608 LIEUT.-COL. H. H. GODWIN-AUSTEN ON THE 
itself. Thus, I conceive, at one time, previous to the deposition of the 
next set of lower-level gravels (Pease Marsh and Tillingbourne) and 
lastly the drift, these high-level. beds presented the character of a 
much more extensive flat alluvial terrace, bounded by a low scarp, 
jutting out towards the bend of the river, over what is now Stoke 
Park and Woodbridge. 
Still confining ourselves to section No. 1, we may note that another 
great change of conditions took place, indicated by the upper strata 
of loam and flints(g) that rest, apparently in a conformable manner, 
on the Lower-Greensand gravels (f) derived from the south. A great 
lapse of time, however, and the removal of many feet of the lower 
set of beds may be interpolated here. This is shown by a comparison 
of these two sections. At 15 miles 19°5 chains (at a point west of 
the new railway-station, fig. 3) the total thickness of the gravels and 
sands (a-f, fig. 1) is only 14 feet; they rest on the Tertiary clay, 
here two feet above the line, which at this point is 61°23 feet above 
the Wey; therefore the highest level is 77°23 ft., or, taking the level 
of the Wey at the railway-bridge at 100 ft. above the level of the 
sea, we have 177°23 from that datum-line. 
At the three-arch bridge, Cross Lanes, the depth of the cutting is 
44 feet in the same sands, and deducting the 12 feet of drift-gravel 
(precisely similar to the surface-beds in the first section), the total 
thickness of sands exposed is 32 feet ; and it would be a little more if 
the base were seen. Adding the height of line above the Wey, here 
69°37 feet, we have 101-37 for the top of the sands, or a difference 
of 24 feet at least, lost by denudation. 
Let us now see what relation this section bears to the country on 
the south, and what has been observed there. My father, in a paper 
entitled ‘* Land-surfaces beneath the Drift-gravel ”*, with which was 
given a map of this area, refers to the fact that the gravel-beds of 
the valley of the Wey are underlain by an old terrestrial surface, in- 
dicated by peat, trees, and sedimentary deposits, and that the remains 
of extinct Mammalia are usually associated with this old surface. 
He gives, as an example, the Pease Marsh, and mentions the fact that 
these beds are usually about 30 feet above the level of the present 
drainage-level: he says, p. 114, “ The older terrestrial surface does 
not occur anywhere, that I know of, on the immediate banks of the 
Wey or Mole; these rivers and their affluents now flow at levels much 
below the general outspread of the transported gravel :” such sections 
as are above described occur in the valley of the Tillingbourne, at Hast 
Shalford and Tangley Pond; they are lower than the terrace above the 
outcrop of the Neocomian clay, and rest upon this formation ; in some 
instances’ ‘ the roots of the larger trees descended into the subjacent 
clays.” The old terrestrial surface north of the gorge of the Wey, 
lately brought to light, must ‘not be confused with this much later 
one of the Tillingbourne, overlain near East Shalford Farm by 
8 feet of drift-gravel. My father remarks, p. 116, “This old land- 
surface supplies us with a definite and valuable, though isolated, date 
* Quart. Journ. Geol. Soe. vol. xi. p. 112 (read December 13, 1854). 
t Loe, cit, p. 114. 
