KAKWA RECREATION AREA: NORTHEASTERN BRITISH COLUMBIA GEOLOGY AND RESOURCE POTENTIAL (93H/15, 16, 931/1, 2) By J. Pell, .J.L. Hammack, B. Fletcher and W.D. Harris Geological Consultants
KEYWORDS: Regional geology, Kakwa Recreation Area, Parks and Willmore Wilderness .Area in Albert;, The .ire#IS resource assessment. stratigraphy. coal, dimension stone, quite remote and access is generally on lhmeb sk,011 bat, phosphate,lead-zinc barite, mineral potmtial. or by helicopter or float plane. .!,I old lorging road, ahg the McGregor River valley, leads to the s~then and west- ern edge of the recreation area ;lrd an extensi, n leads l,rllo INTRODUCIION the area: however, wash-outs along this road I ave mad? it The Kakwa Recre.rtion Area encompasses approximately impassable to vehicles. Trails suit~rble fordirt t ikes ald 2111- 128 000 hectare's ( 2x0 km') of wildernesh land imme- terrain vehicles lead into the nurtheaster~par of the mea diatelywest of the Albertaborder and approximately from Shelman Meadows, in Alberta. 70 kilometres north of the town of McBride, British Colum- Relief in Kakwa is considerab~.:.with clevat ons rmgir,g bia. at latitude S4"OI)' north,longitude 120"20' wcst (Fig- from lessthan 915 metres (3000 feet) ir the larvis Creek ure 1-6-1). It is thcnorthernmost parr of acontiguous, valley, alongthe western eclp,: of the ar :a, tc c','t:r northwest-trendirlg belt of parks and wilderness areas that 3050 metres (IO 000 feet) at Mourlt Ida (3190 n )and WOIIII~ includes Yoho N;ltion;rl Park and Mount Robson Provincial Sir Alexander (3275 m). Much of the terrain s ver) sleep Park in British Colwnbia. and Banff and Jasper National and cliffs are common. There arc: .arge icefield near Wollrt 66 wy Brunch Geolo~iculFieldw,vk 1991, Puper 1992-1 Ida. Mount Sir .4lexander and Mount Dimsdale and along In theIntersection Mountain area, rocks of the Miette the northwestern boundary of the recreation area. Group include a well-bedded, cliff-forming unit consisting There has been very little exploration work in Kakwa, in of medium orange-brown-weathering, dark grey, calcareous part due to itsremoteness. Thereare coal leases in the quartzite-granuleconglomerate and quartz wacke with northeastern part of the region and some oil and gas permits interbedded medium to dark grey phyllite. This unit is were also held there in the early 1980s. Quartzite, near the underlain by a thick, poorly exposed,dark grey phyllite. centre of the region, has been examined for its potential as a building stone. A lead-zinc-barite showing is located a few LOWERPALEOZOIC kilometres north of the recreation area and a gypsum pros- pect a short distance to the southeast. Although there has Lower Paleozoic strata underlie a significant proportion been limited activity, the geology indicates that a number of of Kakwa Recreation Area (Figure 1-6-2) and comprise a potentially economiccommodities could existwithin the conformablesequence thatdisconformably overlies Pro- boundaries of the recreation area, including coal, phosphate, terozoicrocks. TheLower Cambrian Cog Group, which gypsum,lead, zinc,barite and dimension stone. Kakwa formsthe base of this succession, consists of the RecreationArea is currentlyunder consideration for McNaughton. Mural and Mahtoformations (Table 1-6-1). upgrade to Class "A" parkstatus and, prior to its The McNaughton Fonnation is a resistant,rusty to dark- reclassification. the mineral potential of the area must be weathering unit that forms a thick and fairly monotonous evaluated, which is the focus of this project. sequence dominated by medium to thick-bedded light grey quartzites.These quartzites areoften laminated or GEOLOGICAL SETTING crosslaminated: thinblack shalelayers and granule to pebble-conglomerate beds are present locally. In some areas Kakwa lies within the Foreland tectonostratigraphic divi- crosslaminationsare stainedpinkish, giving the rock an sion of the CanadianCordillera and is underlainby a attractive banded appearance. In the area south and west of sequence of carbonate and clastic sedimentary rocks rang- Wishaw Mountain, black siltstones and argillites are inter- ingfrom Late Precambrian to Early Cretaceous in age. bedded with the quartzitesand locally form units tens of Folds and southwest-dipping, northeasterly directed thrust metres thick thatcontain thin quartziteinterbeds. The faults are the dominant structuresin the region. Major thrust McNaughtonFormation is largelydevoid of fossils: sheets contain strata which generally young to the northeast. however, trace fossils such as worm tubes (Scolithus) and Previous work in the area includesregional mapping by meandering patterns on bedding planes, suggestive of worm Campbell, Mountjoy and Young (1973), McMechan (1986). trails, occur in theupper parts of theunit. In the Kakwa McMechanand Thompson (1985) andTaylor andStott area, the McNaughton Formation is estimated to be approx- (1979). imately 1500 metres thick (McMechan, 1990 Slind and Perkins,1966). STRATIGRAPHY The Mural Formation is a reddish brown. recessive unit UPPERPROTEROZOIC (HADRYNIAN) predominantlyconsisting of silty andsandy dolostones, dolomitic quartzites, shalesand minor limestone. Its contact Rocks of the Hadrynian Miette Group are exposed in the with the underlying McNaughton Formation is gradational hangingwall of the Mount St. George fault in the Moonias and consists of a zone of interbedded light grey quartzites, Mountain area; the Snake Indian and Wishaw faults near dolomitic quartzites and dolostones. The Mural Formation Intersection Mountain; andthe Mount SirAlexander and begins wheredolomitic rocks dominate over quartzites. Wishaw faults south of Wishaw Mountain (Figure 1-6-2). Orange to tandolostones, dolomitic quartzites and grey Only theupper parts of thisunit areexposed withinthe quartzitescharacterize the lower part ofthe formation, study area and detailed observations were possible only in while grey and greenish grey shales, grey crystalline lime- the Moonias Mountainand Intersection Mountain areas. stones. dolostones and lesser amounts of quartzite are more AtMoonias Mountaintwo lithologicunits were common in the upper part. Dolomitic quartzite beds often observed.The lowestcomprises a relativelyresistant, grade up-section intosandy dolostones. Scolirhus worm thicklybedded, medium brown weathering quartzite- tubes are common in thesandy layers (Plate 1-6-1). This granule to pebble conglomerate, quartz wackeand medium formation is 225 to 300 metres thick in the Kakwa region. greyquartz arenite, interbedded with brownand grey- The Mahto Formation is a grey to maroon, resistant unit, weathering argillite andminor light grey quartzarenite. overlying the recessiveMural Formation. In the Kakwa area Minimum thickness for this unit is 300 metres. The con- it is approximately 300 to 350 metres thick. It consists of glomerate is composed of well-rounded quartzite pebbles lightgrey to creamy beige,pink and maroon, medium to supponed by amatrix of medium-grained, poorlysorted thick-bedded quartzites with minor amounts of interbedded quartz wacke. This lower unit is overlain by in excess of brown and dark grey sandy shales, dolomitic quartzites and 200 metres of thinly bedded, dark brown-grey argillite with siltstones. As with the other units of the Gog Group, fossils thinsilty interbeds. Siltybeds are locally crosslaminated are restricted to Soolithrrs worm tubes. Quartzites are gener- and show graded bedding. Onethick unit within the argillite allyfine to coarsegrained and, locally, granule- hasabundant tat-weathering dolostone breccia blocks of conglomerate layers are present. Colours of the quanzites probableolistostromal origin. These blocks are up to 6 vary from solid greys, pinks and maroonsto very attractive, metres in diameter and stand out in relief against the more intricately swirled and banded patterns in shades of maroon, recessive argillite. pink and creamy white (Plate 1-6-2).
68 Brirish Columbia GeoloRicul Survey Branch TABLE 1-6-1 TABLE OF FORMATIONS
LOWER CRETACEOUS Gates Fm: 12-1 10 m) sandstone. carbonaceous shale, coal (Middle and Torrens River members, in descending order) Moosebar hn: (550mi shale, minor sandstone BULLHEAD GROUP Gething Fm: (25-UO m! sandstone. sillstone. coal Cadomin Fm (t25 m) conglomerate ~- unconhrntity __ MlNNES GROUP Gorman Creek Fm: 1650-1000 m! sandstone. siltstone. minor cwal UI'PER JURASSIC AND LOWER CRETACEOUS Monteith Fm 1200-400 m) sandstone, dtslone. shale JL RASSIC Fernie Fm: (250~900m) shale. silly sandstone, siltstone -_ unconfonnity __ -.~ TIIIASSIC SPRAY RIVER GROUP Whitehorse Fm: l130~400m) dolustone. limestone, evaporites (Winnifred. Brewster and Starlight evaporite members. in descending order) Sulphur Mountain Fm: (405~475mi dtstone, silty limeslone (Llama. Whlstler and Vega-Phrusu memhen. in descending order)
PERMIAN Mowich Fm: It IO m) sandstone, conglomerate at base Belcoun Fm: (>IO m) limestone, conglomerate at base
UPI'ER CARBONIFFROUS Haninglnn l'm: (0-5 m) limestone wibasal pebble conglomerate
- unconfonnity ~ -.__. L'IWER CARBONIFEROUS RUNDLE GROUP 12400 m) limestone, dlrloslone (Mt. Head. Turner Valley. Shunda & Prkisko formations. in descending order) UPPER DEVONIAN AND LOWER CARBONIFEROUS Exrhaw & Ran11 fmr: IIHOL2M) m) rhale, minor limestone
~~ ""c""f0rmity UPPER DEVONIAN Palliser Fm: I1530 m) limestone Ifossil-poor1
. Flume Fm: 175-145 m) limestone, slromalopomid biostrome - unconfmniry __ MIDDLE DEVONIAN Dunedin Pm*: (160 m) limcstonc, svltwme. conglomerate " unconf<,mity __ MIDDLE ORDOVICIAN Unnamed unit': l>75 mi dolostone. quamite and limestone Skoki Fm: II I0-3XC m) dolostone. minor limestone LOWER ORDOVICIAN Monkman quartzite: (30-75 ml quanrite, dolomitic quartzite Survey Peak Frr: l45llb600 mi silty dolostunc. limestone, shale LPPER CAMBRIAti LynxFm: MIDDLE CAMBRIAN Arctumvs Fm: Pika i;: Eldon Fm: Snake Indian Fm: LOWER CAMBRIAN COG GROUP Mahto Fm: 1300-350 m) maroon. pink. grey quartzite, dolastone Mural Fm: 1225-300 m) duloslone. quartrile. limeslone, shale McNaughton Fm: I? IS00 ml quartzite, granule conglomerate
" unconformity ~ llPPER PROTEROZOIC P!ate 1-6-1. Subvertical Scolirhru worm tubes in Lower Plate 1-62, Intricately swirledcolaur-handing patterns Cambrianquartzites *ithin the Mural Fornmation.Section in Lower Cambrian Mahto Formation quartzites. Banding vicwed is perpendicular to bedding. parallels solution fronty. Symhol indicate? bedding orientation.
The Middle Cambrian Snake IndianFormation is areces- 100 metres of ribbed-weathering strata of the Pika Forma- sive to ribbed-weathering unit with colourful banding in tion. shades of tan, red, green and grey, and overlies the Mahto Formation quartzites(Plate 1-6-3). The lower part of the In much of the area. the base of the Pika Formation is formation is more recessive and tan weathering; it consists placedat thebase of a yellow-orangedolostone unit of thin-bedded re,d, green and greyshales, with tan-coloured between the massive Eldon limestones and the overlying, dolostone, silty limestone layers and minor sandstone inter- wavy, thin to medium-bedded lime mudstones. These lime- beds. lhe upper part of the formation is ribbed weathering, stonesare commonly bioturbated, locally contain dol- with thick resistant grey limestone units separated by reces- omitizedworm burrows and aresometimes interbedded sive bands of brightly coloured shales and thinly interbed- with thin grey shales. In the Mount Sir Alexander area, the ded dolostones. The limestones are variably thin to thick Pika Formation consists of two distinctive units. The lower bedded, wavy bedded to nodular and commonly show evi- unit comprisesan orange to buff-weathering.recessive of medium grey lime mudstone, that commonly dence of bioturbation, with dolomitiLed burrows. The topof sequence the fonnation is marked by the last thick, recessive, brightly contains dolomitized laminae and worm burrows. The top coloured shale and dolostone (Mountjoy and Aitken. 1978). of the lower sequence is marked by approximately 5 metres Inthe Kakwa area, this formation is approximately of interhedded grey-brownto orange-brown argillite and Ann metrec thirb grades into an upper, massive, more resistant unit compris- -.. .1..-l.. _"",..._.. ing medium to light grey, laminated lime mudstones that are Massive,cliff-forming, dark grey limestones of theEldon locally oolitic and display lode graded beds and Formation overlie the Snake Indianshales and carbonates crosslaminations. (Plate 1-6-3). These limestones varv from thin bedded and nodular to thick beddedand oftenare bioturhated, with The top of the Middle Cambrian sequence is marked by dolomitized wormburrows and beds a commonfeature the Arctomys Formation, a distinctive,red-weathering (Plate 1-6-4). Thedominant lithology is lime mudstone, recessive unit. SO 10 100 metres thick. It comprises blood- however, oolitic grainstones also occur locally. The Eldon red and minor amounts of dark green dolomitic shale and Formation is approximately 350 to 375 metres thick in the silty shale and thin bedded, tan-weathering dolostone. Mud Kakwaarea and is overlainby approximately 80 to cracks. salt crystal casts and ripple marks are common.
70 British Columbia Grolo~iculSurwy Branch Plate 1-6-3. The exposed Cambrian section on the CdSl flank of Mount St. Patrick, as viewed from tht southeait. Th lowest un't exposed is the masxive, cliff-forming Lower CambrianMahto Formalion (cMh) which is overlain by thf: n:cessivt Midd e Cambriall lower Snake Tndiar Formation (cSII). The colour-handed and slightly rihbed-weathering upper Snake Iridian iormttion :Slu) fbnns the next cliff slep .~ndis overlain by a cliff-forming ledge of Ihe Middle Cambrian Eldon Formation :cE). Recessive .trata (sf th: Middle Cambrian Pika and Arclomys fo~mations(cPA) form the next step and the uppermosl ledge, seen only lr the t tr uppu I,:li corner of the photograph, is cliff-forming Upper Cambrian Lynx Formalion (r:Lx).
The Upper Cambrian Lynx Formation is a resistant, cliff- The Lower Ordovician Survey PeakFormal on is :I rfxist- forming unit that crops out at thepeaks ofmost of the ant unit that conformably overhe!; Upper Cam rian stra.t,a.11: highest mountair~sin the area and is characterized by well- is 450 to 600 metresthick anc has aIlprox mately 30 tn defined huff andgrey colour-handing and bedding (Plate 70 metres of recessive,light greenish gr y to sil\t:ry 1-6-5). It confonnatdy overlies recessive shales of the Arc- weathering, strongly cleaved, c;~lcareous sha e and sluley tomys Formation ard is estimated to be 600 to 800 metres limestone with interbeds of limey flat-Ixbble conglomerate thick (McMechan, ! 986). The lower part of this formation at its base. Burrows and feedin)!. traces on b :dding plane!; consists of medium-bedded, buff, grey and locally orange- are locally very common. The remainder of he unit ,: Nom.. weathering, very line grained dolostones with interbeds of prises resistant, buff to orange-\r,eathen.rig. si1 y dolostames, fine to coarse-grainc:d quartz arenites and sandy dolostones, dolomiticsiltstones and blue-grey-wearherir g limmt'ones. light grey siltstooes and minor, medium-bedded, grey lime- Greyargillite partings are c~xnmonin thi i part of the stones. The sandstonesare often crossbedded and may con- sequence and flat-pebble conglomerates areF .esent loc;ally. tain dolostone chi JS (Plate 1-6-6). Thedolostones are The siltstones and dolostones ;arc wavy bedd :d and hwe a locallystromatolitic and characterized by sedimentary very rough weathered surface, with more res stant, whi!;p!r structures such IS layers of flat-pcbble conglomerate, bur- laminae. They are interbeddesi with silty, t ]in-betid~zito rows, lode casts, slilmp folds and disrupted bedding. Beds massive limestones that are ge?t:rally nr~dula~to wavy Ixd- containing nodules of white chert are also present locally. ded and can be partially dolo~n~tized.Eioth I le dolost~me:j The upperpart of the Lynx Formation is dominated by and limestones locally show evidence (of biot lrbation, ~;~x- limestone. Its base is marked by 50 to 100 metres of rela- taining burrows and feeding trds that are : me times ril- tivelyrecessive, greenish grey to grey-weathering cal- icified. Some layers arerich in fossil detmris; b .achiopo'd :mi careous argillite with limestone nodules. Thisis overlain by trilobite fragments are commnn tan to grey-wealhering.wavy bedded to nodular, The SurveyPeak Formation is ovel.lain ,ythe Lrwer argillaceous or silt!! limestones with thin to thick beds of Ordovician Monkman Quartzite Formalion. ' 'be Monkman more resistant grey limestone. is a resistant, light grey weathering marker mit that wer-
Geological Fieldwork 1991, Paper 1992-1 71 ages between 30 and 100 metres thick and comprises fineto bedded, medium to light &reyand orange-weathering, fineiy medium-grained, thin-bedded tomassive, light grey to buff- crystalline dolostone.True thickness could not be deter- weatheringquartzites and dolomitic quartzites. Crosshed- mined but is not less than 75 metres. ding,ripple crosslaminations and burrows are common features. MIDDLEPALEOZOIC Middle Ordovician strata, assigned to the Skoki Forma- tion, overlie the Monkman quartzites. The Skoki is a resist- The middle Paleozoic sequence in the Kakwa area is ant, tan-weatheringformation characterized by monoto- dominated by carbonate rocks exposed in athrust sheet nous, mediumto thick-bedded, finely crystalline which is bounded on the east by the Broadview fault and on dolostones.For the mostpart, the dolostonesare rather the west by the Mount St. George and Wishaw faults (Fig- featureless, however,locally they can contain oncolites, ure 1-6-2). stromatolites, intraclasts, mud cracksand rare chert nodules. The lowest unit in the middle Paleozoic package is the the Minor amounts of wavy bedded to nodular limestone are Middle Devonian Dunedin Formation which disconforma- present in this formation and gastropods are found locally. bly overliesOrdovician strata. It is exposedat only one Thick-bedded, crosslaminated, sandydolomite horizons can location within the study area. approximately 3 kilometres also occur. south of MountBuchanan (Figure 1-6-2) where it is esti- The youngest LowerPaleozoic rocks observed in the mated to be approximately 60 metres thick (McMechan and Kakwa areaare an unnamed unit composed of medium- Thompson, 1985). It is Characterized bytwo distinct bedded to massive dolomitic quartz arenite and dolostone. lithologies, an upper,resistant limestone-dominated pack- This unit was mapped in the Mount Buchanan area where it age and a lower. less resistant sequence dominated by clas- conformably overlies the Skoki Formation (Figure 1-6-2). tic rocks.The upper package consists of thick-bedded, Medium-beddedto massive, medium to light grey,fine- mediumgrey and yellow-buff-weathering,medium grey grained dolomiticquartz arenite predominates and has a lime mudstones and wackestones with minor interbeds of distinctivemedium yellow-tan tobuff-orange weathered medium orange-brown weathering, light grey, fine-grained surface. This sandstoneis locally interbedded with medium- quartzarenite andsiltstone. The lowerclastic sequence
72 British Columbia Grological Survey Brunch Plate I-6-:i. Thc Cambrian and Ordovician section exposed at Mount Ida. as viewed from Jarvis L&es. The main , liff-formine unit, that comprise!. the bulk of the mountain, is the Upper Cambrian Lynx Fonndtion (cLx); it is overlain '5y more rcces ive str.tta(ti the Ordovician Survey Peak Formation (oSP). which cap the mountain. Recessive strata of the Middle Cambrian Arcton ys and Pika formations (cP/\) that underlie Lynx stratd, arc poorly exposed, outcropping on the small spur between th~two icefields The Mliddlc Cambrian Eldon Formation (cE) fonns the lowest cliffs, immediately above the scree slope.
consists of mediumorange-brown weathering, fine to ing shaley limestones generallyy Form a dark :rey wea.ther.- coarse-grained,light grey quartz arenite and siltstone. ing,relatively recessive, thin-bedded to nocular unit that Elsewhere, the Dunedin Formation includes a basal quartz- becomesincreasingly shaley Ir['-sectiort. Th :y cornmoldy pebble conglomerate(McMechan and Thompson; 1985). contain abundant corals and crii-toids and ex remely al,on.- however, this was rot observed in the study area. dant brachiopods: locally, they weather to fol n hrachic~pod Upper Devonlan Fairholme Group strata unconformahly gravels. overlie the Dunedin Formation. The Fairholme Groupcom- The Perdrix Formation has a gradational cc ntact .Mitt, the prises the Flume, Perdrix, Mount Hawk and Simla forma- underlying Flume Formation. It IS characteri; Ed by gr,?yisll tions of Frasnian ag: (Table 1-6-1).The Flume Formation is green to hlack shales with thin, c;~lcareo~~sin16 rbeds tha art: generally 75 to X5 metresthick, however, in theMount recessive and generally very po,:'rIy exposed ThicE.ne?s of Buchananarea it i!; in excess of 145 metres(Geldsetzer, the PerdrixFormation is estimated at hen een 185 and 19x2). Where the whole sequence is exl'osed, as in the area 470 metres (Geldsetzer, 1982). ack of ::ood :xposure, ;md east of Mount Buchanan, the Flume Formation consists of a faulting, make true thickness tstimatiors dif icult. thin quartzose sand$tone unit overlain by a thin unit of red The MountHawk Formatior confcmmahl r ovetlies tht and green calcareomr shales followed by a stromatoporoid Perdrix shales and consists of clirf-fom~inggr :y limsstctrter, hiostrome which is sharply overlain by shaley limestones. often with a ribbed weathering pattern. 11 the GeoloRical Firldwork 1991, Papw 1992-1 73 Plate I-6-h.Lime mudstone chips in n crossbcdded dolomitic sandstone bed from the lower pan of the Lynx Formaticm locally. The nodular limestone units predominantly consist this formation is approximately S30 metres thick. Its base is of skeletal mudstonesand wackestones;skeletal wacke- marked by athin, brown-weathering fossil “hash” layer stones and grainstones comprise the more massive beds. In containing whole and fragmented gastropods, brachiopods the Kakwaarea, the MountHawk Formation is 90 to and crinoids. The lower part of the formation consists of 140 metres thick (Geldsetzer. 1982). recessive to ribbed-weathering, thin, wavy bedded to nodu- TheSimla Formation conformablyoverlies theMount larlime mudstones. with some medium-bedded limestone Hawk and averages 60 to 70 metres in thickness. It com- ledges which grade upwards from grainstonesto mudstones prises a sequence of massive, thick-bedded, resistant, light (Geldsetzer, 1982). These strata are oftenmottled light grey. grey limestones, interbedded with lesser, thin-bedded lime- dark grey and huff weathering. Rareoolitic beds (oolitic stones. Grainstones are the dominant lithology (Geldsetzer, shoals) containing lime-mud intraclasts are present locally. 1982). Like the Mount Hawk Formation, Simla limestones Fossilsare uncommon, with only rarebrachiopods and are very fossiliferous. with colonial corals, bryozoans and scleractinian corals being noted near the base of the forma- crinoids the dominant organisms. Brachiopods occur locally tion. Locally, Hat-pebble conglomerate beds, with a reddish, and gastropods were noted in a few places. In some loca- iron oxide coating, are also present. tions, lisht grey, limy encrustations obscurethe fossiliferous The upper part of the Palliser Formation consists of more nature of these rocks; in other areas, silicification enhances resistant, thin tu medium-bedded, grey to grey-brown mot- the fossils. Thin bands and nodules of black chert occur in tled limestones.Its base is definedby approximately some sectims. In the Kakwa area, lithological similarities 10 metres of black and grey, rhythmically laminated lime between the Siml3 and Mount Hawk formations often make mudstones, which are in sharpcontact with underlying recognition of the contact difficult and it is often easier to lower Palliser lithologies. This marker unit is overlain by distinguish theunits from a distancedue to the lighter thin-bedded lime mudstones and shaley limestones that give weathering colour of the Simla limestones. way,up-rection, to monotonous. medium-bedded lime The Palliser Formation, of Famennian age, consists of a mudstones and pelletal grainstones. Macrofossils are rare in thick succession of monotonous limestones which discon- this part of the section. with brachiopods and crinoid osci- formably overlie the Simla Formation. In the Kakwa area, cles occasionally present: trace fossil markings are common 74 British Columhiu Gcolo,yiml Suwev Brondt Twocarbonate units of Carbmiferou:; age are Fre:il:nt within the study area; the widespread Lower C trboniferws RundleGroup, and the thin, ~-liscontinuous. Uppe- (Jw boniferous Hanington Formatior.The alter is tyyicall y absent due either to nondepositirmn or erosion as pa,-t 0- a widespread sub-Permiandisconformity, The Jnly 1mou.n occurrence of theHanington Formation with n the study area is at the type section, appr0,imately 3 ki 3metre:s east of Moonias Mountain (Bamber and Macquee~, 197'1; Fi:;- ure I-6-2i. Rundle Group rocks crop nut in the southt:ast<:-n and north-central parts of the rxreation lrea ,the Inters#-c- tion Mountainarea and northea..t of Mooni; s Moonlitin; Figure 1-6-2) and reach a thickness 'IF approxilnat',:ly 400 metres. The Rundle Group is subdivid-d into lour 'ormatlon!, in this area. From oldest to young?st, the!, are the Pekisko, Shunda, 'Turner Valley and Mount Head for nations. l'he Pekisko,Shunda and Turner 'bhlley fomati Ins arc 'xry similar in character. All are vari.Ibly thi1 to 1 lick 'cedded, light to medium grey weathering and consih of nteclium grey skeletal grainstones, wackwones atld pat kstones vith minor lime mudstone. Crinoidal clebris is then ost abundant skeletalconstituent. Chert no:hles are typi :ally ab!;f!llt, however, they are locally abundmt. Thf: ove lying Mount Head Formation is predominarltly composed nl 1ig:lt grey weathering, light to dark grey, fine-grairwd do xtonf whch is locallypetroliferous. Chert nodules and c tert hcdr. are very common. Macrofossils are c:)mmon in all of the fomrta- tions of the Rundle Group. The most comnon ;ypes ,ncl,Jde rugosan, scleractinian and litho\trotion cxals: brdchiopo~ls. gastropods and echinoderms are also prr!sent. Rocks of the Hanington Forrrution d~:conf~rmably w:r- lie those of the Rundle Group. AI^ the type re( tion, tiis Nunil consists of mediumto thick-b<:clded, partiall dolomiti2,ed skeletalwackestone. packstonc ;and lime mu Istone. (lerl. nodules and layers are locally common and 3 thin bed 01' chert-granule to pebble conglcmnlerate 'IS four d at i.s 'base Plate 1-6-7. Dr:tached and fragmentcd slromatoporoids in The unit is S metres thick, and i5 litho1oj:icall very similar the Upper Dwunian (Frasnian) Flunle Formation. to the overlying Belcourt Fornmion of' Perm an age. 1Divi~ sion has been made primarily (In the basis , Nf microlimil interpretationwhich has e!:t.l~blishe~i an Upper ('w on bedding planes in the lower part of this section. Nodules honiferous age for this formation (Banixr a. d Maxptsn, of black chen also occur locally. 1979). Permian strata disconformabl) overlie rock of the: Lc'wer UPPER PAI,EOZOIC Carboniternus Rundle Group and the IJ >per kbouifrxlu!; The Upper Pdleomic sequence comprisesa basal clastic, HaningtonFormation. Two lithologi(.ally unique unit:; shale-dominated pat:kage, overlain by a thick sequence of characterizethe Permian oftbe area, the L ,per I'erc~ian carbonaterocks, capped by thin sandstones and chert- MowichFormation sandstones and !tie LCwer I'ern~iao pebbleconglomerates. Terrigenous clastic rocks of the BelcourtFormation gritty lirne.,tones and c lnglornel.ates. Banff and Exshaw tormations, which arepredominantly The Belcoun Formation appears to be axent over much of Lower Carboniferous in age, form the base of this sequence the study area, but where exposed it is sepal rted fkn the and unconformably nverlie the Palliser Formation,These overlyingMowich Formation by a m d-Pe mian discon- units, which cannot be subdivided in the Kakwa area, are formity (Bamber and Macqueen. 1979). recessive and poor1 y exposed. They consist predominantly Belcourt Formation rocks we'e observed i : one ocality, of black shales with thin interbeds of lime wackestone and approximately 3 kilometres ea!,t (of Moonias P lountiin (Fig- grainstone and minor sandstone; carbonate content of this ure 1-6-2). Here,thick-bedded mediungr y we,rtherin:: unit increases up-section until carbonate rocks dominate and chen-pebble conglomerate with a carbonate I iatrix is hter- the strata are asigned to the Rundle Group. A thickness of bedded with, and grades into, Ihick-bemided, medilm grey 180 to 260 metreshas been estimated forthe combined weathering gritty limemudstme, clean li ne mud!;tcae, Banff and Exshew formations (McMechan, 1986). skeletal packstone and wackemne. Fmely ( rystalline dol- Geological Fie1,dwork 1991, Puper 1992-1 iS . ostone predominates toward the top of the unit. Chert peh- siltstone. fine-grained sandstone, silty limestone and shale bles are dark to light grey in colour and are well rounded. (Gibson, 1975). It is quite platey near the base and becomes Gastropods and brachiopods are locally abundant. The true increasinglyflaggy up-section. Ammonitesare relatively thickness of this unit could not be established. hut is not less common; pelecypods were also noted in some sections and, than IO metres. in one location, moderately well preserved fish fossils were The Mowich Formation isby far the more extensive of found (Pel1 and Hammack, 19Y2. this volume). The Whis- the two units within the study area. It is a light brown-buff tler Member, wherepresent, is generally 10 to 20 metres weathering, light to medium grey, medium to tine-grained thick andconsists of dark grey to black-weatheringsilt- quartz arenite. Outcrops are commonly lichen covered, giv- stone, siltylimestone. silty shale. dolostone,phosphorite ing the rocks a dark grey to black appearance. The unit is andphosphatic pehhle conglomerate (Gibson, 1975). typically less than 10 metres thick, and is mosteasily Ammonites, pelecypods. and locally brachiopods. occur in distinguished by its dark colour and its unmistakable strat- thismember and arecommonly phosphatic. The Llama igraphic position between the thick succession of massive Member is characterized by relativelyresistant, orange- grey carbonatesof the Rundle Group andthe thick orange to brown-weathering, thin tothick-bedded dolomitic quartz brown-weatheringsiltstone sequence of theTriassic Sul- siltstones, silty limestonesand dolostones that contain phur Mountain Formation. pelecypods and rare ammonite fossils, and locally, reptile hones.Where it occurs, it isapproximately 150 to M~sozorc: 185 metres thick. The WhitehorseFormation conformably overlies the Sul- Triassic Spray River Group strata (SulphurMountain and phurMountain Formation and is a variable sequence of Whitehorse fomlations), which crop out in the northern and recessive to moderately resistant, buff to light grey to yel- eastern regions of Kakwa Recreation Area (Figure 1-6-2). lowishgrey weatheringdolostones, limestonesand sand- unconformably overlie Permian rocks. The older Sulphur stones, withminor aniounts of siltstone, intrafnrmational MountainFormation is a moderatelyresistant unit that conglomerate and evaporite. Regionally, it can be divided weathers a characteristic dark reddish brown to brownish into the Starlight evaporite member, [he Brewstrr limestone orange colour. I1 has been subdivided into the Vega-Phroso, member and the Winnifred Member with cumulative thick- Whistlerand Llama members, in ascending order. In the nesses of between 130 and 400 metres (Gibson, 1972, Kakwa area, the Vega-Phroso siltstone member is approx- 1975). Limited exposure in the Kakwa area makes subdivi- imately 245 to 270 metres thick and comprises a shaley to sion of the Whitehorse Formation difficult. The most com- flaggy weathering sequenceof dolomiticand calcareous mon lithologies encountered were very porous, sugary, buff Plate 1-6-8. Disharmonic chevron folds in Lower Cretaceous Minnes Fonnatian strata. north of Mount Minnes. 76 Columbia British Geolo~icalSurvey Branch grainstones, huff and grey fossilifen~usgrainstones. mas- fine to coarse-grained carbonaceous sancstont i, siltitones sive, lightgrey weatheringquartz wacke andmedium- and shales assigned to the “Middle” Gates Me nher. Th,ree crystallinedolostones that often had a verystrongly moderately thick coal seams (nmging frmn 2 to 6 r1) Elre petroliferous odor whsnbroken. Chert layers and lenses and present within this unit (Prihyl. l’?79). intraformational hrect:ia horizons were also observed. TheJurassic Fernie Formation is a recessive,poorly STRUCTURE exposed unit with an esrimatedthickness of 250 to The Kakwa area can he hroadl:; divided intc three stnu- 900 metres that, 011 a -egional scale, unconformahly overlies tural domains with differingstructural s.yles. The e,astr!ln carhonaterocks of the Triassic Whitehorse Formation domainincludes the area underlain by furas ic and Cn:- (McMechan, 19Xfi). In the Kakwa area, it crops out east of taceous strata, east of the Broa:hiew faldt (F gure 1-662). theBroadview fault (Figure 1-6-2) and is always in fault The rocks in this region are rela1:vely incomr sent; shales contact with older !strata. The lowcr part of theFernie and thin-bedded sandstonesarc ).he dominan lithologies. Formation consists o‘dark grey and black shale with minor Folds arepredominantly chevro.1 style with short wiw:. sandstone: very thin to thin-bedded, greyish brown weather- lengths, small amplitudes and hi:;:hly vaiable axial pl;ur:s ingsiltstone, silty sandstone and shale with local, more (Plate 1-&X). They tend to he di!harmonic. A .ial trxes ‘of resistantsilty sandstone units in the upper part of the the folds trendsoutheasterly ,md are !;ubpe-allel to llie formation. hounding faults. The Upper Jumsic to Lower Cretaceous Monteith For- The central domain is bounded by the 13roac view laul, to mation confmnahly overlies Fernie Formation strata. It is a the east and, to the west, by the Ulishaw fault i I the bicirlity resistant, lighr grcyi.11 brown to yellowish brown weather- uf, and south of Mount Buchtnxn and by tt e Mom !it. ing marker unit, approximately 200 to 400 metres thick, that Georgefault to the north of !,lount I3uch: nan (Figxe predominantly cunsi!.ts of very fine grained laminated sand- 1-6-2). Numerous minor thrustsoccur withi 1 this m;ljor stones. Wood fragments and crinoids with star-shaped stems sheet; in most cases they are not. more th; n 10 Grolo~iralFieidwork 1991. Pupr 1Y92.1 i7 Plate 1-6-1). Upright to overturned folds in Upper Devonian strata, northeast of Kakwa Lake. The recessive Perdrix Formation (dPx) is exposed at the base of the cliffs and is overlain by the cliff-formingMount Hawk and Simla formations(dSMh) that cannot he easily diflerentmcd in this section. The Palliser Formation(dP) is exposed at the top of the ridge; a slightly more recessive unit at the base of the Palliszr forms a slight step ahove the Simla and Mount Hawk strata. heddedand quite competent. Proterozoic Miette Group 3 metres thick and occurs at the top of the Gething Forma- strata are exposed,in 3 number of locations, in the immedi- tion. The overlying Gates Formation, the top of which has ate hangingwall of the east-hounding faults. The dominant been eroded, hosts three seams that were trenched in the late structures in this part of the area are open folds and broad 1970s and are reponed to be I .X to 2.7, 3.6 to 6, and 5.5 to warps with east or southeast-trendingaxial traces and north- 6 metres thick, respectively (Prihyl, 1979). The coal-bearing erly directed thrusts with east to east-southeast traces. Nor- strata cap the ridge and the seams. which contain an esti- mal faults are also prominent within this block, particularly mated 4 to 4.5 million tonnes of coal, could be exploited at in the southwestern area, near Mount Sir Alexander. Most stripping ratios of between 1:l and 15:l (Prihyl, 1979). strike westerly and southwesterly. Small drag folds areoften Coal seams also occur within theLower Cretaceous associated with the normal faults. The east-west structural Minnes Fonnation in the Mount Minnes and Mount Gorman trends within this domain are anomalouson a regional scale. areas, in the northeastern part of the Kakwa area. Several seamsare present,particularly in the upper part of this formation; however, they aregenerally less than I metre ECONOMIC GEOLOGY thickand not of serious economic interestunder current conditions. COAL Coallicenses are heldin thenortheastern corner of DIMENSIONSTONE Kakwa Recreation Area, covering the ridge south of Mount Quartzites of the Lower Cambrian MahtoFormation, that Gorman. This areais underlain by a shallow, south-dipping cropout in the centre of KakwaRecreation Areanear sequence of LowerCretaceous stratathat containsfour Babette and Wishaw lakes, were examined in the late 1970s significant coal seams. The lowest seam is reportedly 2.4 to and early 1980s for their potential use as dimension stone. 78 British Columbia Geological Suwey Branch At thattime, roadswere extended to the prospects from exihtinglogging lroads in the McCregorRiver valley. At Babette Lake the :mala were drilled, while at Wishaw Lake an attempt was made lo quarry test blocks. The only mineral Lwatim claims currently held within the recreation area cover these Stone prospects. The MahtoFonnxion, at theBabette Lake prospect, consists of fine to medium-grained. locally crossbedded quartzites that vary l'rom creamy white 10 dark maroon in colour; some beds are uniform in colour. while others have quite attractive colour handing. Some of the colour handing is parallel to sedimertxy laminations anif crosslaminae and may reflect a depositional feature, however, much of the ;ai;lly,rd hy gv~b#~l"cwrm.t) n~clhd handing appears to be unrelated to original sedimentary features and forms iltricately swirled patterns that may he related to solution fionts (Plate 1-6-2). Beds slightly more locality,approximately 12 centirnetres II~ph lsphate rw:k than a metre thick are common. Large blocks, in the 1 to overlies thin tomedium-beddt:d. grey argil1 Iceous lime- 2 cubic metre siLerange. are found in talusbeneath cliff stone and calcareous siltstone. 'The phuzphor :e horizorl is outcrops. At Wishau Lake, the Mahlo quartrites are creamy black to dark brown in colour, as anodula texture ;md white or beige to light pink in colour: most of the colour containsabundant ammonitefossils. It is overlrirl by banding at this location is parallelto laminations and YO centimetres of grey, silty limestone, whic 1 is, in l;urn, crosslaminations, Bedding thicknesses range from SO centi- overlain by I8 centimetres of phphatir ,hale and si tstwe. metres to justover a metre: beds up to 2 metres thick Sixteen centimetres of very fis,ile black shal, s ove-lie: the are reported(Hori., 1984). Quarriedblocks, 2 to 2.5 phosphatic shale and the sequence is capped ~y more grey cubic metres in six. are present on site,however, there limestones. Thelower nodular and fo:,sil-ri:h phospllate are noblocks in {he size range preferredby industry horizon is moderately high gracle, contailling i pprox m;alf:ly (1.4~1.6~3m) on :,ite at this time. 22 percent P,O,, while theLpper hor zon ~f phcsphatic shalesand siltstones contains biztween X an< 1 I per mn! When cut into slabs and polished, the quartzite from these P,O, (Samples 1091 and 1094, Table 1-6.: ). Tht: erltirt prospects has a coluur and textural qualities comparable to phosphalic interval is only 1.2 lrstres tlxk ir this area and high-quality. cornm:rci;llly exploitedmarble andstrength limestones comprise a greater pjponion ofit :han do phs. cornparable to hiph-,.pality granite (How, 1984). Due to the phorites and phosphatic shales. extreme hardness of this material, however. it is more diffi- cult and hence, mort: expensive to finish than either marble A thisdphosphate occurrence was fixmdin the south.. or granite. Also of cilncern, is the variahle porosity of these eastern corner of Kakwa Recrealion Area. ne. r Inte..sect or1 quartzites. In some places,the rock is well cementedand Mountain. It outcrops on a cliff .ace and is e timatcd to be no more than a metre in thicknrs,. Nodu'aran I fossilifcrou:; has low porosity, while in others it is quite porous, stains phosphorites with fluorite-coatedfrac.ure urfaces wen: easily and would 11clt produce an acceptable product unless treated with some type of sealant coatinp toreduce staining. found in talus beneath the outcrops. Crd? sax ples from this The distribution of porous, and therehre, less desirable area contain between I8 and 21) per crnt F :Os (!;arnple,i material within the,e prospects has not been documented 1251A and B, Table 1-6-2). (Z.D. Hora. permn:,l communication, 1991 ). CARBONATE-HOSTEDVt:rru AND PHOSPHATE REPLACEMENTSHOWIN~;S Vein and replacementshowings in car ionate rcckr,, Phosphorite beds are found within the Whistler Membcr although not common in the Kakwa arm. w :re di>covere,d of tht. Triassic Sulphur Mountain Formation at three loca- in sixlocations. Southeast of Moult Id , anorange- lionsaround K.akwa. In the northernpart of thearea weathering, irregular dolomitized zone is e, posed in Ight mapped, near the boundary of the recreation area, phospha- grey limestones near the top OF I he Midile C lmbrien :Snake tic rocks occur near the core of a syncline in the Sulphur Indian Formation. Coarse-graini:d dolomite ( ,ccurs in veins MountainFormation (Figure 1-6-2). At thislocation, the andsolution-collapse breccia infillings w thin the: (dol- phosphatichori7.m is 10 to 15 centimetres thick and is omitized rocks. Small shear zc9nt:s. dominant y con:isti,lg of exposed in a rubtmly outcrop associaled with calcareous fine-grained calcite, are also pesent in this a1 :a. To the west siltstones and silty imestones. The pho3phorite is dark grey of Mount Ida, an irregular zone #ofaltercd an, recrystallized or bluish to white weathering. with n dark brown to black dolomite,cut by coarse-graned dolcsmite veins,occurs fresh surface. It has a gritty texture, a petroliferous odorand within limestones of the Middle Canyxian Eldon Fcrm;I- contains abundant ammonite and pelecypod fossils. Purple tion. No evidence of potentsally economic commodities, fluorite is presetnt as veinlet infillings and fracture coatings. such as lead,zinc or magnesile was iound in either ,m:a Grab vamples of these phosphorites contained 21 to 23 per (Table 1-6-3). althoughcorrttl;ltive strata i 1 soulheastern cent P,O, (Samples 1097A and B, Table 1-6-2). British Columbia are known ~IIhost ezonoi 1ic deposils In To the east of this occurrence, on theeast limb of the similar environments (Grieve a,nd Hoy. 198 : Simandl and adjacent anticline, phosphatic rocks again outcrop. At this Hancock, 1991). Geo/oc~icu/Fieidn:,wk IYYI, Paper IYY2-I 7Y ~ In thesouthern part of the area, southeast of Mount QUAR.I.ZITE:-HOSTEDVEIN SHOWINGS Buchanan,coarse-grained dolomite occurs in veinsand open-spnce fillings in a brecciated zone within Ordovician Quam veins containing pyrite or associated with pyritic Skokidolostones. East-northeast of Mount Buchanan alteralion halos were found in Lower Cambrian quartzites at cosrse-grained calcite veins containing minor amounts of two locations. A few kilometres south of Mount Ida. pyritic barite cut irregularly dolomitized zones in Upper Devonian quartz veins associated with ruhty. pyriticalteration halos Mount Hawk limestones.These veins are narrow and cut McNaughton Formation strata. North of Kitchi Moun- appear to be barren; they are not particularlywidespread tain, irregular quartz-pyritc veins, with alteration halos that (Table 1-6-3). locallycontain SO to 70 per centpyrite occur within the Mahto Formation. No gold or base metals were noted in the Barite veins and replacement zones, over a metre wide, limited samples collectedfrom these veins(Table 1-6-3) were found in Rundle Group carbonate rocks at two loca- eventhough veins in similar rocks.south of Jasper,are tions, near theupper pan of theunit. One site is in the known to carry gold (Shaw and Morton, 1990). northernmostpart of thearea mapped, approximately 2 kilometres north of the recreation area boundary and the other is near Moonias Mountain, north of Jarvis Lakes. In both localities, the veins consist predominantly of coarse- STRATIFORM SULPHIDES grainedwhite barite, at the northernlocation carbonate inclusionsand rusty vugsare common within thevein. Apparentlystratiform massive sulphide mineralization Samples collected from these veins did not contain appre- wasfound in fine-grainedsandstones of thePermian ciahle amounts of base metals (Table 1-6-3); however, the Mowich Formation at two locations. Near Moonias Moun- rusty material from the northern locality could not be ade- vain, approximately 3.5 kilometres north of Jarvis Lakes. quately sampledand in both cases the material analyzed was beds of pyrite I to 3 centimetres thick were discovered. In predominantlypure barite. The Belcourt Linc prospect, the southern part of the area, near Intersection Mountain, a located approximately 6 kilometres north of the recreation gossanouszone, approximately 6 metresthick and area,occurs inthe same stratigraphicposition and also 20 metres in strike length, occursin what should beMowich consists of barite veins with patchily distributed zinc miner- strata. In the same area. pieces of dark, bituminous sand- alization. This showing is reported to contain up lo 2 per stone containing up tu 40 per cent pyrite were found in iloat cent zinc (Lenten, 1980); grab samples of gossanous mate- beneath Mowichoutcrops. Samples of pyrite-rich ?and- rial and altered dolomitic wallrock, collected during a brief stones contain anomalousconcentrations of zinc, up to visit to the showing, contain 0.35 and 0.65 per cent zinc, 0.7 per cent (Table I-6.3). Zinc mineralization in Permian respectively, whilebaritic vein material does not contain sandstones has also been reported from the Belcourt show- appreciable zinc values (Table 1-6-3). ing, a few kilometres north of Kakwa (Lenten, 19x0). TABLE 1-64 CHEMICAL ANALYSES OF VEIN, REPLACEMENT AND STRATIFORM OCCURRENCES - Carbtmate-hosted vein-replacement showings in Rundle Group strata I071 na Cn.2 2 <2 13 0.04 barite Norih Ridge 2028 na CO.? I0.w got.oethttc 6 k N of Kakwa KCC. Area BEL3 nil 0.2 2 c2 43 0.32 barite 6 k N of Kakwa Rrc. Area 4 k SE of Mt. Ida 4 k~~ SF." nf~~ ~Mt ~.. ."Idn 6 k W of MI. Ida 3 k ENE of MI. Ruchanan 3 k ENE of Mr. Buchanan 3 k SE of MI. Buchanan Quanrite-hosted vein-replacement showing I100 6 <0.2 4 7 21 3.71 qdpy 3 k S of Mt. Ida 2078 6 a2 5 12 5 > 10.00 pyrm 2 k N of Kitchi Mi DISCUSSION AVD CONCLUSIONS cases, smallerblocks might he iutilized hut again, ttNis wouldresult in increasedcosts. Distance to e Geological Fieldurrk 1991, Paper- 19!22-1 81 Colunlbia and West-central Alberta: Geological Surrey Mountjoy, E.W. and Aitken, J.D. (1978): Middle Cambrian of Canada. Bulletin 247, 61 pages. SnakeIndian Formation [New], Jasper Region, Grieve, D.A. and Hoy. T. (1981): Lead-Zinc Showings in Alberta; Bullc2tin ofCanadia!r Petroleum Geolo~?y).. Vol- CarbonateRocks, Southern Rocky Mountains: in ume 26, Number 3. pages 343-361. Geological Fieldwork 1980, B.C. Minis1r;v of Ener;?y. Pell. J. and Hammack. J.L. (1992): A New Triassic Fossil Mines and Petroleum Resources, Paper 19X 1-1, pages Fish Locality.Kakwa Recreation Area, Northeastern 105-1 IO. Britibh Columhia (Y3l/l); ill GeologicalFieldwork Hura, Z.D. (1984): Industrial Minerals and Structural Mate- 1991. Grant, B. and Newell. J.M., Editors, R.C. Miuis- fry nf Eueq?. MIIWSand PcWolelrm Resorrr-res, Paper rials: in Geological Fieldwork 1983, B.C. Minisfry /$ Energ?: Mines and Petroleum Resour-ces,Paper 1984- I, 199?-1. (this volume). pages 213-218. Pribyl, A. (1979): Preliminary Report on the Geology of the Legun, A. and Elkins, P. (1986): Wapiti Syncline Phosphate Mt. Corman and Coal Ridge Area B.C. Coal Licenses; Potential; in Geolugical Fleldwork 1985, B.C. Minisrry B.C. Min;.sfr-y of Energ?. Mitwsand PetroIPum R~,.sourw.s. 00549, 17 of Enet-gy, Minesand Perroleum Resowces. Paper Open File Coalfile Report pages. lY86-I, pages 151-153. Shaw, R.P. and Morton. R.D. (1990):Gold Mineralization in Lower CambrianMcNaughton Formation,Athabasca Lenters, M.H. (I 980): Report on Geological Mapping, Pros- Pass,Canadian Rocky Mountains: Structural, Miner- pecting.Trenching and Geochemical Sampling, alogical and Temporal Relationships; Canadian Jour- Belcourt Claims, Liard Mining Division; B.C. Ministry nal of Earrh science.^. Volume 27, pages 477-493. 01' Ener~qy.Miner and Petroleum Resour-ces. Assess- ment Report 8404, 26 pages. Simandl, G.J. and Hancock, K.D. (1991): Geology of the Mount Brussilof Magnesite Deposit, Southeastern Brit- McMechan,M.E. (1986): Geology of theNortheast ish Columbia; in Geological Fieldwork 1990. B.C. Min- McBride Map-area (93H3/15, 16). British Columbia; ;.vry ofEner~qJ.Mines and Prtmleum Resourcrs, Paper Geological Slrrrey of Canada, Open File 1229. 1991-1, pages 26!)-278. McMechan,M.E. (1990): UpperProterozoic to Middle Slind, O.L. and Perkins, G.D. (1966): Lower Paleozoic and Cambrian History of the Peace River Arch: Evidence ProterozoicSediments of theRocky Mountains fromthe Rocky Mountains; Bullrtin of Canadian between Jasper. Alberta and Pine River, British Colum- Petroleum Geology, Volume 38A. pages 36-44. bia: Bullerin of Canadian Petroleum Geology, Volume McMechan, M.B. and Thompson, R.I. (1985): Geology of 14, No. 4. pages 442-468. SoutheastMonkman Pass Area (Y31/SE), British Taylor, G.C. and Stott. D.F. (1979): Geology of Monkman Columbia; Geological Surwy uf Canada, Open File PassMap-area (931). NortheasternBritish Columbia; 1150. Geolo,qical Survey of Canada. Open File 630. 82 British Columbia Geological Survey Branch