In some places the non-micaceous quartzite forms thick
massive sequences devoid of pelite; the best example of
this is on the hill northwest of Tregillus Creek.

The conglomerate is light grey and light brown. It con-
sists of pebbles and granules of white moderately coarse
grained well sorted quartzite in a poorly sorted matrix
of sand-sized clear and blue glassy quartz (Fig. 38). Gran-
ule conglomerate is more abundant than coarser grained
varieties. The percentage of quartzite clasts decreases with
decreasing grain size. The conglomerate is less than 15 m
thick and is usually 1 to 5 m thick. It is overlain by a
thin sequence of quartzite and pelite in turn overlain by
the calcareous rocks of the Kee Khan marble.

The poor sorting and local graded bedding of the
quartzite and its even and rhythmic interbedding with the
pelite suggest the rocks were deposited as proximal tur-
bidites (examples of which were shown by Walker, 1978,
Fig. 2, and by Poulton and Simony, 1980, Fig. 7 and 8).
The lack of crossbedding and sole markings also indicates
a proximal position on a submarine fan complex. The

Figure 38. Conglomerate from the upper part of the Tre-
gillus succession of the Snowshoe Group. The clasts are
white quartzite. The coin scale in each frame is a Cana-
dian dime. A (GSC 191031) and B (GSC 101032) come from
the southwest slope of the ridge north of Lightning Creek
at Pinegrove Creek (presently a ski resort).

massive sequences of quartzite may be channels within
the complex.

The age of the Tregillus is unknown. The rocks are
similar to those of the Hadrynian Windermere Super-
group, particularly the Horsethief Creek Group (see
Poulton and Simony, 1980) and as contradictory evidence
is lacking, they are correlated with that group.

Kee Khan marble

The Kee Khan marble is a thin discontinuous sequence
of marble, calcareous quartzite and phyllite. It is distin-
guished from other marble horizons by its magnetite-
bearing, chrome-green phyllite and position above the
conglomerate of the Tregillus, but otherwise the grey cal-
careous rocks of the Kee Khan are similar to others of
the Snowshoe Group.

The Kee Khan marble is limited to the northwest
corner of the Wells map area, following the distribution
of the Tregillus clastics. The Kee Khan was previously
mapped as Kaza Group (Snowshoe Formation) by
Campbell et al. (1973). Marble and phyllite of the unit
form the headwall of Kee Khan Creek and a base for the
top of the ski lift of the Troll Resort at Pinegrove Creek.
This exposure and those in bulldozer trails on Pinegrove
Mountain are representative of the Kee Khan marble at
its thickest, approximately 75 m.

The Kee Khan marble conformably overlies micaceous
quartzite of the Tregillus clastics. The contact is gener-
ally sharp and is drawn at the first calcareous quartzite
or chrome-green phyllite above the quartzite conglomer-
ate of the Tregillus.

Grey foliated marble is the dominant lithology of the
Kee Khan rocks. It weathers orange, brown or grey. It
is composed of 0.5 to 1.5 mm calcite crystals with subor-
dinate quartz, micas and minor feldspar. The calcite and
quartz are equant; the muscovite, chlorite and biotite
define foliation surfaces. The marble occurs in less than
10 m thick layers separated by calcareous and noncalcare-
ous phyllite and quartzite.

Phyllites of the Kee Khan are characteristically
chrome-green and olive-grey and grey varieties. The
chrome-green phyllite consists of chlorite, sericite, quartz,
epidote and minor magnetite. In places they are calcare-
ous and gradational with marble and, in others, sandy
and gradational with phyllitic quartzite. Locally thin
layers of orange weathering marble interbed with the
phyllite (Fig. 39). The olive-grey and grey phyllite is gen-
erally not calcareous and occurs as discrete interbeds with
the marble and quartzite.

The quartzite is poorly sorted, medium- to coarse-
grained, micaceous and commonly calcareous. Quartz
and feldspar clasts are the same types as those in the Tre-
gillus. The micaceous matrix is chlorite-rich where the
quartzite grades into the green phyllite.

The chrome-green phyllite is interpreted as derived
from both a terrigenous clastic and volcanic source. The

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