236 JOWETT AND MUFF : GLACIATION OF BRADFORD, ETC. 
It is very probable that on account of the conformation of 
the ground (see PI. XXI.) the Oxenhope Lake was still dis- 
charging at Cuckoo Park. The surface-level of this lake was 
therefore about 960 feet. The difference in the levels of the 
lakes was thus barely 15 feet. This explains why the gap at 
Stanbury Height is such a shallow one, being cut down only 
a few feet. 
By the time that the ice had retreated sufficiently to allow 
the Flappit Spring overflow to operate, the Haworth ridge was 
sufficiently free from ice to admit of the waters of the Worth 
Lake passing round the spur. The Worth and Oxenhope Lakes 
thus coalesced to form one large lake with arms stretching up 
Bridgehouse Beck towards Oxenhope, up the Slade Beck to the 
south of Stanbury, and up the main valley of the Worth. 
In addition to the above another complication ensued, but 
with results of an opposite nature. The retreat of the ice 
combined with the rapid lowering of the surface-level of the 
Worth Lake exposed the ridge on the north-west side of the 
Worth Valley. A lake was then formed at the head of the 
Newsholme Dean Beck, which discharged into the Worth Lake. 
The Outlets of the Newsholme Lake. — The highest overflow 
of this lake took place by Dry Clough, rather over a mile west 
of Oakworth. It commences as a very shallow valley on the 
watershed, at 1,100 feet, but deepens rapidly and runs as a 
streamless valley down to the 925-foot contour, where it ends. 
It appears to have been deserted about the time that the Flappit 
Spring channel was coming into operation. 
The retreat of the ice opened a channel at Griff Wood to 
the north-west of Oakworth. This valley is quite dry and 
terminates at 840 feet in a level fan of detritus, through which 
an iron rod passed for nine feet before reaching rock. On 
following the valley upwards towards the north-north-west, it 
is found to trench completely through the watershed. Shortly 
after this, it makes a sharp bend to the west-north-west, and 
runs as a shallow channel along the hillside for about 300 yards. 
This feature, viz., the deflection of the overflow-channel at its 
intake away from the ice has already been noticed in connection 
with the dry gap at Wibsey Bank Foot (p. 224). It also occurs 
