Vol. 58.] TEESDALE, WEARDALE, AND THE TYNE VALLEY. 593 
(3) Glacial Striz, ete. 
The strie in Weardale occur on the beds of limestone, and are 
especially plentiful in the neighbourhood of Stanhope. In all 
cases they are approximately parallel to the valleys in which they 
eccur. Among others, I noted the following :— 
1. Surface of the Great Limestone, at Ashe’s Quarry, Stanhope (900 feet). 
N.N.W. to 8.S.E. (63). 
2. Surface of limestone, in quarry at Jack’s Crag, near Stanhope (980 feet), 
S. 50° E. (62). 
3. Surface of limestone, Broadwood Quarry, near Frosterley (550 feet). 
S. 80° E. (64). 
[Since writing the above I have received a copy of the Trans- 
actions of the Weardale Naturalists’ Field-Club, which contains an 
account of a striated surface at Sandy Carr, 1 mile north of 
Wolsingham.' The surface consists of a Gannister, being situated 
near the base of the Millstone Grit, at an altitude of 900 feet 
above sea-level. The direction of the striz is given as east-north- 
easterly. | 
(4) Boundaries of the Ice at the Period of Maximum 
Glaciation. 
The valleys of the Wear and of its tributaries appear to have 
been occupied by ice of local origin, with the exception of Bedburn 
Beck, which at the period of maximum glaciation was occupied by 
a lobe of ice connected with the Teesdale Glacier. 
At the head of Weardale and in the upper portions of Wellhope - 
and Burnhope Burns the ice stood at a level of 2000 feet. 
At the head of Ireshope Burn (1800 feet) the ice of Weardale 
seems to have been confluent with that of Langdon Beck (Teesdale), 
but there is no evidence that there was any flow of ice from Wear- 
dale into Teesdale or vice versa, the ice being apparently shed off the 
col in both directions. 
In Swinehope Burn and Westernhope Beck, and on Snowhope 
Moor (74), the ice reached the 1750-foot contour-line ; and in the 
lower portion of the Dale, near Witton-le-Wear, the whole country 
appears to have been overridden. 
Below Witton-le-Wear the ice of Weardale was confluent with 
that of Teesdale, as is shown by the boulders of Lake- District rocks ; 
and also with that from the Tyne Valley, as evidenced by the boulders 
of Scottish granite and Silurian grit in the Drift north of Tow 
Law. This Driftis practically continuous with that of the Derwent 
Valley, which I shall show in §$ IV to be connected with that of 
the Tyne Valley. 
} «Glacier Footprints in the Wear Valley’ by W. M. Egglestone, Trans. 
Weardale Nat. Field-Club, vol. i (1909) pp. 78-86. 
