part 3] THE GLACIATION OF KORTH-EASTEBJS" IRELAND. 357 



The valley of the Glenmakeeran River is, in its upper part, wider 

 and more open than that of the Carey, and is encumbered with 

 drift up to a height of about 680 feet. This drift is gravelly in 

 character, and the level of its upper edge is remarkably constant. 

 Above that level the drift is scanty, but there are numerous scattered 

 boulders of Fair Head dolerite and Carboniferous sandstone. 



In the lower parts of these valleys the Glacial gravels are 

 strongly in evidence, in places reaching over 100 feet in thickness, 

 and they are arranged in a series of terraces through which the 

 streams have cut, leaving against the hillsides flat-topped shelves 

 which make very conspicuous features in the scenery. 



The terraces stand at 680, 510, 430, and 340 feet, while in- 

 distinct remnants of other terraces at still lower levels appear 

 in the angle between the Care}*- and Glenshesk Rivers near their 

 junction (see fig. 1). The uppermost terrace was seen only in Glen- 

 makeeran, and is not so well marked as those at lower altitudes. 



Beneath the terrace-gravels a red boulder-clay is observed in 

 several sections, and in one of these it is 20 feet deep, its base 

 not being exposed. 



The terrace-gravels contain Carboniferous sandstone, basalt, 

 schist, chalk, flint, vein-quartz, red granite, red quartz-porphyry, 

 and the riebeckite-eurite of Ailsa Craig, also the granite of Goat- 

 fell and the columnar quartz-porphyry of Drummadoon in Arran. 



On the summit of Fair Head there is a little drift, but- many 

 surfaces of dolerite are strongly inoutonne and striated, and 

 erratics of granite including that of Goatfell are sparsely scattered 

 over the undulating surface. The striae on the shores of Lough 

 Doo run from north 40° east (true). 



In Murlough Bay, south-east of Fair Head, so many large land- 

 slips have taken place since the formation of the drifts that it is 

 impossible to make out the sequence of the Glacial deposits, 

 although boulder-clay can be seen in several places. 



The surface of the Carboniferous rocks which lie between Fair 

 Head and Ballycastle is covered by gravelly drift in places showing 

 moraine-like forms ; but the denudation here has been severe and 

 what look, at first sight, like moraine mounds may be the remains 

 of a former extension of the gravel-terraces. 



The flanks of Knocklayde are but sparsely covered with drift, 

 except on their lower slopes, where gravels similar to those already 

 described occur, although, owing to the steeper inclination of the 

 sides of Glenshesk, no terraces can be detected in that valley. 



The western part of the area, that west of the Ballycastle 

 Rallwajr and the fault, is less heavily covered with drift, except in 

 the morainic area extending from Annoy to Ballymoney, which 

 will be described later. 



The coastal region consists of rugged basaltic uplands with but 

 little drift, and inland between these uplands and the morainic 

 country lies a large bog drained by the Inver Burn, Stracam River, 

 and other streams into the Bush River. 



The drift over the whole of this region is characterized by the 

 presence of the rock of Ailsa Craig and other northern erratics. 



