62 J. G. GO0DCH1LD ON THE GLACIAL PHENOMENA OE THE 



therefore that the line of ice-shedding must have been crossed. The 

 drifts just mentioned contain stones from the Upper Old Red con- 

 glomerates, others from the Lower Limestone shale ; and along with 

 these well-glaciated fragments of the Bluecaster diorite come in the 

 drifts to the N.N.E. Some of these drift- stones may be traced nearly 

 three miles to the N.N.E. of the nearest rock of the kind in place. 



On Swarth Fell east-north-easterly striae occur at elevations be- 

 tween 1950 and 2200 feet above the sea, on the same bed of rock 

 as that which has preserved the Baugh-Fell scratches. In one 

 instance they are crossed by a set ranging nearly S.E. Some of 

 the scratches are distinct enough ; but the remainder are very slight, 

 like those mentioned as occurring on Baugh Pell. None of these 

 striae prove which way the ice flowed. 



On the watershed between Mallerstang and Lunds north-north- 

 easterly scratches have been lately bared in the cuttings along the 

 Settle and Carlisle Railway ; and at Riggs, about a mile to the 

 N.N.E. from the spot where these striae occur, some remarkable 

 veins of silicified limestone have furnished boulders which have tra- 

 velled in a northerly direction. A reference to the map will show 

 that it is probable that the line of ice-shedding here nearly or quite 

 coincided with the present line of watershed between the Eden and 

 the Yore. 



A few other valley-striae occur in Mallerstang, but they do not 

 call for any particular remark ; but on the bold line of Millstone- 

 grit crags, known as Mallerstang Edge, a bed of gannister, on the 

 same geological horizon as that which bears the glacial markings on 

 Baugh Fell and Swarth Fell, shows two sets of striae ranging north- 

 north-easterly, at elevations about 2100 to 2150 feet above the sea. 

 In these cases, again, there is clear evidence that the glaciation was 

 but slight as compared with that at lower levels ; for around the 

 well-glaciated parts other striae may be found, even on the same 

 slab, which appear to be confined to the upper parts of the quartz- 

 pebbles that project from the surface of much of the rock. Even 

 on these the direction of the striae is clearly parallel to that of the 

 more obvious groovings near. 



Crossing into Swaledale we do not find much satisfactory evidence 

 anywhere south of the Swale to prove which way the ice went. In 

 Sleddale Beck (one of the northward-flowing tributaries of the 

 Swale) boulders of limestone from a faulted inlier have clearly been 

 carried northward ; as, however, this limestone lies not far above 

 the bottom of a deep valley radiating from the highest ground 

 within ten or twelve miles, later glaciers might be supposed to have 

 acted as the means of transport. 



At Keldside, after a storm, striae were laid bare from under drift 

 almost in the bed of the river Swale ; and these clearly pointed right 

 across the valley in which the river flows. 



To the north of this in West Stonesdale there is abundant evi- 

 dence to prove that parts of the ice moved across the valley of the Swale 

 and up the tributary valleys to the north. Many boulders of grey 

 limestone, of a kind that does not occur in this area above a cer- 



