478 S. V. WOOD, JUN., ON- THE N"EWER 



the western edge of the ice, towards the last part, at least, of its re- 

 treat during the present stage, and throughout its advance during 

 Stage III., rested. Hence their great profusion on that side. In 

 the case of the gravels accumulated during the advance of the ice 

 and emergence of the land in Stage III., there is a more intimate 

 connexion as regards constituent material between them and the 

 morainic clay, these gravels, where they approach this clay, being 

 composed, in a most marked way, of the harder materials of which it 

 is made up, so that they are flinty in the Eastern, and oolitic in the 

 East Midland counties ; while in Sheets 1 and 7 pebbles from the 

 beds numbered iv. and viii. in fig. YI. form a considerable pro- 

 portion of the whole material ; and in Sheets 66, 67, and 48, the 

 rolled chalk so characteristic of the Morainic clay is, where the 

 gravel is overlain by this clay, associated in the upper part with 

 the flints and quartzites of the overlying morainic mass, in which 

 position also the sand of c is, in Sheet 66, often largely made up of 

 chalk grains *. 



Up to the time of the setting in of the general submergence of 

 England, that is to say during the formation of beds b 1 and h ^, the 

 only sea of which we flnd any indication is that of the Crag, ex- 

 tended northwards so as to reach the Humber ; and consequently, 

 as the inclination of England, so far as it diff'ered from what it now 

 is, was more easterly, the ice, which descended from the eastern 

 slope of the Pennine, sought this sea, so that the earliest Glacial 

 accumulation, the Till h 2, and the basement clay of Holderness 

 represent the morainic extrusion of this ice on the sands 6 i of i1,s 

 bottom ; and if there be any other glacial accumulations of similar 

 age in England, they can only be of a purely terrestrial nature. 



After the completion of the great submergence, however, this was 

 different, and the ice sought the sea in its changed position, travel- 

 ling to it under the entirely altered inclination of England which 

 had thus taken place, as we shall see in examining the phenomena 

 of the Chalky Clay. 



To arrive at an idea of what this inclination was, we must com- 

 pare the evidences of the submergence in the different parts. Cromer- 

 Lighthouse hiU, in flg. YIII., is one of the highest points in Norfolk 

 which is covered by marine gravel (for shell fragments occur in this 

 gravel capping the Contorted Drift in the Cromer Cliff), and its 

 height is 247 feet. The distance from this to Moel Tryfaen, where 

 tbe gravel with marine Mollusca lies at the elevation of 1350 feet, 

 being 230 miles, and the difference in altitude 1103 feet, it would, 

 if the entire submergence were shown at Cromer, as it is at Moel 

 Tryfaen, give the westerly increment of depression as nearly 4*8 

 feet per mile; while the distance to Well Hill (where, from the 

 summit of the chalk downs not having been covered, we get the 

 limit of submergence at about 560 feet) being 120 miles, it 



* At Bealings, in the north of Sheet 48, this presence of chalk in abun- 

 dance continues in the upper part of the gravel, though uncovered by tbe clay, 

 for a mile or so only beyond the limit reached by the clay, the chalk disappear- 

 ing from the gravel beyond this distance. 



