EDEN VALLEY AND YORKSHIRE-DALE DISTRICT. 69 



undercurrent of local ice flowed northwards along this hollow, 

 while at higher elevations the main stream conformed to the 

 general direction taken by the Eden- valley ice. 



The influence of the local ice upon the Eden-valley stream 

 generally is well shown near Tebay, where the map (PI. II.) shows that 

 the southern boundary of Shap-granite dispersal has been deflected a 

 long way to the south, because just about there a considerable 

 depression exists, and the local ice does not seem to have risen high 

 enough to keep the Eden-valley stream so far from the Silurian 

 country as it has done in the neighbourhood of higher ground. So 

 too with the same boulders in the valley of the Bela. Here the 

 north-easterly-flowing ice passed over a deep valley in which the 

 lower layers of the ice were sheltered from the northerly impelling 

 force that affected the upper part ; and in consequence, the south- 

 easterly-moving Eden-valley ice, meeting with less cross-resistance, 

 flowed up the valley, striating the rocks and forcing the Eden-valley 

 drifts up the ravine. This is still more evident with the Brockram 

 drift in the same valley ; the map shows that there is a deflection of 

 the boundary-line of this drift two miles and a half out of the 

 course it has taken to the south. It is as well to mention that this 

 does not rest upon negative evidence, because the numerous drift- 

 sections to the east of the line (A) do not yield a single stone that 

 may not have come from the Carboniferous district to the south. 



We have therefore in these cases clear proof that while the 

 higher strata of the ice sheet were moving steadily forward in a 

 north-easterly direction, the lower layers, being sheltered from much 

 of the northerly impelling force that urged on the upper strata, and 

 being at the same time acted upon by a like amount of south-easterly 

 impelling force as affected the ice to the north and south of the 

 Bela, were forced in a direction nearly at right angles to the course 

 taken by the upper part of the ice sheet over the same ground. 



Only some such explanation as that given by Prof. Ramsay will 

 account for the fact that while the ice near the low ground in the 

 Howgill Eells and the adjoining parts of the Dale district was shed 

 nearly along the line indicated by the dots on the map, some of the 

 higher strata moved in directions nearly at right angles to the 

 course taken by the underlying streams. It is impossible to give 

 any satisfactory explanation of the striaj on Swarth Fell and Baugh 

 Fell if they were not caused by ice flowing from the high ground at 

 the head of Mallerstang. It has been shown that in Mallerstang 

 itself the drift moved towards the north — perhaps because the ice 

 had no other course open to it ; but at higher levels, where there 

 were fewer obstructions, the ice would flow everywhere away from 

 the highest ground. That the Baugh-Eell, and especially the 

 Swarth-Eell striae were produced by ice coming from the head of 

 Mallerstang seems to be almost proved by Prof. Hughes finding 

 Carboniferous sandstone in the drift on the north-western side of 

 the highest ground of the Howgill Eells. Most of the adjoining 

 Carboniferous Eell-tops are higher than any part of the Howgill 

 Eells ; it is therefore quite likely that some of the higher strata of 



