valley broadens 
farther southward beyond Meriden, and is bounded on the western side 
by a strong ascent. On the face of this hill, not far north of the proba- 
bly post-glacial trench that the Quinnipiac has cut through it from the 
west, there are numerous outcrops of reddish shaly sandstone with strike 
N. 70° E.,and dip 15° northwestward into the hill, and thus accounting 
for its steep eastern slope; but the westward dip itself is very unusual 
in the Triassic area, and suggests some local disturbance. Standing on 
the hill and facing about N. 50° E., one may look in the direction of 
the quarry bluff by Meriden, and in the distance beyond it see the de- 
scending northern end of Lamentation, showing that the hillside is in 
line with the fault already traced. Just south of the Quinnipiac, there 
are plentiful outcrops; the beds are about level near the bridge, but 
farther east steepen to a dip of 25° northwestward, beyond which the 
outcrops suddenly end. This confirms the occurrence of the fault. As 
its heave is on the east and of a value of several thousand feet, it is 
natural enough to find the beds immediately west of it somewhat flexed 
upward from the attitude that prevails generally in the monocline. 
Their abnormal dip is satisfactorily explained by associating it with this 
fault, as in the stream bed northeast of Lamentation, already men- 
tioned.’ Still farther to the southwest, the hill is so broadly covered 
1 The upward drag on this great fault, by which the dip of the beds on its west- 
ern side is here reversed from an eastward to a westward direction, is homologous 
with the drag that has flexed the posterior sheet (Percival’s P 2, E1) of Pond 
Mountain, the southernmost member of the main trap sheet, east of New Haven. 
This block is cut off by the heavy fault that limits the present area of the Triassic 
rocks on the southeast, and brings up the crystalline base of the formation against 
them; the drag has in one small locality even overturned some of the beds, so that 
the conglomerates that here belong beneath the posterior sheet seem to lie over it 
at a steep eastward angle. That they are really overturned and normally belong 
below the trap is shown, first, by the occurrence in the quarry near by to the north 
of much larger outcrops of similar conglomerate, dipping westward under the trap ; 
second, by the dense texture of the trap that apparently underlies the overturned 
beds, this dense texture being elsewhere characteristic of the base of the trap sheet, 
and in strong contrast with the loose vesicular texture of the upper surface of the 
sheet; third, by the absence of all trap fragments in the overturned conglomerate, 
while they are plentiful in the shaly conglomerate with westward dip that overlies 
the trap in an exposure by a pond an eighth of a mile northeast; fourth, by the 
general abrupt eastern face and gentler western slope of the trap ridge, which 
shows that its prevalent dip must be westward, and that the eastern dip of the 
conglomerate is local and exceptional. Search has been made for cross-bedding in 
the conglomerate, by which its upper and lower surface could be so snd detected ; 
but it could not be found. 
