28 
as 40° for the Millstone grit, there is only a difference of 4°, 
and the lowest beds of the grit are not exposed. 
Resting on the mottled bed of Millstone grit in the Morse 
railway section, comes a rose coloured sandstone of about eight 
inches thick, composed of well rounded grains of quartz, 
decomposing felspar and mica, and dipping at an angle of 19°. 
Over this bed, resting upon it conformably, comes another 
chiefly made up of large quartzitic pebbles, some of them 
lithologically corresponding to the Caradoc Sandstone of the 
lower Lickey Hills, Worcestershire. There is also a second 
pebble which is identical with those in the Old Red Con- 
glomerate. I am not aware that a Pebble bed, such as the 
one here described, has been observed elsewhere in the Forest 
of Dean, which would certainly have been the case had it 
belonged to the Millstone grit. 
The Pebble bed passes somewhat abruptly into a coarse 
variegated Sandstone which rests upon it at the same angle of 
dip, and like the 8-inch bed below is composed of well-rounded 
grains of quartz, decomposing felspar and mica. A section of 
this rock is given in Fig. III. magnified 22 diameters, and a 
fragment of Mica from the same in Fig. IV. magnified 130 
diameters. The sandstone is irregularly interspersed by layers 
of mar! or kaolin. 
Resting on the last bed comes a small Pebbly Conglomerate, 
the pebbles being well rounded and embedded in a highly 
ferruginous matrix, 
This ends the section, the small Pebble bed being capped by 
alluvial deposit. And now arises the question, whether the 
mottled sandstone, and the beds which underlie, are of the 
same age as those which rest upon it ata different angle of 
dip. 
In reasoning out this problem, the first possibility which 
suggests itself is, as to whether we have come across the old 
river bed which Sir Cuartes Lyextt described as running 
through the Forest.* The same phenomenon is also referred 
* Hlements of Geology, p. 510. 
