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On Mount Gething, the major features of this structural zone are a
flat-topped or ‘box’ anticline and a thrust fault. On the southwest limb
of the anticline, lower beds of the Dunlevy formation dip 45 to 60 degrees
to the southwest; on the crest of the same anticline, which is about 1 mile
wide, the same beds are flat or gently arched; on the northeast limb the beds
dip steeply to the northeast or are overturned. Along the thrust, on the
northeast side of the anticline, the lower beds of the Dunlevy are thrust over
on the upper or conglomerate-bearing part of the same formation (Beach
and Spivak, 1944).

A little farther northwest, on and near Stott Creek and at a lower
elevation than on Mount Gething, the anticline is more closely folded
than on that mountain, and lower strata are exposed on the crest, succes-
sively, of Jurassic, Triassic, and Permian age. The displacement along
the fault is greater than on Mount Gething, and several subsiduary folds
occur east of the fault (Beach and Spivak, 1944). It may be added that
although Beach and Spivak mention only one fault in the text, they show
two on Mount Gething on the Dunlevy-Portage Mountain map-sheet.
They record only one, however, to the north near Stott Creek, on the
same map-sheet, where the two faults coalesce. It may be that the
Gething-Stott structural zone is a northern continuation of the Commotion-
Hulecross structural zone. The latter will be described on a subsequent

age.
Eee Beattie Hill Structure
(See Figure 8)

Across Peace River to the northwest, the Gething-Stott structural
zone passes into a wide belt of disturbed rocks, both folded and faulted,
west of Rainbow Rocks. Little is known of the structure, except at the
westernmost end of this disturbed zone, on Beattie Hill.

West of Aylard Creek and in the eastern part of Beattie Hill, the
Triassic ‘Dark siltstones’ and overlying ‘Grey beds’ are flat-lying. On
the west end of the same hill these Triassic strata dip steeply to the west
(McLearn, 1940A). The structure may be a ‘flat-topped’ anticline, of
which the east limb is concealed, or it may be a monoclinal structure
bounded on the east by a fault.

Branham Ridge Syncline
(See Figure 8)

A broad, shallow syncline lies between the Beattie Hill and Horseshoe
Hill structures (McLearn, 1940, Figure 1; Beach and Spivak, 1944).
Strata ranging from the ‘Grey beds’ to the Dunlevy formation are involved
in this structure on Branham Ridge. The resistant rocks of the Dunlevy
are exposed in high cliffs on the top of the ridge and in large rock slides
on its higher slopes. The Fernie group is exposed in creek bottoms. The
‘Grey beds’and Pardonet beds are concealed below rock slides and boulder
clay on the lower slopes of the ridge, but their occurrence is inferred. This
syncline plunges to the southeast, for on the south side of the river the
Dunlevy formation is at a much lower elevation than on Branham Ridge.

The Branham Ridge syncline extends southeastward, and may be
continuous with the Pine River syncline in Pine River Valley. More