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The Shadows of Kingston Mills

Note the bleached margins of the reddish syenite boulders in the conglomerate. The basal clastics corresponds to the "Rideau beds" of Baker , whose type section is 1 km NW of here, and to the Shadow Lake Formation of Liberty Enter Highway westbound. Highway bridge crosses Cataraqui River, which is part of the Rideau Canal system.


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Hill on your right north is a partially exhumed Precambrian hill, transected by a late NE-trending fault with a throw of about 10 m, NW-side-down. Roadcut exposes the middle part of the Gull River Formation, the C-marker being readily recognizable. Glacially polished surfaces show spectacular glacial grooves. Spectacular columnar structures can be seen at the end of this road in sandstone of the Nepean Formation Potsdam Group, Cambrian age. Exposure of unconformity between Nepean Formation and Precambrian rocks on east side of road. Gravel pits between 1 and 3 km east of Highway 15 expose Pleistocene outwash deposits Henderson, Leave car on right shoulder of Highway 15 at road junction, and walk about m to north along the shoulder to roadcut or marble.

White marble with angular fragments of rusty-weathering paragneiss. The coarse-grained marble contains small flakes of biotite and graphite, and the gneiss fragments have rims consisting mainly of diopside, feldspar, and quartz. Wollastonite has not been found in this outcrip, though rare occurrences of this mineral are known in the area.

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Note the gently dipping, crudely developed gneissic layering which is folded by upright second folds. Outcrop of quartzitic gneiss with garnet, K-feldspar, plagioclase, magnetite, and traces of tourmaline, intruded by pegmatite with apatite and intergrowths of quartz-tourmaline. The rusty colour of the gneiss is due to weathering of iron sulphide. Garnet is fine grained. The gneissosity is nearly verticle and trends NE.

A shallow north-plunging lineation 1. Walk south on small overgrown path approx. This outcrop exposes facies 2 of the Nepean FormationL Sandstone with very large-scale cross-beds.

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The well-sorted, medium-grained quartz sandstone is characterized by very large, simple cross beds thought to be indicative of an eolian deposit. Note the blue colour of the quartz, caused by exsolution of very fine needles of rutile in this granulite-facies metaquartzite. The outcrop shows two sets of glacial striae, the older trending degrees, the younger trending degrees and cutting off the older set where the ice moved uphill best seen east side of the outcrop.

Chattermarks indicate that the ice causing the younger set moved to the southwest. Remnants of subglacial pot holes and fluting by subglacial streams can be observed the latter is best seen in the southern part of the outcrop. Remnants of calcite-cemented Pleistocene gravel are preserved on sandstone in the southern part of the outcrop. An irregular set of steep fractures in the sandstone strikes between and degrees.

Another irregular set of rust-stained fractures strikes approximately degrees and shows some post-Pleistocene movement, but is is not certain whether this is of tectonic origin or due to frost heaving. This now relatively low cliff may have provided the metaquartzite blocks observed in the curtain dunes of Stop 4.


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The dyke has well-developed chilled margins in which coarse tabular plagioclase phenocrysts can be recognized. The dyke is locally sheared and cut by veins of fibrous calcite, serpentine, and quartz. The large dyke is cut by a cm-wide dyke trending degrees. The granite on the east side of the outcrop contains skarn inclusions, and a layer of calcareous gneiss in white pegmatite can be observed at the western edge of the outcrop.

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Small outcrops along road are Nepean Formation. Leave car beside old limestone quarry and walk back along road downhill to east end of roadcut outcrop. Moderately west-dipping Precambrian quartzites and paragneisses with mafic dykes and sills are unconformably overlain by fine pebble conglomerate and limy sandstone of the Shadow Lake Formation which, in turn, is overlain by limestone of the Gull River Formation. This very flat erosion surface is typical of exposures where the full thickness of Black Riveran strata is present.

Coarse marble with white pegmatite can be seen at the west end of the roadcut. Exposures in roadcut are probably about 30 m above the base of the Black Riveran. Lower ground ahead is underlain by Precambrian rocks.

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Roadcut north of Loughborough Lake bridge. Either walk from parking lot at boat launch south of bridge, or pull car well off road. Roadcut exposes layered clinopyroxene gneiss with two generations of mafic dykes. Dykes of the older generation are fine grained, have a northeasterly strike, and dips ranging from nearly horizontral to vertical.

They have a metamorphic mineral assemblage consisting of hornblende, plagioclase, and biotite with some K-feldspar, opaques, and sphene. Some of these dykes have been intruded by pegmatites and are boundinaged and faulted.


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Secondary epidote alteration is common. A 5-m-wide dyke of medium-grained diabase belongs to the northeasterly striking Rideau swarm of the Frontenac Axis. It consists of slightly altered clinopyroxene and plagioclase which, in thin section, show fine zones of cataclastic deformation. They are coated with epidote and show steeply-plunging striations.

Minor displacements of a horizontal, approximately cm-wide dyke of the older generation indicate that the southeast side moved down. It is probably that these displacements are related to late reactivation on a NE-striking Precambrian fault along Loughborough Lake. Gently plunging folds of gneissose layering can be observed north of the diabase dyke. In the northern part of the outcrop, Precambrian rocks are unconformably overlain, on a very flat erosion surface, by basal sandstones of the Shadow Lake Formation.

Projection of this erosion surface to the south suggests about 20 m of south-side-down dip-slip displacement on the Loughborough Lake Fault. Proceed north on Perth Road. Entering Perth Road Pluton.

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This dominantly granitic pluton is one of nine discrete intrusive bodies designated as Frontenac type by Wynne-Edwards , b. The lenticular body was intruded while deformation was occuring into the crest of a domical structure within surrounding pyroxene gneiss and biotite-quartz-feldspar gneiss Ermanovics, The pluton is crudely zones, grading from a darker, dioritic core into a quartz-rich, granitic margin. Locally a narrow sheared zone is developed along the margins. At this locality, the medium-to coarse-grained, reddish-granite-like rock consists of oligoclase, K-feldspar, biotite and quartz.

A weakly developed tectonic foliation is parallel to the margin of the pluton. The relationship of this fabric to the sheared zone north of the pluton is unclear. Narrow shear zones and a number of thin seams of severely crushed rock, however, appear to be related to the formation of the sheared zone. Mylonites are best developed in paragneiss within a lozenge-shape zone, approximately 10 km long and up to 1. According to Ermanovics , the northwestern extension of the zone is a fault, but it is not certain whether this fault formed as brittle continuation of the mylonite-producing event or represents a later fault localized along the earlier formed mylonite zone Barclay, Paleozoic rocks on either side of the axis do not appear to be affected by the fault.

The mylonites contain minerals formed during low grade metamorphism, indicating that mylonitization postdates the peak of the severe regional metamorphism and the imposition of a regional gneissosity Ermanovics, An excellent example of the truncation of this gneissosity by the mylonitic planar fabric can be seen in a separate roadcut outcrop on the eastern side of the road, just south of the road sign of Perth Road. Marbles at the northwestern margin of the zone include tectonic fragments of mylonitized quartzofeldspathic rocks but are themselves coarsely recrystalized and show no relics of cataclastic deformation textures Barclay, On our traverse through the mylonite zone from south to north, note the irregular distribution and width of anastomosing bands of intense mylonitization in the paragneiss.

Where pegmatitic granite is affected by mylonitization, all stages from very slight to very severe can be observed. Mylonitic foliation strikes generally northeast and dips steeply to the northwest. A steeply-plunging extension lineation can be recognized on the mylonitic foliation planes. Asymmetric folds of the mylonitic foliation are most spectacular north of the road sign of Perth Road Village. Many of these have the form of sheath folds, as described by Rannie , and some show refolding of the foliation. Several stages of development of mylonitic foliation are indicated by the fact that folds of mylonitic foliation are locally enveloped by a cross-cutting later foliation.

According to Barclay , the distribution of mylonitic foliation and discrete mylonite bands varies non-uniformly throughout the zone. The orientation and sense of transport directions determined from various kinds of indicators vary considerably. Movement has been predominantly oblique slip, but the stretching direction varies from nearly horizontal to vertical. Relative movement between adjacent blocks along specific shear planes was in some places northwest-side-down and to the northeast; in other places, movement was northwest-side-up and to the southwest.

The asymmetry of the spectacular folds in Perth Road Village suggests that the northwest side moved up. A 2-m-wide ultramafic dyke at the northern end of the Perth Road Village cut, consisting of clinopyroxene, biotite, green hornblende, and minor calcite, has not been affected by the mylonitization. The medium-grained dyke strikes more or less parallel to the foliation , but dips approximately 30 degrees to the northwest, cross-cutting the steeply dipping foliation.

A small outlier of Shadow Lake grit is preserved above the folded mylonites in Perth Road Village east side of road on the down-throw side of a late, NW-striking fault which cuts the mylonite zone and down-drops the northeastern block about 15 m. The Canoe Lake Fault Fig.

The northeastern end of this fault, known as the Rideau Lake Fault Wynne-Edwards, a , was first recognized by Kay Drop down door bar access and the hidden mechanical room door are practically invisible in the space, but required a great amount of detail to produce this illusion, highlighted only by faint shadow lines of the outlining shape. The custom solid cherry wood door within the bar leads to a bevy of Beverages keeping company quenched for ages.

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