2032 Reports and Proceedings— 
river-ice could raft away this material into the estuary. He also 
regards the copious mica which this clay contains as evidence of ice- 
degradation in Scotland having contributed to the mud of this 
river. 
In Stage II. he traced the conversion of some of this laminated 
clay, occupying sheet 49 and the north-east of sheet 50 of the Ord- 
nance map, into land, the accumulation against the shore of this 
land of thick shingle-beaches at Halesworth and Henham, and the 
outspread of this in the form of seams and beds of shingle in a sand 
originally (from its yielding shells in that region) called by him 
the Bure-valley bed, and which Prof. Prestwich recognized under 
the term ‘“‘ Westleton Shingle.” As the valley of the Crag river 
subsided northwards as the conversion of this part of the Chil- 
lesford clay into land occurred, there was let in from the direc- 
tion of the Baltic the shell Tellina balthica, which is not present in 
the beds of Stage I. The formation thus beginning he traced south- 
wards nearly to the limit in that direction of the Chillesford clay 
about Chillesford and Aldboro’. The Cromer Till he regards as the 
modification of this formation by the advance of the Crag glaciers 
into the sea or estuary where it was accumulated, such advance 
having been due partly to this northerly subsidence, but mainly to 
the increase of cold. Then, after describing a persistent uncon- 
formity between this Till and the Contorted Drift, from the eastern 
extremity of the Cromer cliff (but which does not appear in the 
western) to its furthest southern limit, he showed how the great sub- 
mergence set in with this drift, increasing much southwards, but 
still more westward towards Wales. The effect of this was to sub- 
merge the area of Red Crag converted into land during Stage I., so 
that the Contorted Drift lies upon it 50 feet thick, and to cause the 
retreat of the ice which had given rise to the Till to the slopes of 
the Chalk Wold; whence masses of reconstructed chalk were 
brought by bergs that broke off from it and were imbedded by their 
grounding in this drift, contorting it (and in those parts only) by 
the process. He then traced, in the form of gravels at great eleva- 
tions, the evidences of this submergence southwards and westwards, 
showing it to have increased greatly in both directions, but mostly 
in the western; and he connects these gravels with the Contorted 
Drift by the additional evidence of one of these marl masses, in 
which he found a pit excavated near the foot of Danbury Hill, in 
the London-clay country of South Essex, and which hill is covered 
from base to top by this gravel. The gravel which thus covers 
Danbury Hill, of which the summit has an elevation of 367 feet, 
rises in North Kent to upwards of 500 feet; to between 400 and 500 
feet on the Neocomian within the Weald; to 600 feet in North 
Hants (where it overlooks the Weald), and also in Wilts, Berks, and 
the adjoining parts of Bucks; to 420 feet in South Hants; to 540 
feet in Oxfordshire; to 400 feet in Cornwall; to upwards of 700 
(and perhaps 1000 and more) in the Cotteswolds ; to 1200 feet in 
Lancashire,’ and to 1340 feet in North Wales. Hastwards, through 
Kent towards France, their elevation falls, and in the North of 
