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Ministry of Northern Development and Mines
Ontario
Ontario Geological Survey Open File Report 5875
Paleozoic Geology of Southern Bruce Peninsula Southern Ontario
1993
Ministry of Northern Development and Mines
Ontario
ONTARIO GEOLOGICAL SURVEY
Open File Report 5875
Paleozoic Geology of Southern Bruce Peninsula, Southern Ontario
By
D. Armstrong
1993
Parts of this publication may be quoted if credit is given. It is recommended that reference to this publication be made in the following form:
Armstrong, D. 1993. Paleozoic Geology of Southern Bmce Peninsula, Southern Ontario; Ontario Geological Survey, Open File Report 5875, 19p.
® Queen's Printer for Ontario, 1993
Ontario Geological Survey
OPEN FILE REPORT
Open File Reports are made available to the public subject to the following conditions:
This report is unedited. Discrepancies may occur for which the Ontario Geological Survey does not assume liability. Recommendations and statements •of opinions expressed are those of the author or authors and are not to be construed as statements of government policy.
This Open File Report is available for viewing at the following locations:
Mines Library Level A3r 933 Ramsey Lake Road Sudbury, Ontario P3E 6B5
Mines and Minerals Information Centre (MMIC) Rm. M2-17, Macdonald Block 900 Bay St. Toronto, Ontario M7A 1C3
The office of the Resident Geologist whose district includes the area covered by this report.
Copies of this report may be obtained at the user's expense from:
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XXX
TABLE OF CONTENTS
ABSTRACT vii
INTRODUCTION 1
STRATIGRAPHY 1 ORDOVICIAN 2
Georgian Bay Formation 2 Queenston Formation 2
SILURIAN 3 Manitoulin Formation 3 Cabot Head Formation 4 Wingfield Formation 5 Dyer Bay Formation 5 Fossil Hill Formation 6 Amabel Formation 7 Guelph Formation 9
UPPER SILURIAN 12
Salina and Bass Islands Formations 12
ECONOMIC GEOLOGY 13
KARST 14
STRUCTURAL GEOLOGY 15
ACKNOWLEDGEMENTS 15
REFERENCES 16
CONVERSION TABLE 19
Map P,3236 - Paleozoic Geology, Southern Bruce Peninsula, Southern Ontario Back pocket
V
ABSTRACT
The Paleozoic strata of the Bruce Peninsula form the defining physiographic feature of the peninsula, the Niagara Escarpment, and host significant building stone and aggregate resources. In 1987 the Ontario Geological Survey initiated a multi-year project designed, to map the exposed Paleozoic bedrock of the Bruce Peninsula at a scale of 1:50 000. In addition to surface mapping, a number of shallow to moderate depth (up to 123 m) drill holes were cored to provide subsurface data.
This report consists of the marginal notes for the preliminary map of the Paleozoic Geology of the Southern Bruce Peninsula (P.map 3236) . The map area consists of the mainland part of the Bruce Peninsula between latitudes 44^30'and 44* *45' . Fieldwork in this map area was conducted during the summer of 1989, by the author and his assistant, Mr. A. Anastas.
The oldest exposed Paleozoic unit in the map area comprises shales and minor limestones and siltstones of the Upper Ordovician Georgian Bay Formation. These are poorly exposed along the western shore of Owen Sound. Overlying this unit are the red shales and interbedded green shales and limestones of the Queenston Formation. The dolostones of the Lower Silurian Manitoulin Formation form a discontinuous subordinate escarpment below the main Niagara Escarpment. The Silurian-Ordovician contact (between the Manitoulin and Queenston formations) is exposed at Indian Falls and on the northeast side of Owen Sound. The Cabot Head, Dyer Bay, and Wingfield formations are poorly exposed along the base of the Niagara Escarpment. A regionally angular unconformity at the base of the Fossil Hill Formation progressively cuts the underlying Wingfield and Dyer Bay formations to the south, such that the Fossil Hill Formation disconformably overlies the Cabot Head Formation south of Owen Sound. The Amabel Formation, forming the main face of the Niagara Escarpment, is subdivided into two members: the lower Lions Head Member; and upper Wiarton/Colpoy Bay Member. The latter member is subdivided into two lithofacies: biohermal and non-biohermal. The biohermal lithofacies is best developed towards the top of the Amabel Formation. The Guelph Formation consists of biohermal , non-biohermal and inter-biohermal lithofacies. The bituminous and typically laminated inter-biohermal lithofacies consititutes the Eramosa Member. The biohermal lithofacies is developed stratigraphically below, lateral to, and above the inter-biohermal lithofacies. In a northwest trending zone, in the vicinity of Shallow Lake and Hepworth, the Eramosa Member is limestone instead of dolostone.
The Wiarton/Colpoy Bay Member of the Amabel Formation and the Eramosa Member of the Guelph Formation are significant sources of dimension and building stone products, and aggregate in the map area. The distribution of the Eramosa Member is delineated on this map. The Manitoulin Formation is also quarried for aggregate in the map area.
vii
In the Bruce Peninsula, a number of zinc sulphide occurrences have been identified in the biohermal lithofacies of the Guelph and Amabel formations, as well as in the inter-biohermal Eramosa Member. The resource potential of most of these occurrences has been extensively evaluated. A previously unreported occurrence of sphalerite was discovered in the biohermal lithofacies of the Guelph Formation southeast of Wiarton.
The only hydrocarbon-producing field on the Bruce Peninsula is the now-abandoned natural gas field at Hepworth. This field produced natural gas from Middle Ordovician strata up until about 1935.
IX
Paleozoic Geology of Southern Bruce Peninsula, Southern Ontario
by D. Armstrong^
^Geologist, Sedimentary and Environmental Geoscience Section, Ontario Geological Survey
XI
PALEOZOIC GEOLOGY OF THE SOUTHERN BRUCE PENINSULA
INTRODUCTION
Regional mapping by the Ontario Geological Survey (OGS) of the exposed Paleozoic strata on the Bruce Peninsula commenced in 1987 with mapping of the northern portion of the peninsula, north of latitude 45°00'N (Armstrong and Dubord 1992). This was followed, in subsequent years, with mapping of the central and southern portions of the peninsula (Armstrong 1993, and this report, respectively).
The southern Bruce Peninsula map area is covered by 1:50,000 scale N.T.S. map sheets: Wiarton (41A/11); and the western part of Owen Sound (41A/10). The Bruce Peninsula can be accessed by King's highways 6 and 26, via Owen Sound, and by King's Highway 21, via Southampton. Public and private, paved and gravel roads provide good access in much of the map area. Access to some of the more remote regions is afforded by the Bruce Trail, numerous other trails and abandoned roads.
Subsurface information in the southern Bruce Peninsula map area is provided by records of five petroleum exploration wells (locations plotted on the map) and two shallow drill holes (up to 106.45 m deep) cored by the. OGS in 1990 (OGS-90-2 and OGS-90-3). Detailed core descriptions and geophysical logs of the two shallow OGS drill holes will be published in a future open file report (Armstrong in prep.). Regional subsurface information is provided also by a deep (to Precambrian basement) drill hole cored by the OGS in 1982 (OGS-82-4) in the central Bruce Peninsula, approximately 6 km northwest of Wiarton (see Johnson et al. 1985) .
STRATIGRAPHY
The exposed Paleozoic strata of the Bruce Peninsula have been studied and mapped by a succession of geologists since the turn of this century. Although the resultant geological maps (Williams 1919; Caley 1945; Liberty 1966; Liberty and Bolton 1971) are generally consistent in their delineation of most formational contacts, there are significant exceptions, notably the two youngest formations (the Amabel and Guelph formations). Additionally, numerous reports have been written on the stratigraphy, paleontology, and depositional histories of the Silurian strata of the Bruce Peninsula (Williams 1919; Bolton 1953; Bolton 1957; Sanford 1969; Liberty and Bolton 1971). Owing to its accessibility and relatively good bedrock exposure, the Silurian strata of the Bruce Peninsula have also been the subject of a number of geological field trips (e.g.. Winder and Sanford 1972; Telford 1978; Armstrong and Goodman 1990).
1
The southern Bruce Peninsula is underlain by over 700 m of Paleozoic strata, however, less than 200 m (stratigraphic thickness) of these strata, ranging from Upper Ordovician to Middle Silurian in age, are exposed. An additional 200 m of Upper Silurian strata may subcrop beneath Quaternary sediments in the southwest corner of the map area.
ORDOVICIAN
Georgian Bay Formation The oldest strata exposed on the southern Bruce Peninsula are the grey-green, siliciclastic shales, bioclastic limestones, and calcareous siltstones of the Upper Ordovician Georgian Bay Formation. This unit is exposed in a narrow outcrop belt along the western shore of Owen Sound in the vicinity of Pyette Point and Gravelly Bay. Typically, outcrops are small sections or bedding planes along the shore. The limestone interbeds of this formation commonly contain abundant bryozoans, brachiopods, orthoconic nautiloids and pelecypods, as well as rare corals and stromatoporoids. Sedimentary structures such as ripple marks and gutter casts are common in the limestone and siltstone interbeds. Locally, bioclastic limestone interbeds are capped by ripple laminated calcisiltites.
The Georgian Bay Formation is approximately 100 m thick in drill hole OGS-82-4 (Johnson et al. 1985). Only approximately 10 m of the uppermost part of this formation is exposed in this map area.
Oueenston Formation The Upper Ordovician Queenston Formation conformably overlies the Georgian Bay Formation. In addition to its characteristic red siliciclastic shales, the Queenston Formation on the Bruce Peninsula, contains significant interbeds of grey-green shale, siltstone and limestone.
In the map area, Queenston Formation strata are exposed in small sections along and above the western and southeastern shores of Owen Sound. A limestone-rich interval in the lower half of the formation locally caps small bluffs. The best such exposure in the map area, is at Sutton Point (approximately 10 km north of Owen Sound) where 3 m of argillaceous, bioclastic limestone overlies more than 5 m of grey and red shales. This limestone-rich interval is probably continuous with similar strata exposed to the north, in the Big Bay area and on Cape Croker (Armstrong 1993). Upper Queenston Formation strata, mostly red shales capped by 2 to 5 m of grey-green shales, are well exposed beneath dolostones of the Lower Silurian Manitoulin Formation at the waterfall in Indian Creek less than 1 km northwest of Balmy Beach (in the Indian Falls Conservation Area) and in an outcrop on the northeast side of the town of Owen Sound.
2
Limestone interbeds in the Queenston Formation range from non-fossiliferous, very fine-grained, dark grey beds up to 10 cm thick, to very fossiliferous, grey, argillaceous beds up to 1 m thick. Fauna include abundant brachiopods, bivalves and bryozoans, as well as sparse corals and orthoconic nautiloids. In addition to limestone interbeds, very thin- to thin-bedded, calcareous and non-calcareous, fine-grained, green-grey to grey-brown siltstone interbeds are locally significant. Commonly, these siltstone interbeds are either planar or ripple-laminated.
Traditionally, the basal contact of the Queenston Formation with the Georgian Bay Formation is placed at the base of the lowest significant red shale bed (Liberty and Bolton 1971). Aside from the grey-green shales, which commonly occur in the uppermost few metres, the Queenston Formation typically contains only minor, thin grey-green shale beds and rare carbonate beds. On the Bruce Peninsula however, a significant interval of interbedded grey-green shale and limestone occurs in the lower half of the formation. In drill hole OGS-82-4, located northwest of Wiarton, this interval is approximately 10 m thick and is separated from lithologically similar Georgian Bay Formation strata by approximately 10 m of red shale (Johnson et al. 1985). The basal contact of the Queenston Formation with the Georgian Bay Formation is not exposed in the map area.
Almost 60 m of strata assigned to the Queenston Formation were intersected in drill hole OGS-82-4 (Johnson et al. 1985). Records from oil and gas wells drilled in the map area indicate that this formation ranges from 55 to 80 m in thickness. The thickest exposed sections in the region are: 8.5 m at Sutton Point; more than 6 m at Indian Falls; and more than 20 m in the cliff exposure in the northeast end of Owen Sound. The sharp and disconformable upper contact of the Queenston Formation with the Manitoulin Formation is exposed in the latter two outcrops.
SILURIAN
Manitoulin Formation In the southern Bruce Peninsula map area, the Lower Silurian Manitoulin Formation is exposed in a discontinuous escarpment along the western and southeastern shores of Owen Sound. Scattered bedding plane outcrops of this formation occur on a 2 to 4 km wide plain, which extends westward from this escarpment to the base of the main Niagara Escarpment.
The Manitoulin Formation consists generally of thin- to thick-bedded, light grey-brown to blue-grey, buff-brown weathering dolostones, calcareous dolostones and minor limestones. This formation can be grossly subdivided into two informal units: a lower thin- to thick-bedded, fine- to coarse crystalline dolostone, which is commonly planar laminated or cross-stratified; and an upper, thin-bedded, bioturbated.
fossiliferous, fine- to medium-crystalline dolostone (Anastas 1992). In the southern Bruce Peninsula map area, the basal 0.5 to 2 m of the lower unit is commonly bioturbated, argillaceous, fine crystalline and slightly to very calcareous. Very thin shale beds and partings occur locally in these basal beds. Silicified fossils (brachiopods, crinoids and corals) are common in the upper unit and thin, discontinuous, silicified, fossil-fragment grainstone beds are common in the lower unit. Chert nodules and lenses are common throughout the formation. Hardgrounds (early-cemented surfaces) are visible in the upper beds of this formation, in the readout on 10th Street West in Owen Sound.
The Manitoulin Formation dolostones sharply and disconformably overlie shales of the Queenston Formation. This basal contact is exposed at Indian Falls (less than 1 km northwest of Balmy Beach) and in an outcrop on the northeast side of Owen Sound. It also may be locally exposed beneath the almost continuous escarpment of Manitoulin Formation dolostone north of Hogg.
The upper contact of the Manitoulin Formation with the Cabot Head Formation is not exposed in the map area; however, in drill core it is very gradational (Johnson et al. 1985) , The thickest exposures of the Manitoulin Formation in the map area, up to 10 m, are located 1.5 km east of Kemble and at Indian Falls. Johnson et al. (1985) report a thickness of 12.5 m for this formation in drill hole OGS-82-4.
Cabot Head Formation In the southern Bruce Peninsula, the Lower Silurian Cabot Head Formation (the Cabot Head (restricted) Member of Liberty and Bolton, 1971) consists primarily of siliciclastic shales. Generally, it is poorly exposed due to its shaly nature. In the map area, it subcrops beneath the vegetated slopes of talus and glacial drift between the main Niagara Escarpment and the plain formed by the underlying Manitoulin Formation. Because of its poor exposure, narrow outcrop belt and the scale of mapping, this unit, as depicted on the accompanying map, is combined with the overlying Dyer Bay Formation.
Only three exposures of the Cabot Head Formation were identified in the map area: in a readout on the northwest side of Owen Sound; a readout south of Owen Sound near Inglis Falls; and in a ditch outcrop southeast of Gowan Lake, 2.6 km northeast of Wolseley. In both readouts approximately 1.5 m of mainly green siliciclastic shales are exposed beneath overlying dolostone units. In the outcrop on the northwest side of Owen Sound, the Cabot Head Formation is sharply overlain by dolostone of the Dyer Bay Formation, whereas in the Inglis Falls readout, it is sharply overlain by the Fossil Hill Formation. In the Gowan Lake outcrop, approximately 1.5 m of green and maroon shales directly underlie a thin bed (20 cm) of very fine-
crystalline dolostone (basal bed of the Dyer Bay Formation or carbonate interbed in Cabot Head Formation?).
The lower contact of the Cabot Head Formation is not exposed in this map area. In drill hole OGS-82-4, approximately 25 m of strata were assigned to this formation (Johnson et al. 1985). This formation is reported to be up to 40 m thick in petroleum exploration wells in the map area (these well records likely included overlying units in this thickness).
Wingfield Formation The Middle Silurian Wingfield Formation consists of grey-green shale interbedded with thin beds of grey-brown, fine- to medium-crystalline dolostone and argillaceous dolostone, with grey-green shale lithoclasts and partings. Although dominantly dolostone, thin shale interbeds predispose this unit to recessive weathering.
The Wingfield Formation thins progressively towards the south, as it is cut by a regional angular unconformity at the base of the overlying Fossil Hill Formation (Armstrong in prep.). Although not exposed in this map area, it is interpreted to subcrop beneath Quaternary sediments near Wiarton. The Wingfield Formation is less than 2 m thick in an outcrop south of Big Bay, less than 2 km north of this map area (Armstrong 1993). It was not intersected in either of the two shallow OGS drill holes in the map area.
Dyer Bay Formation Dolostones of the Middle Silurian Dyer Bay Formation are not well exposed in the map area. Only three outcrops were found: on the south shore of Bass Lake; in a road cut 2.5 km northwest of Balmy Beach; and in a readout on the northwest side of Owen Sound. Because of its poor exposure, narrow outcrop belt and the scale of mapping, this unit is generally combined with the underlying Cabot Head Formation, on the accompanying map.
The Dyer Bay Formation consists of thin- to medium-bedded, light grey to dark grey-brown, micro- to coarse-crystalline dolostone and argillaceous dolostone. The basal 1 m is commonly microcrystalline. This formation typically exhibits platy, planar to slightly irregular parting. The Dyer Bay Formation is sparsely to moderately fossiliferous, with fauna being dominated by bryozoans; the fauna also include corals, brachiopods, and few gastropods. Trace fossils are abundant, as are various non-biogenic sedimentary structures such as soft-sediment slumps, scour marks, ripple marks, horizontal and low angle cross-stratified beds and lithoclasts.
Both in outcrop and in the subsurface (drill holes OGS-90-2 and OGS-90-3), the basal contact of the Dyer Bay Formation with the Cabot Head Formation is sharp. This contact is exposed in
only one outcrop in the map area, the roadcut on the northwest side of Owen Sound. The sharp and disconformable upper contact of the Dyer Bay Formation with the Fossil Hill Formation is also exposed at this outcrop and at a roadcut 2.2 km northwest of Balmy Beach.
In the southern Bruce Peninsula, the Dyer Bay Formation is disconformably overlain by the dolostones of the Fossil Hill Formation. The units that overlie the Dyer Bay Formation in the central and northern parts of the peninsula, the Wingfield and St. Edmund formations (Armstrong and Dubord 1992; and Armstrong 1993), have been cut out by a regionally angular unconformity at the base of the Fossil Hill Formation. The Dyer Bay Formation itself is cut out by this unconformity in the southeast corner of the map area. In an outcrop on the northwest side of Owen Sound, the Dyer Bay Formation is less than 1 m thick and at the Inglis Falls roadcut, just south of Owen Sound, this formation is absent. In Gleason Brook at Oxenden, just 2.6 km north of the map area, most of the entire Dyer Bay Formation interval (approximately 4 m thick) is exposed (Armstrong 1993).
In the southcentral part of the map area, drill hole OGS-90-2 encountered 2.87 m of this formation, whereas approximately 14 km to the north, drill hole OGS-90-3 encountered 4.42 m of this formation (Armstrong in prep.). In drill hole OGS-82-4, located north of this map area, the Dyer Bay Formation is 4.88 m thick and is overlain by the Wingfield Formation (Johnson et al. 1985).
Fossil Hill Formation The Middle Silurian Fossil Hill Formation, primarily consists of thin- to medium-bedded fossiliferous dolostone. In the southern Bruce Peninsula map area, it commonly occurs at the base of the Niagara Escarpment or forms a discontinuous subordinate escarpment below the main escarpment. Notable outcrops of this formation occur: 2.4 km north of Kemble; south of Gowan Lake and Bass Lake; near Lindenwood 4.6 west of Hogg; 2.2 km northwest of Balmy Beach; and in readouts on the northwest side of Owen Sound and at Inglis Falls.
The Fossil Hill Formation consists of thin- to medium-bedded, light to dark brown, fine- to coarse-crystalline, fossiliferous dolostone with an abundant and commonly silicified fauna and local chert nodules. The fauna is dominated by pentamerid brachiopods and includes locally significant occurrences of corals (syringoporid, halysitid, and favositid types) and stromatoporoids.
On the Bruce Peninsula the basal contact of the Fossil Hill Formation is a regionally angular unconformity, cutting progressively older units in a southwardly direction. Just north of this map area, this formation sharply overlies grey-green shales and interbedded dolostones of the Wingfield Formation
8
(Armstrong 1993). Northwest of Owen Sound the Fossil Hill Formation disconformably overlies the Dyer Bay Formation. South of Owen Sound, at Inglis Falls, the Fossil Hill Formation disconformably overlies the Cabot Head Formation.
The Fossil Hill Formation ranges from approximately 4 m thick in northern part of the map area, to less than 2 m thick at Inglis Falls. In the subsurface, this formation thins southwardly from 3.75 m in drill hole OGS-90-3 to 1.98 m in OGS-90-2. Anomalously high values for the thickness of this unit (up to 18 m) are reported in records from petroleum exploration wells in the map area. This may be due to the inclusion of lithologically similar overlying and underlying units.
Amabel Formation The white-weathering dolostones of the Amabel Formation form the main cliff face of the Niagara Escarpment on the Bruce Peninsula. On the peninsula, the Amabel Formation is stratigraphically subdivided into a lower unit, the Lions Head Member and an upper unit, the Wiarton/Colpoy Bay Member (modified from Liberty and Bolton 1971). In this study, the Amabel Formation is subdivided into three lithofacies: lithofacies A^ corresponds directly to the Lions Head Member, and lithofacies A^ and A^ correspond to the non-biohermal and biohermal lithofacies of the Wiarton/Colpoy Bay Member, respectively. In the map area, lithofacies Ag constitutes the lowest few metres of the formation. Lithofacies A]3 comprises most of the remainder of the formation, that is, the Wiarton/Colpoy Bay Member. Lithofacies A-. occurs discontinuously in the upper part of the Wiarton/Colpoy Bay Member.
The Lions Head Member, or lithofacies A , consists of light grey-tan, thin- to thick-bedded, platy to blocky parted, fine-crystalline, dense, non- to sparsely fossiliferous dolostone with locally significant blue to purple mottles, chert nodules and microstylolites. The sparse fossils, which include corals, stromatoporoids, and crinoids, are commonly broken and silicified. Mottles are typically distinct and range from sparse, small, burrow-like shapes to more intense swirly forms. Thin blue beds with sharp upper contacts (possibly hardgrounds) occur locally near the base of this member.
In this map area and immediately to the north (Armstrong 1993) , small (1 m thick by 2 m wide) fossiliferous lenses (bioherms?) occur locally in the middle to upper part of the Lions Head Member. Although the faunal constituents of these lenses is obscured by dolomitization, echinoderm concentrations and bryozoans have been identified. The best exposure of these biohermal (?) lenses is in a readout 2.2 km north of Kemble (recently removed by road widening) and in a second cut 1.8 km further north (Armstrong and Goodman 1990; Armstrong 1993).
The sharp basal contact of the Lions Head Member with the underlying Fossil Hill Formation tends to weather recessively and
is not generally well exposed. The occurrence of pyrite and glauconite at or near this contact (both in outcrop and drill core) and the southward thinning of the Fossil Hill Formation suggests that the contact is disconformable. This contact is exposed: in an outcrop 2.2 km northwest of Balmy Beach; in the Inglis Falls readout; in a readout 1 km north of Inglis Falls; and in a small outcrop approximately 3 km southeast of Owen Sound.
Despite intense dolomitization, which obscures fossil content and primary sedimentary structures in the Wiarton/Colpoy Bay Member, two gross lithofacies have been identified: the non-biohermal lithofacies A^; and the biohermal lithofacies A^. These lithofacies are differentiated on the basis of apparent fossil content and related porosity, bedding morphology, weathering characteristics and locally, style and intensity of mottling.
Lithofacies Aj consists of white to light grey-tan, blue-grey mottled, fine- to medium-crystalline, thick- to massive-bedded, sparsely to very fossiliferous dolostone. Although a moderately to well developed, fine, inter-crystalline porosity is common to this lithofacies, porosity can range from nonexistent to local fossil moldic and vuggy. Lithofacies A^ appears to consist mainly of sand-sized echinoderm fragments. Locally identifiable fossils include echinoderms, corals (rugose and tabulate), cephalopods and brachiopods. The characteristic streaky, diffuse, blue-grey mottling and related (?) ribbed pattern exhibited on weathered vertical faces (i.e., on dissolution enhanced joint surfaces), appear to indicate primary bedding and locally is suggestive of cross-stratification.
Generally, lithofacies Aj gradationally overlies lithofacies A^. Locally, however, coarser beds of lithofacies Aj sharply overlie lithofacies A^, or interbeds of one lithofacies occur within the other. In the northern Bruce Peninsula, lithofacies A^ grades laterally, to the north and northwest, into lithofacies Ag. (Armstrong and Dubord 1992) .
Lithofacies AQ is lithologically similar to lithofacies A^ except that it is commonly more intensely and irregularly blue-grey mottled and it is coarser crystalline. In addition, the fauna, which are essentially the same as in lithofacies Aj , are generally more obvious, larger and rimmed by blue-grey colouration. Also, bedding is more lensoidal or undulatory than in lithofacies A^, and lithofacies A^ tends to weather more ruggedly than lithofacies A]-,; the latter weathers into relatively smooth, large, jointed blocks. These characteristics are consistent with a biohermal origin for lithofacies A^. Small lenses of lithofacies A^, a few metres in width, occur locally in lithofacies A^ and could not be indicated on the map.
The large, northwest trending biohermal ridges that occur within the upper half of the Amabel Formation in the central
Bruce Peninsula (Armstrong 1993) are not well developed in the southern part of the peninsula.
No single outcrop on the Bruce Peninsula exposes a complete section through the Amabel Formation. The most complete section, approximately 25 m thick (Bolton-1957), is exposed in the large road cut on the north side of Wiarton. Other good exposures of this formation are located along the Niagara Escarpment: at Springmount; 2.5 km northeast of Springmount; at Inglis Falls; and on Highway 26, 0.5 km east of Bothwell's Corners.
In the subsurface of the southern Bruce Peninsula- the thickness of this formation ranges from 25.73 m (drill hole OGS-90-3) to 31.93 m (drill hole OGS-90-2) (Armstrong in prep.). The thickness of the Amabel Formation encountered in petroleum exploration wells is not typically reported because this unit is commonly combined on the well records with the overlying Guelph Formation.
Guelph Formation In this study, four lithofacies constitute the Guelph Formation. Two lithofacies, G^ and Gj , correspond to the strata assigned to the Eramosa Member (previously of the Amabel Formation; Liberty and Bolton 1971). The remainder of the Guelph Formation consists of a non-biohermal lithofacies G^ and a biohermal lithofacies G^. Lithofacies G^ and Gj (i.e. the Eramosa Member) occupy an inter-biohermal position in the lower part of the formation. The bioherms of lithofacies G^ occur at various stratigraphic horizons in the formation: underlying, overlying and lateral to the Eramosa Member lithofacies. Lithofacies G . occurs throughout the Guelph Formation, overlying and grading laterally into lithofacies G^ and gradationally overlying lithofacies G^ and G-^.
The Eramosa Member, generally consisting of thin-bedded, bituminous dolostone, can be subdivided into two lithofacies, G^ and Gt). Lithofacies G^ is composed of tan-grey to black, very fine- to medium-crystalline, thin- to medium-bedded, sparsely fossiliferous, moderately to very bituminous, laminated dolostone. Interbeds of non-laminated, slightly bituminous dolostone, lithofacies Gt), are common. Fossils, including brachiopods, ostracods and corals, are typically small and sparse. Laminae occurring towards the base of lithofacies Gg. are stromatolitic.
Lithofacies G^ consists of light tan to grey-tan, thin- to thick-bedded, sparsely fossiliferous, slightly to moderately bituminous dolostone with sparse to abundant microstylolites and local chert. Locally, this lithofacies is moderately fossiliferous, containing fragmented corals and shells. Lithofacies G^ is commonly interbedded with lithofacies Gg. and is transitional in character between lithofacies Gg and GQ. The contact between lithofacies G-^ and G^ is gradational.
10
In the southern and central Bruce Peninsula, the lithofacies which constitute the Eramosa Member occur in three informal units: 1) a basal unit consisting of lithofacies 0 ,; 2) a middle unit consisting of the laminated lithofacies G^ (informally termed the "Marble Bed"); and 3) an upper unit consisting of interbedded lithofacies Gg. and Gj . This internal stratigraphy of the Eramosa Member is best exposed in the building stone quarries located along Oliphant Road, a few kilometres northwest of Wiarton (Armstrong 1993; Armstrong and Meadows 1988). These units are not differentiated on the accompanying map, however outcrops of lithofacies Gg. are indicated.
The internal stratigraphy of the Eramosa Member appears to be continuous throughout the southern Bruce Peninsula, at least as far south as Owen Sound Ledgerock's Owen Sound Quarry. Extension of these units further southward is obscured due to drift cover. One outcrop of thin-bedded, slightly bituminous dolostone (lithofacies G^?) in the North Spey River, 2.1 km south of Rockford, may be part of the Eramosa Member.
Approximately 12 m of Eramosa Member strata are exposed in the Oliphant Road quarries. OGS drill holes in the southern Bruce Peninsula intersected the Eramosa Member with an average thickness of 33 m (Armstrong in prep.).
In a roughly northwest trending zone from south of Shallow Lake to 4 km west of Hepworth, much of the Eramosa Member (both lithofacies G^ and Gj ) is limestone instead of dolostone. The only other occurrence of limestone on the Bruce Peninsula, in either the Guelph or Amabel formations, is located in the central part of the peninsula, on the eastern shore of Stokes Bay.
Lithofacies G^ comprises the bulk of the Guelph Formation on the Bruce Peninsula. This lithofacies consists of light grey-tan to brown, fine- to medium-crystalline, thin- to thick-bedded, sparsely to very fossiliferous dolostone. It is typically tabular bedded and beds are generally horizontally oriented. Locally, lithofacies G^ exhibits minor blue-grey mottling. Fauna within lithofacies G^ includes bivalves, gastropods, brachiopods, cephalopods, corals, stromatoporoids, and echinoderms. Locally, these fossils are concentrated into biostromal horizons or into small (less than 3 m diameter) biohermal mounds; both of which are included within this lithofacies.
On weathered surfaces, lithofacies G^ commonly exhibits a course sub-horizontal ribbing (centimetre to decimetre scale), which corresponds to interbeds of softer, more porous (more fossiliferous?) dolostone and more resistant, less porous beds. Locally the non-porous beds appear laminated. As with the Amabel Formation, dolomitization has obscured much of the primary structures and fossil content in the Guelph Formation.
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In addition to inter-crystalline, fossil moldic and vuggy types of porosity, a small "wormy" porosity is locally developed in lithofacies G^. These pores appear to be either small leached burrows or inter-pisolite cavities. This "wormy" porosity occurs in outcrops near Allenford (probably stratigraphically, the highest Guelph Formation strata exposed in the southern Bruce Peninsula) and at the north end of the Bruce Peninsula, in the Tobermory area (Armstrong and Dubord 1992),
Generally, lithofacies G^ gradationally overlies lithofacies G^. Lithofacies G^ also grades laterally into the flank beds of lithofacies G ^ bioherms. Non-horizontal (up to 20°) beds of lithofacies GQ, G^ and G^ are interpreted as draping over lithofacies G^ bioherms and are included in the lithofacies G, map unit. Generally lithofacies GQ is stratigraphically, the highest part of the Guelph Formation exposed on the southern Bruce Peninsula. Drill hole OGS-90-2 intersected over 26 m of this lithofacies.
Lithofacies G^ consists of light grey-tan to tan, locally blue-grey mottled, medium- to very coarse-crystalline, thin- to thick-bedded, irregular to lensoidal bedded, fossiliferous dolostone. This lithofacies is interpreted to be biohermal in origin. The fossil types are essentially the same as in lithofacies G^, however, more abundant and larger frame-builders (corals and stromatoporoids) predominate. Fossils are commonly concentrated in type-specific zones. Very coarse encrinitic grainstones are common in the lower and flanking parts of these bioherms.
Blue-grey colouration, either as mottles or rimming fossils, similar to that exhibited by the Amabel Formation biohermal lithofacies AQ, is common. In addition, the commonly thick and lensoidal bedding of lithofacies G ^ is also similar to that of lithofacies A^. Where lithofacies G^ bioherms occur at stratigraphically low positions within the Guelph Formation, their lithologic similarity to 7\mabel Formation biohermal lithofacies complicates the placement of the inter-formational contact.
Guelph Formation biohermal lithofacies G j is best developed in two stratigraphic horizons. South of Owen Sound and northeast of Cruickshank to McNab Lake, lithofacies G^ is developed directly over Amabel Formation lithofacies A^ or A^ and appears to be, in part, laterally equivalent to lower parts of the Eramosa Member. The most notable of these lower Guelph bioherms, in terms of faunal content and preservation, are those which are exposed along Highway 6 and 10 south of Owen Sound to Rockford. No lower Guelph Formation bioherms were encountered in the two OGS drill holes in the map area. However, relatively fossiliferous beds, possibly derived from these lower bioherms, were intersected in the basal few metres of the Eramosa Member in both OGS-90-2 and OGS-90-3 (Armstrong in prep.).
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In the upper Guelph Formation, lithofacies G, bioherms overlie, and may be, in part, equivalent to upper Eramosa Member strata. These bioherms are best developed in the Boat Lake-Sauble Falls-Lonely Island area, and in the Mountain Lake-Francis Lake area. Notable outcrops in these areas are the fossiliferous and fossil-specific beds on the west shore of Lonely Island and the thick coral-rich beds outcropping between Francis and Mountain lakes. The upper Guelph biohermal lithofacies was encountered in drill hole OGS-90-3, where it is 21 m thick (Armstrong in prep.).
It appears as though there is no intervening non-biohermal lithofacies between the upper Guelph lithofacies G^ in the Francis Lake area and the lower Guelph lithofacies G j of the McNab Lake area. Although there are few outcrops in the connecting area, the hummocky terrain, as evidenced in aerial photographs, is consistent with biohermal strata near surface. This characteristic was also seen in biohermal zones in the Ira Lake and Forty Hills areas of the central and northern Bruce Peninsula.
Areas designated on the map as being underlain by lithofacies G^ commonly include a number of individual bioherms and intervening areas with outcrops of lithofacies G^ or G^. Beds of these latter lithofacies are commonly oriented sub-horizontal, as they drape or flank the bioherms.
The basal contact of the Guelph Formation with Amabel Formation is not exposed in the map area. In drill core the contact is sharp, however, formation-specific characteristics (eg. mottling) can occur on both sides of the contact (Armstrong in prep.).
The upper contact of the Guelph Formation with the Upper Silurian Salina Formation is covered by overburden, so the total thickness of the Guelph Formation is unknown in this map area. There is no single outcrop in the map area which exposes a complete section through the Guelph Formation. The thickest Guelph Formation interval intersected in OGS drill holes in the region is almost 60 m (OGS-90-2). The lowest 33.5 m of this interval is assigned to the Eramosa Member (Armstrong in prep.).
UPPER SILURIAN
Salina and Bass Islands Formations Although not exposed in the southern Bruce Peninsula, the Upper Silurian Salina and Bass Island formations have been interpreted by Liberty and Bolton (1971) to subcrop beneath thick Quaternary deposits in the southwestern corner of the.map area. The Salina Formation in this area is described by Liberty and Bolton (1971) as consisting of interbedded grey dolostone, green shale, brown dolostone, and red shale. They describe the Bass Island Formation as consisting of brown fine-crystalline dolostone.
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ECONOMIC GEOLOGY
The Manitoulin, Amabel and Guelph formations have been quarried on the Bruce Peninsula since before the turn of the century. A variety of commodities have been produced, including building stone, aggregate and lime (Parks 1912; Goudge 1938). The Manitoulin Formation is currently quarried for aggregate by E.G. King Ltd. in Sarawak Township, less than 2 km northwest of Hogg.
The Wiarton/Colpoy Bay Member of the Amabel Formation is currently quarried for aggregate at Sutherland Ltd.'s quarry in Keppel Township, less than 2.5 km northwest of Benallen, and at E.G. King's quarry in Sydenham Township, less than 5 km east of Owen Sound (just east of the map area). This unit is also quarried for dimension stone at the Adair Marble Quarry, south of Hope Bay in the central Bruce Peninsula (Derry Michener Booth and Wahl and Ontario Geological Survey 1989; Armstrong 1993).
The Eramosa Member of the Guelph Formation is quarried for building, landscaping and dimension stone at: a number of quarries in the Oliphant Road area northwest of Wiarton; at the McCartney Quarry, 5 km southeast of Wiarton; and at the Owen Sound Ledgerock Quarry, 0.5 km southwest of Cruickshank (Armstrong and Meadows 1988; Derry Michener Booth and Wahl and Ontario Geological Survey 1989). The laminated nature of lithofacies Gg. in the middle unit of this member, commonly called the "Marble Bed", produces a decorative polished dimension stone. Outcrops of the middle unit occur in the two areas underlain by the Eramosa Member in the southern Bruce Peninsula; in belts which extend from the Oliphant road quarries to Francis Lake and from west of Hepworth to Cruickshank.
Elsewhere in the map area, three small, currently inactive quarries were developed in Guelph Formation strata (other than the Eramosa Member). These quarries are located 3 km northeast of Allenford, on the northeast side of Alvanley and 0.4 km northeast of Boat Lake.
All of the lithofacies of the Guelph Formation (including the Eramosa Member) may locally yield thicker-bedded blocks suitable for dimension stone. Amabel Formation lithofacies Aj is a proven source of dimension stone and underlies a relatively narrow belt in the eastern half of the southern Bruce Peninsula, from Wiarton to Owen Sound. This unit also has good potential as a source of aggregate. The Ontario Geological Survey recently conducted an evaluation of aggregate resources in St. Edmund and Lindsay townships (Ontario Geological Survey, in prep). Aggregate quality tests conducted by the Ministry of Transportation of Ontario (MTO) yielded generally favourable results for outcrop samples of both the Guelph and Amabel
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14
formations. Development is controlled, on the eastern side of the peninsula, by the Niagara Escarpment Plan.
The Guelph and Amabel formations are host to a number of zinc sulphide (sphalerite) occurrences on the Bruce Peninsula. These have been extensively investigated since the early part of this century (Williams 1919; Guillet 1967; Liberty and Bolton 1971; Sangster and Liberty 1971; Tworo 1985). Despite intensive mapping, trenching, geochemical sampling, and diamond drilling, none of these occurrences were proven to be economic deposits. The only sphalerite mineralization found in the map area occurs as fracture- and pore-fillings in coral-rich beds (lithofacies G^) immediately overlying the Eramosa Member, in an outcrop 1.4 km west of Mountain Lake.
In the southern Bruce Peninsula, potential shale resources are limited to the narrow outcrop belts of the Cabot Head, Queenston and Georgian Bay formations. The significant limestone and siltstone interbeds in the Queenston Formation in this area may limit the development potential of this shale.
The only hydrocarbon-producing field on the Bruce Peninsula is the now-abandoned natural gas field at Hepworth. This field produced gas from the Ordovician Simcoe Group (or Trenton-Black River Group) at a depth of approximately 427 m, from 1901 to approximately 1935 (Bailey and Cochrane 1984). Outside of the Hepworth field, five hydrocarbon exploration wells have been drilled in the southern Bruce Peninsula map area. Of these, the three wells closest to the Hepworth field encountered shows of natural gas at depths of 429 to 491 m.
KARST
Relatively thin drift cover over the Bruce Peninsula has exposed the predominantly carbonate bedrock surface to the dissolution action of water. Karst features and processes on the Bruce Peninsula were described by Cowell (1976) and Cowell and Ford (1980). Karst pavement has developed on exposed bedrock surfaces and karstic dissolution has progressed through joints, fractures and other porous zones into the subsurface. In general, dissolution s^ems most intense in lithofacies with a higher fossil content and associated higher initial porosity (i.e. lithofacies A^ and G^ and the biostromal zones in lithofacies Gc)• Typically, pitted karstic pavement is well developed on bedding plane outcrops of the Guelph Formation on the western shore of the peninsula.
Dissolution-enhanced joints characterize karst development in the thick-bedded Amabel Formation dolostones (lithofacies A^ and A^), located on the topographically higher eastern side of the peninsula. In both the Amabel and Guelph formations, clint and grike karst systems are locally well developed.
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STRUCTURAL GEOLOGY
Liberty and Bolton (1971) report the regional dip of Paleozoic strata on the Bruce Peninsula to range from 4.8 to 7.6 m/km to the southwest. The regional strike and dip for this map area, determined using the base of the Fossil Hill Formation (encountered in two OGS drill holes and an outcrop) as datum, are 163° and 6.64 m/km to the southwest, respectively.
A well developed joint system is evident in the dolostone strata of the Bruce Peninsula. Joint orientations were systematically measured in this map area. Two major joint orientations were observed at 55 to 90° and 125 to 165°. Generally, joints were less well developed in biohermal strata. In grass-covered fields, where dolostone bedrock is covered by less than 1 m of overburden, joint patterns are visible as stripes of greener and taller grass. This phenomenon is presumably due to water retention in the joints. These joint patterns are well developed in fields underlain by the Manitoulin, Fossil Hill, Amabel and Guelph formations, and are visible on 1:10,000 scale aerial photographs.
ACKNOWLEDGEMENTS The author acknowledges the on-going assistance of the owners and operators of the quarries in the southern Bruce Peninsula. Permission, granted by the Chippewas of Saugeen Band to enter the Chiefs Point and Saugeen Indian Reserves (I.R. 28 and 29) is appreciated. The author also greatly appreciated the assistance of Alexis Anastas during the field season.
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16
REFERENCES
Anastas, A.S. 1992: Sedimentology and stratigraphy of the Manitoulin Formation,
Lower Silurian, southern Ontario, Canada; University of Waterloo, unpublished MSc Thesis, 150p.
Armstrong, D.K. 1989: Paleozoic geology of the southern Bruce Peninsula; in
Summary of Field Work and Other Activities 1989, Ontario Geological Survey, Miscellaneous Paper 146, p.222-227.
1993: Paleozoic geology of the central Bruce Peninsula, southern Ontario; Ontario Geological Survey, Open File Report 5856, 19p.
in preparation: Bruce Peninsula Paleozoic drilling program results; Ontario Geological Survey, Open File Report.
Armstrong D.K. and Dubord, M.P. 1992: Paleozoic geology of the northern Bruce Peninsula, southern
Ontario; Ontario Geological Survey, Open File Map 198, scale 1:50 000.
Armstrong, D.K. and Goodman, W.R. 1990: Stratigraphy and depositional environments of Niagaran
carbonates, Bruce Peninsula, Ontario; American Association of Petroleiim Geologists, 1990 Eastern Section Meeting, hosted by Ontario Petroleum Institute, London, Ontario, Field Trip Guidebook #2, 59p.
Armstrong, D.K., and Meadows, J.R. 1988: Stratigraphy and Resource Potential of the Eramosa Member
(Amabel Formation), Bruce Peninsula, Ontario; Ontario Geological Survey, Open File Report 5662, 89p.
Bailey Geological Services Ltd., and Cochrane, R.O. 1984: Evaluation of the Conventional and Potential Oil and Gas
Reserves of the Ordovician of Ontario; Ontario Geological Survey, Open File Report 5498, 77p.
Bolton, T.E. 1953: Silurian formations of the Niagara Escarpment in Ontario;
Geological Survey of Canada, Paper 53-23, 19p. 1957: Silurian Stratigraphy and Paleontology of the Niagara
Escarpment in Ontario; Geological Survey of Canada, Memoir 289, 145p.
Caley, J.F. 1945: Preliminary Map, Owen Sound, Ontario; Geological Survey of
Canada.
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Cowell, D.W. 1976: Karst Geomorphology of the Bruce Peninsula, Ontario;
McMaster University, unpublished M.Sc. Thesis, 231p.
Cowell, D.W., and Ford, D.C. 1980: Hydrochemistry of a dolomite karst: the Bruce Peninsula of
Ontario; Canadian Journal of Earth Science, Volume 17, p.520-526.
Derry Michener Booth and Wahl and Ontario Geological Survey 1989: Limestone Industries of Ontario, Volume III - Limestone
Industries and Resources of Central and Southwestern Ontario; Ontario Ministry of Natural Resources, Land Management Branch, 175p.
Goudge, M.F.. 1938: Limestones of Canada, Part IV, Ontario; Canada Department
of Mines and Resources, Bureau of Mines, Publication 781, 321p.
Guillet, G.R. 1967: Notes on Zinc-Lead Mineralization in Silurian Dolomite of
the Niagara Escarpment and Bruce Peninsula, Ontario; Ontario Department of Mines, Miscellaneous Paper 8, 25p.
Johnson, M.D., Russell, D.J., and Telford, P.G. 1985: Oil Shale Assessment Project Drillholes for Regional
Correlation 1983/84; Ontario Geological Survey, Open File Report 5565, 49p.
Liberty, B.A. 1966: Geology of the Bruce Peninsula; Geological Survey of
Canada, Paper 65-41, 8p., 13 maps.
Liberty, B.A. and Bolton, T.E. 1971: Paleozoic Geology of the Bruce Peninsula Area, Ontario;
Geological Survey of Canada, Memoir 360, 163p.
Ontario Geological Survey in preparation: Aggregate Resources Inventory of St. Edmund and
Lindsay Townships, Bruce County; Ontario Geological Survey, Aggregate Resources Inventory Paper.
Parks, W.A. 1912: Report on the Building and Ornamental Stones of Canada,
Volume 1; Canada Department of Mines, Mines Branch, Publication Number 100, 376p.
Sanford, B.V. 1969: Silurian of Southwestern Ontario; Ontario Petroleum
Institute, Eighth Annual Conference Proceedings, Technical Paper Number Five, p.1-44.
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Telford, P.G. 1978: Silurian stratigraphy of the Niagara Escarpment, Niagara
Falls to the Bruce Peninsula; in Currie, A.L. and Mackasey, W.O. (eds.), Toronto'78 Field Trips Guidebook, Joint Annual Meeting of the Geological Society of America, the Geological Association of Canada and the Mineralogical Society of Canada, p.28-42.
Tworo, A.G. 1985: The Nature and Origin of Lead-Zinc Mineralization, Middle
Silurian Dolomites, Southern Ontario; University of Waterloo, unpublished M.Sc. thesis, 276p.
Williams, M.Y. 1919: The Silurian Geology and Faunas of Ontario Peninsula, and
Manitoulin and Adjacent Islands; Geological Survey of Canada, Memoir 111, 195p.
Winder, C.G. and Sanford, B.V. 1972: Stratigraphy and paleontology of the Paleozoic rocks of
southern Ontario; Excursion A45-C45, 24th International Geological Congress, Montreal, 74p.
18
CONVERSION FACTORS FOR MEASUREMENTS IN ONTARIO GEOLOGICAL SURVEY PUBLICATIONS
Conversion from SI to Imperial
SI Unit Multiplied by Gives
Conversion from Imperial to SI
Imperial Unit Multiplied by Gives
1 mm 1cm I m I m 1km
1 cm@ lm<a) lkm(a) Iha
lcm# lm# lm#
I L I L I L
I g I g 1kg 1kg I t 1kg I t
Ig/t
Ig/t
0.039 37 0.393 70 3,280 84 0.049 709 7 0.621 371
0.155 0 10.763 9 0.386 10 2.471 054
0.061 02 35.314 7
1.308 0
1.759 755 0.879 877 0.219 969
0.035 273 96 0.03215075 2.204 62 0.001 102 3 1.102 311 0.000984 21 0.984 206 5
0.029 1666
0.583 333 33
LENGTH inches 1 inch inches 1 inch feet 1 foot chains 1 chain miles (statute) 1 mile (statute)
AREA square inches 1 square inch square feet 1 square foot square miles 1 square mile acres 1 acre
VOLUME cubic inches 1 cubic inch cubic feet 1 cubic foot cubic yards 1 cubic yard
CAPACITY pints 1 pint quarts 1 quart gallons 1 gallon
MASS ounces (avdp) 1 ounce (avdp) ounces (troy) 1 ounce (troy) pounds (avdp) 1 pound (avdp) tons (short) 1 ton (short) tons (short) 1 ton (short) tons (long) 1 ton (long) tons (long) 1 ton (long)
CONCENTRATION ounce (troy)/ 1 ounce (troy)/ ton (short) ton (short) pennyweights/ 1 pennyweight/ ton (short) ton (short)
25.4 2.54 0J048
20.116 8 1.609 344
6.451 6 0.092 903 04 2.589 988 0.404 685 6
16387 064 0.028 316 85 0.764 555
0.568 261 1.136 522 4.546 090
28.349 523 31.103 476 8 0.453 592 37
907.184 74 0.907 184 74
1016.046 908 8 1.016 046 908 8
34.285 714 2
1.714 285 7
OTHER USEFUL CONVERSION FACTORS
1 ounce (troy) per ton 1 pen nyweight per ton
Multiplied by
mm cm m m
km
cm(2) *m@ km@
ha
cm# m# m#
L L L
g g
kg kg
t kg
t
g/t
g/t
(short) 20.0 pennyweights per ton (short) (short) 0.05 ounces (troy) per ton (shoi tt)
Note: Conversion factors which are in bold type are exact. The conversion factors have been taken from or have been derived from factors given in the Metric Practice Guide for the Canadian ^fining and Metallurgical Industries, published by the Mining Association of Canada in co-operation with the Coal Association of Canada.
19
3268 ISSN 0826-9580 ISBN 0-7778-1944-9
Il''25 44"45 -I
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MAP VJ2^ft
PAI.KOZOK G K ( ) L ( K ; ^
SOUTHERN BRUCE PENINSULA
SOL rilKRN OM \RI()
11.1' ' i j
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LKGKM) PAI.KO/.OK
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12
11
10
Bass Islands Formation:Do!osione bro/vn, f ine-crysiall ine
Salina Formaiion in iefbedded gfey and brown dolostone, and green and red shale
Gueiph Formation
lOO Li ihctaces G- Bi jne'mai ao cs" '~e ^ gr ; gfey-lan \o t a i (css^tilerOLS i"&3uia"y 10 lensQ.dai Deoaec may nc^uJe L,„iC'Cjps o' oiner Gueipn Fcr'".ation i.mc'sc es
lOc L'tholaces G. Doiosione ngr: 9'C,' la^ :c orGwn taDuiai De:33ea IOCB1I> C r s i ' o n a '
Eramosa Member IOD Liif-c'acies G - D j o s t o n e siig'^^'v ! - " C J e r a t e ,
bilumincus i .gr--ar 10 gfey-'-S"^ — r e s : , c i:es tocai cnert
lOa umcrac iesG, 0:^=5:0'^^ a-^ 'a^ea - : - : :e-a i« . . IL! very Dtum,- (0_S 'CCa - ^ . - i : ; - J - r r " "V'Z-JZSZ'
(•no^ac es G. a'~ zz-^-^.c^
Amabel Formalion
Wiarton Colpoy Say Member 9c ^ ;'-C''a:-=s A_ 5 >'r^-'-a z^i'i':-
'cssi'ifft'Cus w^-e ic .y^-5 ' r , - *=-
uPduialO'i !c 'e^'Disa r j e : j ^
9D L ' tnc 'acesA- D - r s i c e A ^ ••= •: S!'ea", C'^e-g-e, T K " ea r e - - •.
Lions Head Member 9a L'^ota^res A^ D. : ;s t j "e ^'-- j - i . - ^ a "
tnin-tc iPiCH-cejtiea 3e'"5e s ; :2 : i& , fosb u!e'OL.s cca Oi^e •: w-*;. e - .:: ^s c^er* ^ o d „ e s a^t; ' " •ccsv , z 'es
Foss i l Mill F o r m a l i o n D o l o s t o n e , f o s s t l i f e r o u s
fauna commonly silicitied: local chert nodules
St. Edmund Format icn* Dolostone
Wingtield Formation, interbeddea doiosicne and shale, dolostone is thin-bedded s^^ate is grey-green
Dyer Bay Formation. Dolostone 'Qr- g re , 'z aatk grey-brown, Ihm- to m e d i u m o e o o e d . modefa te i / 'ossiiiTerous, abundant sedimentary s i 'u; ; iu 'e5
Cabol Head Formation Shale red and minor grey-green siliciclastic, with minor dolostone m-lerbeds
Manitoulin Formation Dolostone and caicareous dolostone; thin- to thick-bedded tine- to coarse-crystall ine
ORUOVIClAN
Queenston Formation Shale ^ i th mterbeds ot silt-stone and l imestone, red and grey green snicc-as-ttc Shale and sil istone non- to jery 'ossi i ' terous light lo dark grey, generally argil laceous l imestone
Georgian Bay Formation interbedded grey-green shale, tossil i ferous limestone and calcareous Silt-Stone
'vc' c e s c * ' " '» 5 -^jz f'W
S\\1U()LS
X
V
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Bedrock Outcroc
Quaffy locat.on • act've inactiu^e,
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Zinc suipr-ide (sphaieniei
^ ^ ^
v ^ * ^
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G r D : j l a
acc'--< '^•'
G- C ; j • Dc-^^'a-i' 1
occurfGnce
SOIKCKS OK INKOKMAI I' Topoyfapny Ifur'i Map 41 A, i i j ' i Df ine N^' Sysierri
Rtt-Q'os of peurj ieu'" exploratior wells f'Orri " Resources. Peiruieur^i Resource-:' Labora'G',
Mineial Deposit inventory i rc i t* ui v.e '. Deveiopmeni and Mines
MfciriL convefsion facior l 'cct - 0 304e
CKKDirs Geology by D K Arnisirong ano A S geological intarmaliun I'oni OGS dnli ' ana OGS-82-4
To ensure 'he rapid disst^niinaiicn IS unedited Discrepancies may Geological Survey does noi assm- -critical information
• --a
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• AaJiiionai OGS 90-3.
•' ih is '^•op •\ the Oniatio -, - 'lOuKT venly
44°30
•0"52
Issued 1993
InluriTialion from inis publicalior IS recommended that referenr_H
Armslrong DK i993 Paleo.' Peninsula, Southern O'" Preliminary Map P3236 ••
Ot : •' credit is given It Tia " •• 'c l owing form
16' ' ine SoLiiherr-' Biuce Geological Sun/ey
