F. R. Cowper Reed—Coastal Features, Co. Waterford. 553 
of the present’sea-cliffs. These are intermixed with a few fragments 
of the conglomerates, some of which are rounded, and there are a few 
non-local rocks like those in the underlying Boulder-clay. There is 
scarcely any fine matrix t@ the bed. The red sandstone fragments 
average 4—6 inches in length, and often have their angles ‘rounded off, 
but Pee yands the cliff they increase in size, number, “and angularity, 
attaining a length of -1-13 feet. The slabs mostly lie flat, being 
arranged in a decidedly parallel manner so as to give to the bed the 
appearance of stratification, but there is no sorting according to size, 
except in the horizontal manner above mentioned. This deposit is very 
distinct: and definitely marked off from the other beds. It dips at 
a much lower angle to the valley-floor than the rocky slope on which 
the Lower Head rests, and follows the slope and contour of the present 
‘ground, as seen by the edge of the cliff of drift in which it is exposed. 
At about 20 yards from the western corner of the beach it loses its 
distinctive characters, thinning out and merging into an overlying 
‘bed of sandy shingle. This bed of sandy shingle is a regular deposit, 
13-2 feet thick, consisting of small well-rounded pebbles and sub- 
angular fragments of the Old Red rocks, of fairly uniform size and 
roughly bedded. in sand; it overlaps the Upper Head eastwards in the 
cliff section, itself then thinning out and being replaced by a sandy 
bed without stones 6 inches to 1 foot thick and resting directly on 
the Boulder-clay. The materials of which this bed of shingle and 
sand are composed bear the obvious marks of arrangement and 
deposition by running water. Resting upon this bed come a clayey 
subsoil and soil, in all about 2 feet thick, almost devoid of rocky 
fragments and pebbles. 
Just as in the section at Fornaght Strand (Gror. Mae., Dec. V, 
Vol. IV, 1907, p. 17), we find here deposits of water-borne materials 
combined with the subaerial and coastal accumulations of pre-Glacial, 
Glacial, and post-Glacial times. 
The Boulder-clay of this portion of the coast does not contain the 
large masses of granites, gneisses, and metamorphic rocks which we 
have described near Passage (ibid., p. 501). Most of its non-local 
rocks might have been derived from the weathered débris of the 
neighbouring Old Red Sandstone conglomerates, which contain a most 
varied assortment of rocks. The greater part of the shingle of the 
existing beach appears to have been derived from this source. But 
the fragments of Carboniferous Limestone must have been brought 
from the country to the north by the ice or some other transporting 
agent; and there is so far no reason for thinking that the Boulder-clay 
here was the product of any ice-sheet but that from inland. There 
is no evidence that the Irish Sea ice touched the coast in this part, 
and no flints or marine shells have been found in any of the beds of 
drift. 
The relations of the present and ancient watercourses and of the 
inland topography to the movements indicated by the coastal features 
are still under examination, and promise to throw considerable ight 
on the later stages in the geological history of the country. 
