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Ministry of Mines and 79030© 79(I00© Northern Development Minerals MARGINAL NOTES 5s ^— —y /.w j/ ( fi \ r~"- i 46r OO© ----.j, -./if f i .i i t A"--" -j and Mines Division Ontario INTRODUCTION The surficial materials of the South River (NTS 31E/14) map area were mapped during the 1988 field season. The Burk©s Ontario Geological Survey Falls (NTS 31 E/11) map area to the south was also mapped at this time. Previously mapped areas to the west and southwest include the (NTS 31E/12), Orrville (NTS 31E/5), MAP P.3160 Key Harbour (NTS 41 H/15) and Pointe au Baril Station-Naiscoot WK^- 'jH/1 vCTtt* / S River (NTS 41H/9. 10) map areas (Kor 1987), and the Parry ?Iur\ /V./VSX -**S * Geological Series Preliminary Map Sound (NTS 41H/8, 7) and Lake Joseph-Sans Souci (NTS -*-*-r f -\ 31E/4 and 41H/1) map areas (Kor and Miller 1907a. 1987b). QUATERNARY GEOLOGY Detailed mapping of the surficial deposits north (Harrison 1972), east, in Algonquin Provincial Park (Ford and Geddes Tsfy 1986), and south of the study area (Sharpe 1978) were com pleted previously. Reconnaissance physiographic studies of SOUTH RIVER AREA the region (Chapman 1975: Chapman and Putnam 1984: Mol lard 1981) and studies of the glacial and postglacial Huron ba fi^ i( ^^^(IV* s?7 '* /' v SOUTHERN ONTARIO sin lake stages (e.g., Goldthwait 1910; Antevs 1925; Kaszycki 1987; Larson 1987: Noble and Phillips 1988) supplement the Scale 1:50 000 j4fttr .f.-^.\^-l ( published maps, Metres TOGO ri i 2 Kilometres Mapping involved the interpretation of 1:15 840 scale air photos supplemented by the examination of natural sections Wile l), b 1 Mile (lakeshore and creek bank exposures), man-made sections (readouts, sand and gravel pits), lest pits and hand-augered cores. Highways 11 and 522, and numerous township roads provide access to the western portion of the map area. Log v* jrt*2s*y!***\^J ! ging, cottage and park access roads provide limited access to NTS Reference: 31 E/14 ElhhrfSC r f? \ \ the remainder of the map area, necessitating reliance on air Lola- K) ^1*^ 1-J ' photo interpretation. •ffl-z/if\n f i . *ft . \j rrj: -JL. A1 Queen©s Printer for Ontario, 1990 The authors wish to acknowledge the able field assistance Printed in Ontario, Canada of Karen Austin and Leigh Austin, and the administrative assis This map is published with the permission of V.G. Milne, Direc tance of the Ontario Ministry ot Natural Resources district staff tor, Ontario Geological Survey. in Gravenhurst.

This project is part of the five-year Can BEDROCK GEOLOGY ada-Ontario 1985 Mineral Development lONTARIO Agreement (COMDA), a subsidiary agree The Burk©s Fails area is underlain by strongly foliated, gneissic ment to the Economic and Regional Devel and migmatitic rocks of Precambrian (Middle Proterozoic) age opment Agreement (ERDA) signed by the governments which form part of the Central Gneiss Belt of the Grenville Prov of Canada and Ontario. ince, a structural subdivision of the Canadian Shield (Wynne- Edwards 1972). The Central Gneiss Belt has been subdivided 7B0 into a number of domains and subdomains with distinctive lithological, metamorphic and structural characteristics (David son and Morgan 1981; Davidson et al. 1982; Culshaw et al. 1983). The juxtaposition of the domains and subdomains are 1^9 L\) ^^#*\^L Q ^ JlSrCu considered to have occurred during deep-seated northwesterly directed ductile thrusting between about 1160 and 1030 Ma 4 2tt^^r^Si^4 (Davidson et al. 1982; van Breeman et al. 1986). The South River map sheet is underlain entirely by the Ki r\r^?^^tk^ ^ osk domain. The Kiosk domain is characterized by alternating NvVJj^4-^A^,fc/? l zones of amphibolite facies gneiss and hypersthene-bearing granulite developed from highly ilattened plutonic rocks (David son et a!. 1982). Gneisses derived from metasedimentary rocks include graphite and sillirnanite-bearing varieties (Cul shaw et al. 1983); a graphite deposit in Butt Township south of the area is an example of one such variety (Garland 1987). The weakly structured batholith, a metaplutonic body of quartz monzonite to monzonite composition, occurs in the western portion of the map area (Davidson and Morgan 1981). .^^ "^vy QUATERNARY GEOLOGY -fa**> \ ^ © * ©-^ *© ©V^i^ * T The direction of the last (Late Wisconsinan) glacial advance LOCATION MAP i: 1:1 584 000 over the region is south-southwest. In the South River area, ice -^3^1 ^-^ or 1 inch to 25 miles flow indicators, primarily striae, range between 146 0 azimuth i*** and 222 0 azimuth, averaging 172 C azimuth. Chatterrnarks and ice-moulded bedrock forms (rock drumlins, whalebacks} also 1 r^^r^- ; ^j^t-\5y LEGEND indicate ice direction. The region was deglaciated between PHANEROZOIC about 11 500 years BP, (the approximate time of the opening S^fe^^^^Sfc of the Fenelon Falls outlet south of the project area) and iS^^A^ ^SH^ QUATERNARY 10 ?00 years RP (the deglaciation ot outlets in the North Bay RECENT area to the north) (Eschman and Karrow 1985). The western portions of the map area were inundated by glacial Lake Algon YVO^^^Vr^ MODERN LACUSTRINE: beach deposits: sand, silt quin during this deglaciation. The present topography and dis /(V Jfc^-*VC\ tribution of sediment suggests that the Lake Algonquin shore f \-*J ^ -fc——^ V **"*-ta \ M line in this area consisted of an archipelago of islands, not un f rdL'fi ORGANIC DEPOSITS: peat, muck, marshlands like the present-day shore of . Veillette (1986) suggested that in the Abitibi-Timiskaming ALLUVIUM: sand, silt, organics. muck area north of the study area, the Laurentide Ice Sheet was sub divided into two lobes during deglaciation, with a major north- south suture zone along the present Highway 11 corridor. Great volumes of ice-contact and glaciofluvial sediments were deposited along this suture zone. These were subsequently GLACIOLACUSTRINE DEPOSITS: sand, silt, clay partly buried by glaciolacustrine sediments deposited in glacial Unsubdivided Lake Algonquin andjDost-Algonquin lake phases. **tM^w c^4.y 6a Deltaic, valley fill, nearshore: sand, gravel Harrison (1972) proposed that the first northern outlet ot 6b Prodeltaio, lakebottom: silt, clay; laminated, glacial Lake Algonquin opened up through the study area. In his rhythmically bedded to massive interpretation, the South River outlet is thought to have chan nelled meltwater north and east through the Smyth Creek valley. Kawawaymog Lake, Amable du Fond River to North Tea Lake GLACIOFLUVIAL OUTWASH DEPOSITS: outwash and valley fill; sand and gravel and beyond to the Petawawa River. Further ice retreat opened ^ TSE/^^CXX: the Genesee outlet, just north of the study area, in part diverting flow west of Kawawaymog Lake northward, through Genesee ICE-CONTACT DEPOSITS: leeward and valley fill Lake to the Upper Petawawa River. The present study and ob w^n ^sMfc* (variable) servations made by Ford and Geddes (1986) suggest that fluvial A \ l Y 4 Unsubdivided activity through these systems was not as great as would be -^A/l©l 4a Eskers. kames, valley fill, hummock mounds; required by Harrison©s hypothesis. Smyth Creek valley is sand, gravel, till choked by ice-contact esker-kame complexes, indicating that -cr* x^©^f "i ~^P 4a'^L-K, 4b Subaquatic outwash fan deposits; sand, although the sill west of Kawawaymog Lake may have been at an gravel, minor silt and ciay appropriately low elevation to initiate eastward drainage, stag Cf-9. ;j*KOv*^ nant ice probably blocked the valley and therefore prevented Ac Ice-contact sediments overlain by ;^1 m drainage through this route. It is probable that the valley system glaciolacustrine sediments; sand, gravel, with was an embayment of glacial Lake Algonquin. but that eastern silt, clay and sand cap drainage of the lake commenced only once ice retreated north ^kP©-W- ;©^9MW^T-v.©" V **©JlZSv of the Trout Creek area. Lake Algonquin, having reached the TILL: generally ;*1 m thick; leeside and meltout till; Main Algonquin level, was then drained rapidly through a number i^te&fe^/- ^ loose, stony sand matrix; minor supraglacial of outlets, notably the Genesee. Fossmill and North Bay outlets. t ^ VVrY/ and lodgement till; compact, clast poor, silty until the low Hough phase was attained in the Huron basin. At this b t vtf^rV/ sand matrix time the map area was exposed subaerially for the first time ^^ '^^^f^^^^im since deglaciation. BEDROCK-DRIFT COMPLEX: thin, discontinuous The map area can be divided into two physiographic units. A drift; ^0 percent cover; local pockets of relatively low relief terrain, dominated by thick accumulations of deep drift sediment, occurs in the western one-third of the map area, The 2 Unsubdivided eastern two-thirds of the map area is a more rugged highland ot b . ( r^UX?Sr4 Vi \,V mK 2a Till moderate to high relief incised by deep, narrow valleys. The dis ( ZSS r sT^ J*\ 2b Stratified sediments cover: gravel, sand, silt tribution and thickness of glacial drift varies greatly within these VLAt .A/XI M,-v and clay (glaciofluvial and glaciolacustrine ori units. The low relief terrain is underlain by thick complexes of gin} ice-contact and glaciolacustrine sediment which effectively mask the character of the underlying bedrock topography. Drift- UNCONFORMITY covered bedrock knolls regularly protrude from this sedimentary blanket. The rugged highland bedrock terrain, and generally all PRECAMBRIAN areas above 405 m elevation, consist of extensive bedrock-drift complex and areas of thick (^ m) till. The till in these areas generally does not mask the character of the underlying bedrock ^ 'J J ,J \(W/ i ^^.vriy-xP-—ra\fcJ\ \ ftf-f f fa© -xr^v\ BEDROCK: ridges, knobs; ^0 percent exposure; topography, though extensive bedrock exposure is not com m SV""-- 3 /(t-v.-- tfyx/--©. thin, discontinuous drift, with local pockets of mon. The narrow bedrock valleys often contain thick accumula deep drift; unsubdividod granitic to mafic mig tions of ice-contact and glaciofluvial sand and gravel. tffa "-^4C^--' :-:--~--\ matite and gneiss * in pase of multiple modifiers, the order of the modifiers indicates the ^b^.^-'/',"- "—" ^-^N abundance o! the material types within the map unit: e.g., 2ba- BEDROCK-DRIFT COMPLEX strstified sediment more abundant than til!. The map area is dominated by bedrock-drift complex (map unit 2). Bedrock outcrops frequently protrude from the thin ^1 m) mantle of drift, but seldom occur at a mappable scale (unit 1). SYMBOLS Till is The primary surficial material in the complex (unit 2a). The Geologic boundary Abandoned till is generally loose and stony, with a grey sand matrix. Thin (approximate) (raised) terrace deposits of ice-contact stratified drift, glaciofluvial outwash and glaciolacustrine sediments (unit 2b) occur on oedrock knolls as Glacial striae Abandoned sociated with more extensive deposits of similar type. The ex meltwater channel tensive, dense vegetation cover in the eastern upland areas make interpretation of the airphotos difficult. Units 2a and 2b are Moraine Gravel pit differentiated on the basis of vegetation density and type, topo graphic location and sediment association. Small pockets of thicker sediment M m) also occur throughout the bedrock-drift ^;^#ys3as Esker Roche moutonnee complex. These are generally not mappable at a scale of 1:50 000, or could not be identified through airphoto interpreta Kettle, ice-contact slope tion. IK7 79"00© Joins 3 IE/11 TILL SOURCES OF INFORMATION broad Smyth Creek valley, trending roughly south through the lake phases resulted in the deposition of the deltaic sediments. Main Algonquin lake phase in the area (Harrison 1972, Fig Garland, M,L 1987, Graphite in the central gneiss belt of the Mollard, D.G. 1981. Southern Ontario engineering geology Till is the dominant deposit in the South River area. A thin till RECENT DEPOSITS REFERENCES Base map derived from Map 31 E/14 (South River) of the Na mantle dominates the eastern upland area (unit 2a), but thicker centre of the map -area. Feeding the Smyth Creek system are The subaquatic fan deposits may be quite extensive beneath ure 16). Proglacial ponds above this limit produced sandy de Grenville Province of Ontario; Ontario Geological Survey, terrain study, data base map, Sundridge.iSlE/NW; Ontario Extensive alluvial deposits (unit 7) occur along the South River Antevs, E. 1925. Retreat of the last ice sheet in Eastern Canada; tional Topographic System. deposits (unit 3) commonly occur in bedrock saddles, leeward several lesser system©s of ice-contact and glaciofluvial material this glaciolacustrine cover, but the lack of topographic and to posits in the Sausage Lake, Smyth Creek valley and Open File Report 5649, 222p. Geological Survey, Open File Report 5319, 2p. emanating from higher ground to the east. These deposits are and in minor river and creek valleys where older glacial deposits Geological Survey of Canada, Memoir 146, 142p. positions and under glaciolacustrine deposits. A single till sheet nal expression of these deposits on airphotos makes it difficult Kawawaymog Lake areas. Glaciolacustrine sediments are sub Goldthwait,© J. W. 1910. An instrumental survey of the Noble, T.W. and Phillips, B.A.M. 1988. Earth science theme Aerial Photographs: Ontario Ministry of Natural Resources, with two distinct facies is recognized. The dominant facies is generally confined to narrow bedrock valleys trending west- to estimate their true extent. Subaquatic fan deposits are iden divided into: 1) nearshore and deltaic sand and minor gravel were available for reworking. Accumulations of organic debris Chapman L.J. 1975- The physiography of the Georgian Toronto, and National Airphoto Library, Ottawa. (unit 8) shorelines of the extinct lakes Algonquin and Nipissing in study: glacial and contemporary landforms: Consultant©s bluish grey, loose, stony (10 to 30 percent clasts by volume), southwest at regular intervals of roughly 4 km. In the interpreta tified where extraction operations have excavated through the (unit 6a); and 2) offshore silt and clay (unit 6b). Sections within occur in broad depressions on the glaciolacustrine de Bay- Ottawa Valley area of southern Ontario; Ontario Division posits in the western lowlands, and in innumerable small bed southwestern Ontario; Geological Survey of Canada, Report to Ontario Ministry of Natural Resources, Parks and Geology not tied to surveyed lines. and has a sandy matrix. Sandy lenses and stringers occur tion of airphotos, the ice-contact deposits are differentiated upper glaciolacustrine cover (unit 4c). deltaic deposits exhibit planar-, ripple- and cross laminated of Mines, Report 128, 33p. rock depressions and lineaments in the eastern uplands. Mod Memoir 10. 57p. Recreational Areas Branch, Northeastern Region, Sudbury, throughout the till, particularly in association with larger clasts from glaciofluvial outwash deposits by their hummocky topogra sand and fine gravel, usually flat-lying to gently dipping to the Chapman, L.J. and Putnam, D.F. 1984. The physiography of Contour interval: 50 feet ern lacustrine deposits (unit 9), such as beaches and other Harrison, J. E. 1972. Quaternary geology of the North Ontario, 73p. and at the drift-bedrock interface. Occasionally, a more com phy and dense vegetation pattern. south and southwest. The upper surfaces of these deposits southern Ontario, third ed.; Ontario Geological Survey, GLACIOFLUVIAL SEDIMENTS wave-reworked sediments, were noted in mappable quantities Bay-Mattawa region; Geological Survey of Canada, Paper Sharpe, D.R. 1978. Quaternary geology of the Gravenhurst, Magnetic declination approximately 11"09©W in 1988. pact, clast-poor (-c10 percent by volume), slightly fissile till Two distinct east-trending ridge-shaped deposits in the usually lie below the expected Main Algonquin level, and are Special Volume 2. 270p. therefore interpreted to represent post-Algonquin regressional on Eagle Lake. 71-26, 37p. Bracebridge and Huntsville areas. District Municipality of facies was observed on the stoss (up-ice) sides of bedrock northwestern portion of the map area are interpreted as small Glaciofluvial outwash deposits (unit 5), primarily medium- to Culshaw, N.G., Davidson, A. and Nadeau, L. 1983. Structural Metric conversion factor: 1 foot - 0.3048 m. lake levels. No distinct wave-cut terraces were observed in the Kaszycki, C.A. 1987. A model for glacial and proglacial Muskoka; in Summary of Field Work. 1978, Ontario walls. Bullet-shaped clasts and stringers of sorted sands are moraine remnants. Several kilometres long and completely cov coarse-grained sand and minor gravel, occur in abundance subdivisions of the Grenville Province in the Parry map area. sedimentation in the shield terrane of southern Ontario; Geological Survey, Miscellaneous Paper 82, p.152-154. common in this facies. The till was deposited by melt-out from a ered by a mantle of glaciolacustrine sand, these features occur along the bedrock valley systems in the eastern upland area. ECONOMIC GEOLOGY Sound-Algonquin region, Ontario; in Current Research, Part debris-rich basal zone under stagnant ice conditions (Shaw in the saddle between two bedrock upland sites and are dis They are associated with ice-contact deposits, being distin Glaciolacustrine fine-grained deposits, primarily grey silt Canadian Journal of Earth Sciences, v.24, p.2373-2391. Shaw, J. 1982. Meltout till in the Edmonton area, Alberta, CREDITS Quality aggregate deposits are abundant in the area, with nu B, Geological Survey of Canada, Paper 83-1B, p.243-252. 1982). Deposition by lodgement may have been a factor in the sected by the South River. They may be correlated to the guished from them on the airphotos by their relatively flat sur and red clay rhythmites, occur sporadically in depressions in the Kor, P.S.G. 1987. Quaternary geology of the Parry Sound area; Canada; Canadian Journal of Earth Sciences, v.19, merous sand and gravel pits in the Highway 11 corridor. These Davidson, A. and Morgan, W.C, 1981. Preliminary notes on the Geology by P.S,G. Kor, R.J. Delorme and assistants, 1988. formation of the clast-poor till facies. Supraglacial and flow till Genesee Moraine (Harrison 1972) lo the northeast. Striae north face and open vegetation cover. The outwash may be punctu glaciolacustrine basin area, Less than 100 rhythmites are com in Summary of Field Work and Other Activities 1987, p.1548-1569. operations generally exploit ice-contact (subaquatic outwash geology east of Georgian Bay, Grenville structural province, facies are also present as a minor component of the till sheet, of this moraine indicate a southeasterly ice flow (Harrison 1972). ated by kettles and occasionally display small terraced fans at monly encountered at any one site. Antevs (1925) describes a Ontario Geological Survey, Miscellaneous Paper 137, van Breeman. O., Davidson, A., Loveridge, W.D. and Sullivan fans and small kames) and glaciolacustrine delta deposits. Ice- Ontario; in Current Research, Part A, Geological Survey of Every possible effort has been made to ensure the accuracy of and occasionally intercalated with glaciolacustrine sediments. This suggests, using Veiilette©s (1986) model, that the ice which their southern extremities where a broadening of the-enclosing 19 m section near Trout Creek which contains almost 320 rhyth p,377-379. R.W. 1986. U-Pb zircon geochronology of Grenville contact deposits contain fine-grained and oversize material that Canada, Paper 81-1A, p.291-298. the information presentee on this map; however, the Ontario The till is commonly deeply weathered. formed the moraine represents the western lobe of the sutured bedrock valleys caused a loss of competence of the deposi mites, although it is apparent that many more were destroyed in fectonites, granulites and igneous precursors, Parry limit quality and pose processing restrictions. The occurrence of Kor, P.S.G. and Miller, M.J. 1987a. Quaternary geology of the Ministry of Northern Development and Mines does not assume ice mass. tional waters. A large fan north of Forest Lake displays a num narrow zones of disturbance throughout the section he de Davidson, A., Culshaw, N.G. and Nadeau, L. 1982. A Sound, Ontario; in The Grenville Province, Geological numerous bedrock exposures throughout the ice-contact and Parry Sound area, District of Parry Sound; Ontario any liability for errors that may occur. Users may wish to verify Ice contact ber of terraces related to waning flow in the channel. The sedi scribes. Antevs (1925} and Sharpe (1978) contend that the Tecto metamorphic framework for part of the Grenville Association of Canada, Special Paper 31, p.191-207. ICE-CONTACT SEDIMENTS subaquatic outwash fan deposits (unit 4b), glaciolacustrine deposits hampers operations and makes it diffi Geological Survey, Preliminary Map P,3102, scale critical information; sources include both the references listed usually overlain by deltaic sand and gravel and fine-grained ments represent proglacial meltwater channels active during rhythmites represent annual varve deposition, indicating a chro Province, Parry Sound region, Ontario; in Current cult to calculate reserves. It is likely that more extensive ice- 1:50 000. Veillette. J. J. 1986. Southwesterly ice flows in here, and information on file at the Resident Geologist©s office Ice-contact deposits (unit 4) occur in abundance in the structur glaciolacustrine sediments, were identified in shallow basins the retreat of the glacier to the northeast. nology of about 800 years for glacial Lake Algonquin, The rhyth Research, Part A, Geological Survey of Canada, Paper contact deposits occur beneath the glaciolacustrine cover in the 1987b. Quaternary geology of the Lake Joseph-Sans Abitibi-Temrscamingue: implications for the configuration and the Mining Recorder©s office nearest the map area. ally controlled bedrock valleys in the eastern uplands, and be along the Highway 11 corridor. The fan sediments consist of mic sequences commonly grade upwards to a greyish-red, 82-1A, p.175 190. western part of the map area. The loose, stony, sand till is a Souci area, District of Parry Sound and District Municipality of the late Wisconsinan ice sheet; Canadian Journal of neath glaciolacustrine sediments in the low-lying western por laminated silts, sands and fine gravels, commonly deformed massive, blocky silt-clay. These fine-grained sediments are oc Eschman, D.F. and Karrow, P.F. 1985. Huron basin glacial Issued 1990 GLACIOLACUSTRINE SEDIMENTS source of local borrow material or granular base in areas of lim of Muskoka; Ontario Geological Survey, Preliminary Map Earth Sciences, v.23, p.1724-1741. tions of the area. Small kame mounds of stratified sand and by loading and dewatering, with associated massive sand and casionally folded and faulted. A thin unit of planar to ripple-lami lakes:, a review; in Quaternary Evolution of the Great Lakes, ited drift. P.3103, scale 1:50 000. Information from this publication may be quoted if credit is gravel are associated with short, narrow, steep-sided eskers, diamict flows. They are believed to have been deposited sub- The western one-third of the map area is" dominated by gently nated sand and fine gravel generally caps the fine-grained se Geological Association of Canada, Special Paper 30, Wynne-Edwards, H.R. 1972. The grenville province; in often occurring in braided complexes with intervening kettles glacially or near the ice margin by glacial meltwaters debouch rolling lowland terrain composed of sand, silt and clay of quence. The silts and clays represent distal and quiescent lake p.79-93, Larson, C.E. 1987. Geological history of glacial Lake Algonquiri Variations in Tectonic Styles in Canada, Geological given. It is recommended that reference to this map be made (unit 4a), The eskers are composed of gravelly sand with a high glaciolacustrine origin (unit 6). Glaciolacustrine deposits are conditions during the Main Algonquin and early and the upper Great Lakes; U. S. Geological Survey, Association of Canada, Special Paper No.11, p.264-334. in the following form: ing into glacial Lake Algonquin. Glaciolacustrine sedimentation post-Algonquin Ford, M.J. and Geddes, R,S. 1986. Quaternary geology of the boulder content. Where the bedrock valleys broaden and termi commonly confined by bedrock uplands and generally occur phases. Bulletin 1801, 36p. Kor, P.S.G. and Delorme, R.J. 1990. Quaternary geology of in Lake Algonquin subsequently draped the fan sediments. The Algonquin Park area; Ontario Geological Survey, Open File nate, small kettled fans of sand and gravel mark the abrupt loss below about 405 m elevation, the upper projected limit of the the South River area; Ontario Geological Survey, drainage of surface meltwaters into lowering post-Algonquin Report 5600, 87p. of energy of the depositional waters and attest to the melting of Preliminary Map P.3160, scale 1:50000. ice blocks within the sediment. A major system of kettled ice- contact and associated glaciofluvial sediment occupies the