PLIOCEKE PEEIOD IN ENGLAND. 463 



Chalky Clay, is hidden by blown sand, and the extension of these 

 forest-beds there cannot in consequence be detected. At Hopton and 

 Corton Cliffs, however (about the centre of Sheet 67), it is said (for I 

 have not personally been fortunate enough to meet with the base of the 

 cliff sufficiently cleared of beach to see them) that they reappear 

 immediately under the Contorted Drift shown in fig. XIII. The 

 earlier beds of Stage II. being here absent, there is nothing to 

 show the age of the forest-remains of this part beyond their priority 

 to hS. 



During this stage we find no indication of the presence of the sea 

 over any other part of England than the south-eastern part of Nor- 

 folk, the eastern part of Suffolk, and the north-eastern part of Essex. 

 Erom sections discovered by the Survey the marine area appears to 

 have stretched up the Stour valley to Sudbury. 



Stage II. The Lower Glacial beds. 



The movement giving rise to the beds of this series was one of 

 depression, apparently not continuous, but broken into two move- 

 ments, of which the first was, compared to the second, of no great 

 extent. This first movement of depression, extending in an in- 

 creasing degree over northern Norfolk, seems to have been accom- 

 panied at the outset by elevation in north-east Suffolk, so that a part 

 of the laminated clay, forming the latest accumulation of Stage I., 

 was converted into land, giving rise, at Kessingland and Pakefield, to 

 the terrestrial surface on which the mammaliferous clay, with its 

 surface penetrated by roots, and the laminated bed with Unios, already 

 mentioned, were formed, and which are overlain directly by the 

 gravel, c, and the Chalky Clay *. At points to the south-west of 

 Kessingland Cliff — viz. at Henham in the north of Sheet 49, and at 

 Halesworth (on the Blyth river) in the north-east of Sheet 50 — 

 we meet with very clear evidence of a conversion of a part of the 

 Chillesford Clay into land at the close of Stage I. ; for at these 

 places there occur pebble-beaches, from 25 to 30 feet thick, bedded 

 up to foreshores or even low cliffs of this clay. The shingle of these 

 beaches is bedded at the angle of terrestrial repose, not, as in the 

 Ked Crag, in successive beds of oblique stratification, where sand 

 and shells thrown up as banks have been planed off again and others 

 heaped over them, but in one continuous oblique slope throughout 

 the 25 or 30 feet, their section presenting in this respect that which 

 the Chesil Bank, or any other great shingle-beach, would do if cut 

 at right angles to its trend. West and north of this beached shingle 

 the pebbles of which it is formed spread out in seams interstratified 

 with sands that are red or orange-coloured at base, and become lighter 

 in colour upwards. These, in many places, rest on the Chillesford 

 Clay, but in others have taken its place. Where they rest on it the 

 junction is marked by a strong line of erosion which indents the sur- 

 face of the clay ; but in some places in the valley of the Bure — that 



* See Harmer, he. cit. The view taken by that gentleman and myself, that 

 this bed may have intervened between the Contorted Drift and the gravel c, is 

 untenable in view of the case as traced in this present memoir. 



