; 
SECTIONAL TRANSACTIONS.—C. 445 
thirty miles. The folding along the same line cannot represent a contraction 
of more than one mile. 
Many examples of astoundingly rapid variation in throw are found, the most 
extreme case proved being a change from over 700 yards to nil in a distance 
of 14 miles. Such cases are associated with the change of strike at the ‘ bends’ 
in the rim of the basin. 
A few cases of actual crossing of important faults have been found, but 
they are not common. There are several large-scale examples of reversal of 
throw along the same general line of fracture. No clear case of extensive 
lateral displacement along a fault-line has been found. 
It is obvious that a large part of the folding and faulting was pre-Permian, 
and-that it was continued through Permian and Triassic times. 
The deepest part of the present basin lies nearer to its eastern side, a little 
south-west of Manchester. Both the Coal Measures and the Collyhurst Sand- 
stone thicken towards this region, and thus suggest early movement roughly 
coincident with the later folding. ‘ 
Certain cases of rapid changes of strata associated with faults suggest 
possible fault movements during Coal Measure deposition. There is no clear 
indication that any of the three fault-systems is older or younger than the 
others, though the marked dominance of the N.W.-S.E. series may indicate 
that it was first in the field. 
The form of the coal basin indicates a large area of buried measures in 
which the coal should be at workable depth. The determining factor in actual 
development will be the thickness of the Permo-Triassic and Upper Coal 
Measure cover—not the depth of the coal-basin. 
12. Mr. G. Suatrer.—Observations on the Nordenskidld and Neigh- 
bouring Glaciers of Spitsbergen, 1921. 
The Nordenskisld Glacier.—As seen from Bruce City the gathering ground 
of this glacier is approximately marked by two great nunataks, Mts. Terrier 
and Ferrier. From these it passes downwards as a narrowing wedge-shaped 
mass deflected seawards by a long frontal moraine, the result of which is the 
formation of a compressed zone of ice in the south-western corner. 
The front of the glacier stretches two miles across the deep waters of Adolf 
Bay, forming partly submerged cliffs of ice, from which bergs are wrenched 
off at frequent intervals. 
The floor of the glacier has a fairly steep gradient, and consists of hard 
rocks of the pre-Devonian basement series associated with igneous rocks, whilst 
across the more central part is a buried ridge ot highly metamorphosed rocks. 
These rocks form the englacial moraine layers of the lower part of the ice, 
while the softer Permo-Carboniferous: rocks from the surrounding mountains 
furnish material for the surface moraines. 
The glacier may be divided into two main zones according to the distribution 
of tension and pressure. The central portion consists of an amphitheatre of 
broken ice dissected by two sets of crevasses into rectangular blocks, while 
towards the sides the ice assumes a rounded form. 
Directed concentrated pressure is indicated in the south-western portion 
by a zone of hummocky surface neve ice associated with thrust-planes, which 
passes into smooth, finely-corrugated uncrevassed ice dissected by inclined 
longitudinal fissures running parallel with the englacial bands and associated 
with ribbon-structure. Here the ice becomes increasingly stagnant towards 
the periphery, not one of the six surface moraines of this area reaching the 
sea. 
The ice in the central area moved 51.1 feet per day as determined in 
August by Mr. Mathieson with a theodolite. 
The englacial rim of ice adjoining the. frontal moraine was apparently 
stationary. 
Measurement of the overhanging ice-cliffs of the south-western compressed 
q ‘area showed irregular differential slide over the lower dirt-filled ice associated 
with marginal crevasses. The upper hummocky ice moved by thrust-planes 
towards the lower compressed area. 
The glacier is in a retreating phase, and the average retreat of the ice 
