frequency of graded bedding and poor sorting which
could denote these rocks as proximal turbidites. The
sequence, however, is finer grained than the Ramos or
Tregillus and therefore may represent more distal parts
of a submarine fan. Contrary to this suggestion, how-
ever, is the absence of crossbedding and sole markings
common in distal facies. Local sorted, medium grained
sand must reflect either a change of environment or, more
reasonably, sporadic influxes of clean sands possibly due
to storm action on beach or longshore deposits.

The green calcareous phyllite was found only on the
Snowshoe Plateau, at the head of Little Showshoe and
Aster creeks and on Harveys ridge near the ‘Jeep’ trail
to Keithley Creek. This rock resembles metamorphosed
tuff. Either the volcanic activity these rocks represent was
limited or far removed because the beds in all places are
less than 3 m thick.

The age of the Harveys Ridge is unknown. It is
assigned to the Paleozoic by correlation with the Eagle
Bay Formation. The Harveys Ridge rocks resemble those
of unit 3 of the Eagle Bay Formation at Forest Lake near
Barriere (Preto et al., 1980; Preto, 1981). Although the
correlation with the Eagle Bay Formation is made with
some confidence, the age of the rocks of unit 3 is some-
what less secure.

Goose Peak quartzite

The Goose Peak is composed of coarse grained quartz-
ite with minor amounts of fine grained quartzite and
phyllite. The quartzite is characterized by its coarseness,
low percentage of matrix mica and persistent feldspar
content. Thick massive beds may be distinguished from
the Keithley orthoquartzite by their poor sorting. The unit
can be distinguished from other clean quartzite by the
well defined 50 to 100 cm thick bedding. The unit is a
lateral facies change of the Pine conglomerate.

The Goose Peak is located southeast of Mount Agnes
to Cariboo Lake. It has also been traced south of the map
area into the Goose Range. Within the map area the
thickest accumulations occur on the ridge southwest of
Pine Creek; however, it is thicker to the south. These
rocks were previously mapped as the basal conglomerate
of the Snowshoe Formation by Holland (1954), undif-
ferentiated Snowshoe Formation of Campbell (1963) and
as unit 4a by Struik (1982a). No type section for this unit
has been designated; it is named after a reference area
on Goose Peak south of the map area (Struik, 1983). The
quartzite is lensoidal on a regional scale, attaining a maxi-
mum thickness estimated at 250 m.

The contact with the underlying Harveys Ridge rocks
is sharp on the Snowshoe Plateau. At Mount Agnes the
Goose Peak quartzite, overlies grey micaceous quartzite
and phyllite in turn overlying black siltite assigned to the
Harveys Ridge.

The Goose Peak quartzite is light grey or locally dark
grey or pink, weathering grey or brown. It is made up

56

predominantly of clear white and minor black quartz with
up to 10% feldspar. It is poorly sorted and much is
coarse- or very coarse-grained, some being granule con-
glomerate. The clasts are generally subrounded. The
potassium feldspar is coarser grained, more abundant and
more altered than the plagioclase. Minor detrital musco-
vite found in the matrix also is part of some quartz-
feldspar grains. The matrix is composed of sericite and
fine grained quartz and minor plagioclase. The quartz and
some of the plagioclase is secondary.

Phyllite of the Goose Peak is mainly olive grey and
minor black. The olive-grey variety is like that of the
Keithley unit. It occurs as thicker beds than the black and
is associated with the finer quartzite of the Goose Peak.
Some of the olive phyllite is silty. The presence of olive-
grey phyllite increases to the south where it is associated
with the same type of grey quartz veins as those of the
Keithley succession. The black phyllite occurs as thin
interbeds with the coarse grained quartzite.

The quartzite occurs as 20 to 100 cm thick beds, rarely
attaining 200 cm thick. The beds are defined primarily
by the change in percentage of the coarse fraction of the
quartz clasts. A fining upwards of the coarse fraction
exists in some places, but mostly the individual beds are
of a different average grain size. Quartzite with the olive-
grey phyllite is generally more thinly bedded.

The poor sorting, coarse grain size, grading of the
coarse fraction, and low volume of pelitic rock, suggest
that these rocks represent a debris flow deposit, possibly
distal to the laterally equivalent Agnes conglomerate. The
sequences of quartzite with olive-grey phyllite may be the
turbiditic deposits at the border of the debris flows, and
the black phyllite, the accumulation in the debris flow
channel during quiet periods. There is little evidence that
the contact with underlying units is an unconformity and
the influx of coarse detritus may simply represent a
change in topography or climate in the source terrane.

None of the Goose Peak is dated, however, as it stra-
tigraphically overlies the Harveys Ridge succession it too
may be Paleozoic. No correlatives of the Goose Peak
beyond the Quesnel Highlands are known.

Agnes conglomerate

The Agnes conglomerate consists of granule to boulder
clasts of white to grey poorly sorted quartzite. The poorly
sorted quartzite clasts appear to be unique to the Agnes
conglomerate. Black phyllite forms minor thin beds
within the conglomerate. The matrix, and rarely some of
the clasts of the conglomerate, may be limestone. The
Agnes conglomerate is a lateral facies variation of the
Goose Peak quartzite.

The conglomerate is found mainly near Mount Agnes,
on the Snowshoe Plateau and on the ridges flanking Pine
Creek. Small exposures exist at Cornish Mountain and
Mount Amador. The conglomerate was previously
mapped as the basal Snowshoe Formation by Holland