KEYWORDvolcanic-hporphyry, Group, Isk

INTRODThe

Columbia endowmenRiver incMountain, past produdeposits environmeveins to deposits wwithin a 2River, yetCopper Caby alkalicexplanationcorridor ismaps; howeither nevesince it wworking pColumbia Resources,auspices oStrategy: Gthe Univergeologic Supplemengeological evaluate tpolymetallIskut and mainly foclacking: th

1 Geologica Ottawa, ONThis publicadigital filesMinistry of Fhttp://www.alogue/Field

by

DS: Hoodoo osted massive Galore Creek

kut River, Twin

DUCTION Iskut River

is characternt. A 20 km-wcludes the B

Eskay Creek uction or definformed in a

ents ranging fshallow suba

with past produ20 km corridort those fartheanyon and Schac and calcaln for the dearts not forthcowever, a signier been system

was surveyed bartnership wasMinistry of

, the Geologicof the GeosciGEMS), Pacifirsity of Victorknowledge

ntary goals wsetting for th

he potential flic massive su

adjacent regicused where p

he eastern half o

al Survey of CanaN ation is also avas in Adobe AcForests, Mines aempr.gov.bc.ca/dwork.

GeoHoodo

M.G. Mihal

Mountain, sulphide, Roc

k, Stikine asn Glacier River

area of norrized by exwide corridor Bronson Slopand Rock and ned resources a surprisinglyfrom intrusion

aqueous hotspuction or definr immediately

er afield incluaft Creek depolkalic porphyrth of deposits woming from eificant part ofmatically mappby Forrest Kers established bEnergy, Min

cal Survey of ience for Eneic North West ria to address through systere to provide

he Rock and Rfor similar pr

ulphide mineraions (Figure 1published mapof the Hoodoo

ada, Natural Res

ilable, free of chcrobat® PDF foand Lands websi/Mining/Geoscie

ology andoo Mounta

lynuk, J.M.

Andrei Icefck and Roll, cossemblage, Stur, Bronson

rthwestern Brxceptional min

south of the pe, Snip, Joh

Roll deposits (Figure 1). T

y diverse setn hosted sulp

pring settings.ned resources o

north of the ude Galore Cosits that are hories. An obvwithin the nortexisting geolof the corridorped or at leasrr in the 1920between the Bres and PetroCanada (unde

ergy and MinCapital Corp.this lack of putematic mappe a more accu

Roll deposit anrecious metal alization within1). Our work pping was entMountain map

sources Canada

harge, as colourformat from theite at ence/Publication

d Mineralain Area

Logan, A. Z

field, opper uhini

ritish neral Iskut hnny with

These t of phide No

occur Iskut reek, osted vious thern

ogical r has t not

0s. A ritish leum r the

nerals , and ublic ping. urate nd to

rich n the

was tirely p

a,

e BC

sCat

Figuthe C

sheebord(104sheeregi104G104G

LO

104BIskunort

ization of(NTS 104

Zagorevski1

ure 1. Location oCoast Belt and w

et (NTS 104B/dered to the n4G/03; Figureet (104B/15), ional geologicaG/03, 04; anG/02, 07W; Fi

OCATION AAccess to th

B/14E) is via ut River 300 kthwest of Smi

f the 4B/14E) 1 and N. Joy

f the Iskut study western Stikine te

/14E, Figures 2north by the 2) and to the

both covereal surveys (Lo

nd Logan et igure 2).

AND ACCEhe Hoodoo M

the Bronson akm north-northithers, and 75

yce1

area near the boerrane.

2 and 3). This mGalore Creek east by Forres

ed by relativogan and Koyaal., 2000, 10

SS Mountain map

airstrip, locatehwest of Terra5 km east-nort

oundary of

map sheet is map sheet

st Kerr map vely recent anagi, 1994, 04B/10, 15,

area (NTS ed along the ace, 330 km theast of

Geological Fieldwork 2010, Paper 2011-1 37

Fi(Nre

WarV(~is aiheThSttwopSkIs

alexOthdiAné

gure 2. SourcesNTS 104B/14W). egional geology p

Wrangell, Alaskre serviced b

Vancouver and ~5 hour drive) a 60 km flighirstrip that is selicopter serviche nearest petewart, approx

wo seasonal cperation. Accokyline Gold Cskut River.

Iskut Riverlpine glaciers xtending to we

Our fieldwork fhe Iskut River aistributary glac

Andrei Icefieldévé/accumulati

s of geological mLocation of the R

portrayed within t

ka (Figure 1). by scheduled

both are apprfrom Bob Qui

ht southwest frserviced by roce is generallyermanent charimately 110 kmcamps adjacenommodations

Corp. or the K

r occupies a Udraping many ell below treefocused on theand nunataks ociers. (Note th

d as the colleion zone from

ap information wRock and Roll prthe study area (re

Both Terrace commercial

roximately 400inn airstrip. Brrom Bob Quinad access. Sea

y available fromrter helicopterm to the southnt to the airscould be arr

Kossey fishing

U-shaped glaciaof the adjace

eline at ~1000 e mountain slo

of the Andrei Ichat herein weective ice ma

m which the m

within the area beroperty (Black Doed rectangle) is l

and Smithers flights from

0 km by road ronson airstrip nn, the nearest asonal charter m Bob Quinn. r base is in

heast. In 2010, strip were in anged at the camp on the

al valley with ent ridges and

m elevation. opes north of cefield and its e refer to the ass and high many large

etween the Craigog surface showilargely after Kerr

valley glawe refer the northewhich is 104B/15; region is to fly; uncharactalso facilbase caaccompan

REGIOWORK

Most104B/14Eregional InternatioForrest K2) covere

River and the eaing) and importar (1935) as comp

aciers of the ato as the maineast corner of 10.5 km nort

Figure 2). Wcommonly cu

however, teristically waritated by the w

amp at Broniment of VIH

ONAL GEOK

t rocks north E have not bee

program. Tonal BoundaryKerr between 1ed the corridor

astern Hoodoo Mant landmarks arepiled by (Massey

area emanate. n, >2 km wide104B/14 (Figuth-northeast of

Work in this typurtailed by low

mid-August rm and cloud-

well-appointedonson airstrip

H Helicopters L

LOGY AND

of the Iskut en mapped as

Topographical y Commission926 and 1929 along the Isku

Mountain map she also indicated. y et al., 2005).

The Andrei Ge, outflow glac

ure 3) the termif Newmont Lapically rainy c

w cloud and inof 2010

-free. Our word Skyline Goldp and heli

Ltd.

D PREVIOU

River withinpart of a systemapping by

n with additio (Kerr, 1948; F

ut River, but Ke

heet The

Glacier cier in inus of ake in coastal

nability was

rk was d Corp. icopter

US

n NTS ematic y the

ons by Figure err

38 British Columbia Geological Survey

Geological Fieldwork 2010, Paper 2011-1 39

F f pFigu

re 3

. Geo

logy

of

faul

t (A

, B) a

nd m

ode

poss

ible

eas

tern

lim

it

the

Hoo

doo

Mou

ntai

nlle

d ra

nge

of s

inis

tral

of th

e ca

rbon

ate

belt n

– Is

kut R

iver

are

a s

offs

ets.

The

se c

ould

(p

roje

cted

thru

st tr

a c

impl

ified

afte

r Mih

alyn

offs

et th

e no

rther

n R

ce).

For s

ourc

es o

f da

nu

k et

al.

(201

1a).

Sh

ock

and

Rol

l hos

t stra

ata

cons

train

ing

the

gehow

n so

uth

of H

oodo

oat

a (s

chem

atic

ally

sho

eolo

gy s

outh

of M

ouno

Mou

ntai

n ar

e po

ssib

own

by th

ick

red

and

nt V

erre

tt se

e M

ihal

yn

ble

wes

tern

ext

ensi

onbl

ue li

nes

-see

text

fonu

k et

al.

(201

1a).

ns o

f the

Ver

rett-

Isku

tor

cav

eats

), an

d th

e t

40 British Columbia Geological Survey

designatedwith a fewthe 1920s than is todseen at Twmapped thlong nunatextending his 1:126 7conducted 1:50 000 sback to foreastern tosurveys in1:20 000 Managemegrown to 2an additiocaptured ieastern tonThus, mucexposed aeverywhermineraliza

Figure 4. A the photo fo

d the area farthw peaks rising

much more oday. A striking win Glacier (Fighis area, two totak east of Habout 1 km so

720 scale map.in the mid 197

scale Mapping rm two separat

ongue replacedn the late 19

scale Terent (TRIM) m2 km in length,onal 1 km. Hin October, 2ngue having

ch of Kerr’s “Land never-bee, including tion.

view to the southrmed an isolated

her north as onabove the ice

f the region wexample of gl

gure 4). When ongues of ice soodoo Mountaouth of the nu. By the time a70s for the Naprogram, the

te tongues withd by a lake.80s produced rrain Resou

maps, at which , with the ice h

High resolution010 show theretreated an a

Large Ice fieldefore-seen roc

new outcrops

h of the eastern d nunatak in the

ne “Large icee level”. Indeewas covered bylacial retreat caKerr surveyed

surrounded a 5ain, re-joining

unatak as showaerial surveys

ational Topograglacier had m

h a kilometre o Provincial a

the base forurce Inform

time the lakehaving melted n satellite imae terminus ofadditional 1.7 ds...” terrain is ck exposures s with signif

lobe of the Twin 1920s. This phot

field ed, in y ice an be d and 5 km

g and wn on

were aphic

melted of the aerial r the ation

e had back

agery f the

km. now

are ficant

soutHoloal., Twipartwereprog(AnprevAndcoman regi

and unde(MovolcGrouthe Logand data

Glacier showingto was taken at t

Subsequent thwest corner ocene Hoodoo2000) and a

in Glacier nunts of the Iskut e mapped as gram under t

nderson, 1993)vented systemdrei icefield

mmunication, 2overview of

ion, which is noExisting mapolder strata

erlain primarionger, 1977) canic and deriup (Souther, 1geological re

gan et al. (2000north. Prelim

a collected in

g drastic retreat sthe end of a heat

mapping in of 104B/14E

o Mountain vostructural stud

natak (Filliponemap area (1:2part of Geolothe direction ), but persist

matic coverage in 104B/14

2010). Mihalynother geologiot repeated her

ps of 104B/14into two domily by Paleozand a wester

ived sediment1971). Our wo

elationships m0) in the adjoinminary interpre

2010 indicate

since ca. 1920. Tt wave in August

the area coas part of a s

olcanic rocks (dy focused in e and Ross, 19

250 000 scale, Nogical Survey

of Andersontently incleme

in the area E (Anderson

nuk et al. (201ical studies inre. E separate the

mains: an eastezoic Stikine rn domain untary rocks of ork in 104B/1

most recently oning map sheetetation of thees that the La

The ridge on the wt of 2010.

overed the study of the (Edwards et part on the 989). Many NTS 104B) of Canada

n in 1991 ent weather around the

n, personal 0) provides

n the Iskut

e Mesozoic ern domain assemblage

nderlain by the Stuhini

14E extends outlined by ts to the east e geological ate Triassic

west side of

Geological Fieldwork 2010, Paper 2011-1 41

StbrvoovCvoas

PathbymCprinmdi

S

ad(2isrefoarcocacothan(FortuLaarJu

FiHoof

tuhini Group roadens westwolcanic strata (verlies a arboniferous olcanic arc anssemblage (Bro

East-directealeozoic and M

he thrust faultey intrusions th

main periods arboniferous, robable Late ntrusion-related

mineralization. isruption, intru

STRATIGRAStratigraphi

djacent areas, 2000), which botopic age

ecognizable stror stratigraphicrea. Two of thontain distinctarbonate is cholumnals (Figuhe presence ofnd locally, byFigure 6b). A range weatheriuff and volcanoate Triassic agre less diagnourassic in age.

gure 5. Packstooodoo Mountain f the Carbonifero

arc and basinward where it is

(Figure 3). Stucomposite b(to Devonian d carbonate bown et al., 199ed thrust faultMesozoic strataed terrain and hat are Mesozo

of mineravolcanogenic Triassic age

d vein, skDetails of t

usion and miner

APHY ic assignment

particularly tuilds upon extdata. Three

ratigraphic intc correlations wese intervals, Cive thick carbharacterized b

ure 5). Permianf large Rugosay accumulatiothird interval,

ing, coarse biogenic conglomge (see below)ostic and likely

ne dominated byarea. Large crinus limestone stra

nal strata forms overlain by Euhini Group unbasement of

(?)) and Laank deposits o1). ts interleave aa. High angle have subsequeoic to Eocene

alization are massive sulph (Bernales ekarn and the stratigraphralization follo

ts rely on tthe work of ensive fossil co

well dated ervals form th

within the HoodCarboniferous bonate units. Cby abundant n carbonate is ran horn coralsons of giant , dominated botite and K-femerate, is beli). Other congly range from

y crinoid columnsoid columns are ata.

m a belt that Early Jurassic nconformably f deformed, ate Paleozoic of the Stikine

and duplicate faults dissect

ently been cut in age. Two

recognized: hide-style and et al., 2008)

disseminated hy, structural ow.

the work in Logan et al.ollections and

and easily he framework doo Mountain and Permian,

Carboniferous large crinoid recognized by s (Figure 6a),

foraminifera by brown and eldspar-phyric ieved to be of omerate units Devonian to

s in the eastern characteristic

Figure 6a.Mountain a

Figure 6b.Mountain a

DevoniaLowe

the Forrintermedigabbro, quartz seDevonianthe easteoutcrops immediatthis old romafic to phyllite,

. Characteristic Parea; Rugosan h

. Characteristic Parea; giant fusuli

ian er to Middle D

rest Kerr areaiate to mafic mrecrystallized

ericite schist...n rocks have noern Hoodoo M

of marble tely west of thock package. Iintermediate vslate and lim

Permian fossils worn corals.

Permian fossils wnaceans (2 cm lo

Devonian strata as “...pene

metavolcanic tulimestone, g

” (page 12, Lot been positiv

Mountain areaand mafic m

he Bronson airIn addition, an volcaniclastic rmestone intrud

within the Hoodoo

within the Hoodooong) in a packsto

ta are recognietratively defouff, flows, diorigraphitic schisLogan et al., vely identified a; however, ismeta-igneous rstrip may beloundated sequerocks, tuff, graded by metag

o

o one.

zed in ormed, ite and st and 2000). within

solated rocks

ong to ence of aphitic gabbro

42 British Columbia Geological Survey

plugs and The litholometamorphelsewhere concrete agoriginally s

CarbonifStrata

in the eabimodal mwell-bedderocks in characteriswith VHM2004). Caoverlie the

Mafic volCarbo

bright greebasalt and be less tharimmed byjasper (Fignorthwest rubbly carcontains abgrades intscoria. The

The lodefined. Inrocks overwith Viséa

Felsic voCarbo

pink and p

Figure 7. Irrfilled with castems (i.e. feand in somegrades into w

basic dikes unogical associatihism resembl(Logan et al

ge control for suggested Tria

ferous of Carbonifer

stern Hoodoomafic and felsiced carbonate, cthe Forrest K

stics (Logan eMS Zn-Pb-Cu arbonate and o Carboniferous

canic rocks niferous mafien, aphyric to breccia. Calc

an 0.5 m in lony bright red jaspgure 7). This u

of Newmont rbonate matrixbundant large to thick-beddee carbonate locower contact ofn northeast parly polymictic c

an felsic volcan

lcanic rocksniferous felsicale green weat

regular flow top oarbonate containiew centimetres a

e cases veined, bwell-bedded carb

nderlie the Twiions, poly-phale those of l., 2000). Howthese rocks do

assic age (Kerr,

rous age are exo Mountain arc volcanic rocchert and wackKerr area dispet al., 2000) a±Ag-Au mine

other sedimens volcanic sequ

ic volcanic ro

finely plagiocite amygdaloidng dimension per, and/or occunit is well ex

Lake where x to flow-top

crinoids ossiced carbonate

cally forms crinf the mafic volrt of the area, conglomerate anic rocks.

s c volcanic rockthering and aph

on Carboniferousing abundant largabove fingers). Pby red jasper. Flobonate containin

in Glacier nunse deformation

Devonian swever, the lacoes not preclud, 1948).

xtensively exprea. They incks and interva

ke. Similar volcplay primitiveand are assoceralization (Lont-dominated suence.

ocks are typiclase-phyric pidal pillows tenand are comm

cur with interpixposed 7 km w

it is overlainbreccia fragm

cles (Figure 5)containing b

noidal packstoncanic unit is pothe mafic volc

and are interca

ks comprise whyric to quartz-

s pillow basalt is ge fossil crinoids

Pillows are outlineow-top breccias g basalt scoria.

natak. n and strata ck of de the

posed clude als of canic e arc ciated ogan, strata

ically illow nd to

monly illow west-n by

ments ) and basalt ne. oorly canic

alated

white, -

in-

s ed,

phyreffuchargradby cupwunit300hyal

FiguContbase

Figumatr

Figu

ric tuff and rhusive units. Tracterized by ded felsic ash coarse basal b

wards into thin ts define sepam of felsic ej

loclastite basa

ure 8a. Early Cartact line highlighte of the next.

ure 8b. Early Carrix.

ure 8c. Early Car

hyolitic to daThe upper pwell bedded, flow tuff beds

breccia (5-10 mcherty dust tuf

arate eruptive jecta interbeddalt (Figures 8b

rboniferous felsicts the top of one

rboniferous pillow

rboniferous basa

acitic locally fpart of the decimetre-thic

s which may bm) thick, and ffs beds (Figur

cycles that pded with the pib, c), particula

c ash flow and bl eruptive unit an

w breccia with hy

altic pillows and t

flow-banded section is

ck, normal-be underlain

may grade re 8a).These preserve 2-illowed and arly well-

ock breccia. d coarse

yaloclastite

ubes.

Geological Fieldwork 2010, Paper 2011-1 43

diarcovovoCprprfeEada

M

dobe4 a (Fvacowabinco

it demBC(P

C

ligdibepoth

Fibe

isplayed in therea. Pink weatommonly cut olcanic rocks. olcanic sectiarboniferous (resence of lareliminary isotelsic tuff unit narly Carbonifeata).

Mid-Carbonife

An approximominated by theds of crinoidacm diameter (metre across

Figure 9b), anariable abundaontent is spora

with pyroclasticbove the basnterlayered wiontact of the un

Coarse crinhas been

etermination (Lmost precise

ashkirian agearboniferous (

Pennsylvanian)

CarboniferousParallel inte

ght grey andistinctive unit eds 5 to 15 cmoorly induratedhan 5 cm thick.

gure 9a. View toeds flanked by m

e north and ethering, quartz

the section Bedding tops

ion which (?) carbonate targe (>3.5 copic age determ

near the top of erous (Viséan)

erous carbon

mately 190 m hinly-bedded s

al limestone (Fi(Figure 5). Colare preserved

ngular lapilli nce, up to a madic, but genec debris all bue of the uniith crinoidal gnit. noidal packston

extensively Logan et al., 2age control (~328-312 M(Mississippian)) boundary.

s chert-clayserbeds of grey d yellow-weatabove the Carbthick alternate

d claystone la Rounded clou

o the north of a smore massive bed

astern portionz-phyric rhyolmay be rela

s suggest an uprojects be

that is distingucm) crinoids mination of ~3the successionage (N. Joyce

nate

thick section osets to massivigure 9a) with lonial coral hea. Bright greenand reworked

maximum of ~1erally decreaseut absent moreit. Planar chgrainstone ne

ne extends to thsampled for

2000). Faunas reveal a Ser

Ma), spanning) and Upper C

stone to black chert thering claystboniferous care (Figure 10) wayers that are udy quartz grain

set of thin tuffaceds, each 1-1.5 m

ns of the mapite dikes that

ated to felsic upright facing eneath mid-uished by the

ossicles. A 40 Ma from a

n confirms the e, unpublished

of carbonate is ve metre-thick

ossicles up to ads more than n basalt clasts d ash are of 5%. Volcanic es up section e than ~40 m ert beds are ar the upper

he east where fossil age

providing the rpukovian to g the Lower Carboniferous

and recessive tone form a rbonate. Chertwith recessive,

typically less ns ≤ 1 mm

ous packstone thick.

Figure 9b.scoraceous

Figure 10.contains dibeds.

diameter radiolariacleavage may be pelagic ri

Onlyobserved.bearing pthat has nduring thwith unitsor not exdeformedthickness than 100

Late CaThick

volcanic north of Figures 22000) and

. Thickly beddeds basalt clasts.

. Very well beddeistinctive grey an

within chert a; although somand are likelya distal turbi

ibbon chert sucy a few exp. It presumably

portions of Carbnot been structhe course of ous of assumed P

xposed. Where d such that al is that it is mm.

arboniferoukness of Uppestratigraphy hthe Scud Riv

2-4) and in thed are anticipat

conglomeratic c

ed chert-siltstonend yellow weathe

are interpreteme white grai

y reworked feldidite and not ccession. posures of thy grades into tboniferous carturally disrupteur mapping. SPermian age ar

best exposed,ll that can be

more than ~10

us (?) er Carboniferohave been estiver (Brown et e Mess Creek

ated to crop ou

crinoidal packsto

e-claystone unit ering, recessive c

ed as recrystans appear to hdspar. Thus, th

strictly a bio

his unit have the underlying rbonate, but a sed was not identratigraphic co

re similarly dis, the unit is stre stated of thm and probabl

ous mafic and imated as >15al., 1991; see

k area (Logan ut in the study

ne with

clay

allized have a he unit ogenic

been chert-

section ntified ontacts srupted rongly

he unit ly less

felsic 500 m e their et al.,

y area.

44 British Columbia Geological Survey

Varicolourand fine grthat underlarea mighthem as bfollowing)assignmencannot unexample: upright flimestone Early PerKoyanagi (locally con(10 m2) ostrike to thplagioclaseunderlie limPermian, Mto SakmarconformabCarbonifer

Similabeen corrovaricolourerepresent Uolder arc collected fprovide a m

PermianPermia

bedded caris little or are very dare separatgrey chercarbonate. Permian A(Gunning between 50

Well beddMediu

typically wcorals, fengastropodsdebris may11) forminis proposedeterminatKoyanagi, from LatePermian tois supportwhich are tal., 1996 a1990 time

red wacke, porained turbiditilie the northeas

ht belong to thelonging to th. Arguments t can be made

nequivocally rthese rocks ofacing positiand further no

rmian limesto(1994). The mantains limesto

olistoliths of Che north, the ue phyric tuff mestone contaiMoscovian or rian fusulinac

ble volcaniclasrous age. ar contact andoborated in thed volcaniclaUpper Triassicstrata. Limest

for extraction omaximum age

n an sections arrbonate and leno evidence o

diverse in detaited herein: mart-carbonate, w

All of theseAmbition For

et al., 199400 and ~1100 m

ded grey andum grey to well bedded nestrate and bs and giant fuy dominate song packstones. ed for this utions from u

1994; Brownest Carbonifero Middle Permed by the octypically of Rhand Logan et ascale which la

olylithic volcaic sediments ast corner of thehis unit. Howhe Late Triass

for an Upp along strike trule out suchoccupy a struion above orthwest, appa

one as shownaroon to dark g

one cobble-richCarboniferous unit grades upwhich appear

ining Late Carbyounger corals

cean foraminifstic sequence o

d faunal relathe present studastic section c deposition atone granule

of conodonts. Ifor this unit.

e comprised osser chert. In m

of volcanic debil, three mappassive light grwell bedded

e units are cormation ~50 4), where its m.

d cream carbcream-colour

and fossiliferobranching bryousulinaceans arome layers (Fi

An Early to Mnit on the ba

units along st et al., 1996),rous (Gzhelia

mian (Roadian accurrence of ghodian to Wordal., 2000 used cked a Middle

anic conglomat least 900 m e Hoodoo Mounwever, we intesic succession per Carbonifeo the north anh arguments.

uctural, as wemid-Carbonife

arently dip benn by Logan green conglomh layers and

limestone. Apward into mars to conformboniferous or Es and late Assfers, suggestinof probable U

tionships havedy area whereis interpreted

and cannibalismconglomerate

If present, they

of massive to wmost sections bris. Although able Permian

rey carbonate, grey and c

orrelative withkm to the n

thickness ra

bonate red carbonateous. Large ruozoa, brachiopre common. Figure 6 and Fi

Middle Permianasis of fossil trike (Logan , where they ran) through Eand Wordian). giant fusulinacdian age. (Browthe Harland ePermian. As a

merate thick ntain

erpret (see

erous d we

For ll as erous neath

and merate

large Along aroon mably Early selian ng a

Upper

e not e the d to m of

was y will

well-there they units dark ream

h the north anges

e is ugose pods, Fossil igure n age

age and

range Early This

ceans wn et et al., a

Figusectilayer

consPerminclual., 2

Dar

tendBulbthickhalf whicsponnot abru

Mas

formbeddfragtypihornlengare centmapMid

Ear

age argisedicontelsewTria

ure 11. Bryozoanion. Silicified brars up to 30 cm th

sequence, theymian stage; botuded in the M2008)).

rk grey chertIrregularly be

ds to be relabous to hacklyk are crudely

f the thicknessch may be fenge spicules thbe identified

upt contact with

ssive light gr

Medium to cms massive, ligding. Most out

gments and thcally best presn corals may gth. Unlike Ca

generally lestimetres). In twp area, this unddle to Late Tri

rly to MiddlStrata interprcomprise a c

illite with thin,iment-starved tact with undwhere it may b

assic erosion.

n packstone withanching and fenehick.

y considered th Roadian and

Middle Permian

t and carbonedded dark gatively impovy, chert layers

stratiform ans of adjacent metid. Chert is phat could provi

in outcrop. Th overlying ma

rey carbonat

coarse crinoidght grey outcrotcrops contain

hey may be aserved where exceed 10 cm

arboniferous cs than 0.5 cm

wo localities nenit is overlainiassic age.

le Triassic eted to be of condensed sec, fetid limeston

package disderlying massbe entirely rem

in Early to Middleestrate bryozoan

Roadian to bd Wordian stagn (Okulitch, 19

ate grey chert andverished in m

and nodules ud are generallmicritic carbonpresumably sede a source of his unit appeaassive carbona

te

dal grainstone ops that lack aat least sparse

abundant is soreplaced by s

m diameter andarbonate, crinom diameter (ear the eastern n by strata int

Early to Middction of graphne and wacke splays a fausive Permian

moved by subs

e Permian fossils form

be an Early ges are now 999; Ogg et

d carbonate macrofossils. up to 30 cm ly less than nate layers, econdary as silica could

ars to be in ate.

commonly any obvious e horn coral ome layers, ilica. Fossil d 30 cm in oid ossicles (not several

edge of the terpreted as

dle Triassic hitic cherty layers. This

ult-modified carbonate,

equent Late

Geological Fieldwork 2010, Paper 2011-1 45

T

arhais (Fvoinprgrvo

La

warthteLadibew

L

unDcow

FideLa

riassic chert

Black and rrgillite comprias not been ob estimated to

Figure 12). Itolcanic layersnterbeds. Chertroportion (up rains that couldolcanic silt/san

aminated ca

Light grey well laminated lrgillite-dominahe marl layersentatively identate Triassic aimensions favoedding-perpend

weathering and

ate TriassicLate Triass

nits, particulaDistinctive coonglomerate oc

which they were

gure 12. View toeterminations areate Triassic age.

ty argillite

rust, well beddses a section served undeforhave a true th

is composeds with generaty layers are to ~10%) of

d be water lainnd source canno

rbonate

to black, poorlayers up to 20

ated section. Ats are packstontified as Daonege. Subequal our the latter idicular cleavagincomplete fos

c sic strata are darly polymictoarse biotite- ccurs together e derived. Aug

o the north of ruse pending). BlockTo the immediat

ded volcanic chthat is rarely rmed. The defo

hickness of lesd of 3-6 cm ally thinner scomprised of

f silt and sann tuff, althoughot be ruled out

rly indurated m0 cm thick witt one locality, anes of paper-ella or Halobiahinge-parallel dentification. U

ge typically resssil preservatio

dominated by tic boulder c

and K-felwith hypabyss

gite-phyric flow

sty black chert, aky olive-brown rote east, the unit i

hert and sooty exposed, and

ormed section s than ~40 m thick cherty

ooty argillite a significant

nd-sized lithic h an immature .

marl occurs as thin the chert-at least two of -thin bivalves a of Middle to

and -normal Unfortunately sults in slabbyon.

volcaniclastic conglomerate. ldspar-bearing sal rocks from ws, a hallmark

rgillite and grey cocks in the upperis underlain by m

of the Stuthan claspurple opoorly sopyroxene are oftenparticularAn intervclastic se~220 Ma.

TurbiditWell

mainly obut also outcrops turbidite 13a). Basstratificatwith depbeds conboulders pyroxene plagioclas(Figure 1

This presumedmetres acchert and

carbonate of inter third of the sect

massive grey lime

tuhini Group, atic rocks. Ther maroon; doorted chaotic

e crystal and ln characterizedrly recrystallizval of dacite asection yields a.

tic arkosic sel bedded turbf graded volc

include conof this unit

couplets are tysal scours and tion near beddposition from ntain subangul

of mediume and 20-2se) and angu3b). unit rests un

d Middle Tricross have besooty argillite

erpreted Early to tion are conglomestone of presum

are present, bue conglomerateominantly ma

groundmass lithic sand-sizd by clasts ofzed and/or fossh-flow occursa preliminary

ediments biditic sedimeanic sandstoneglomerate. Blt weather olitypically 1 to local developmding tops areturbidity curr

lar to roundegrained aug

25% fine toular intraforma

nconformably oiassic age. Oeen derived fe.

Late Triassic (?)meratic volcanic wmed Permian age

ut are less abue is variable,

atrix-supportedof plagioclas

zed grains. Hof sedimentary siliferous limes near the top U-Pb zircon a

ents are come- argillite coulocky, cliff-foive brown. G15 cm thick (Fment of ripple features conrents. Conglomd cobbles to gite-porphyry o medium-gational rip-up

on basinal strOlistostromal bfrom the unde

) age (fossil age wacke of presume.

undant green,

d in a se and orizons

units, estone. of the

age of

mprised uplets, orming Graded Figure cross-

nsistent merate

small (25%

grained clasts

rata of blocks erlying

ed

46 British Columbia Geological Survey

Figure 13a. couplets.

Figure 13b.angular intra

Augite-ph

An apthick of cois exposedsimilar chmapped ar1000 m this blocky wpyroxene care locallyintrapillowcomprise acalcite andlayers up tflows.

Feldspar-Green

and associatwo areas: and on sAngular, c

Typical Late Tria

Angular to rounaformational rip-u

hyric volcan

pparently contioarse, crowdedd on nunataks haracter extenrea, and couldick. This unit weathering. Cocomprises 15-3y well developw laminated a few per centd sparse chalceto several metr

-phyric breccn to grey weaated epiclastic Upper Twin G

outh and eascoarse breccia

assic turbiditic sa

ded augite porphup clasts.

ic and epicla

inuous section d augite-phyricnorth of Twind to the wesd represent a is light olive g

onspicuous, euh30% of flows aped with light

sediment. Ve by volume anedony. Well bres thick are in

cia and epicathering, feldsrocks are exte

Glacier in eastst flanks of a, without sig

andstone-argillite

hyry boulders an

astic rocks

more than ~3c flows and bren Glacier. Rockst, outside ofsection more

green to brownhedral, often z

and breccia. Pilgrey and silic

esicles commnd are infilled bedded maroonnterlayered with

lastic rocksspar-phyric breensively expost-central 104B/Verrett Moun

gnificant epicl

e

d

340m eccia ks of f the than

n and zoned llows ceous

monly with

n tuff h the

eccia ed in /14E, ntain. lastic

comTwiaugimedtrachHowpyrocarb5%,epidcoulcomand poly

Poly

104Bcongacroattaibrowin whighclastmatrof dincluvolcfeldbrowfossquarplagmedand two daci

Mar

200withLogwellturbgastaphatuffilocadeve

distiporpwithespe

mponents, is pain Glacier areaite- porphyritidium grained,hytic alignme

wever, grain oxene commobonate and chl, or rarely 15%dote alteration ld have been

mprise the domorange-weath

ymictic conglo

ymictic boul

The most wiB/14E is aglomerate. It oss the northernins a thickneswn weatheringwhich bouldershlighted. Congt-supported, brix of maroon decreasing relude: medium canic tuff, coardspar porphyrywn basalt, gsiliferous and ortz diorite, regioclase ±K-fedium- to coarsin upper parts clast types ar

ite tuff (Figure

roon tuff

Maroon to grm thick in th

h Carboniferougan and Koyanl indurated,

bidites and tropods, crinoianitic to fine g

fites occur closally contain acceloped beds arLithologies t

inctive layers wphyry flows, thin both Palecially “Late C

articularly wela where it is aic basalt. Typ, tabular feldent and comprsize ranges fonly accomplorite-filled ves%, of the unitand veining i

n derived fromminant clast typhering conglommerate unit.

lder conglom

despread unit a conspicuoucrops out in an half of the mss of at least g and forms ros of contrastingglomerates belout are more cash tuffite or t

lative abundanto fine graine

rse to medium y, fine grainegrey to whiteof presumed Pecycled congloeldspar porphyrse grained holof the unit, da

e recognized ae 14a).

reen water-lainhe northeasterus strata PnS

nagi map) whecoarse volcan

carbonate-ricids and bivalv

grained, lapilli ase to the top cretionary lapie typical. typical of thwithin several turbidite and leozoic and

Carboniferous (

ll displayed inassociated witpical lithologdspar that mrise 5-35% o

from fine to panies feldspasicles can comt. Chlorite, caris common. Clm this or simpe within the merate and p

merate

of the Stuhinus polymictia northwest-tr

map area where2000 m. It is

ounded outcropg lithology areonging to this uommonly supp

tuffaceous wacnce, common ed tabular feldgrained augite

ed to aphanitie limestone aleozoic age), omerate, coarsry, turbiditic wlocrystalline gacite and picriteabove a layer o

n tuff forms secrn map area (aSt, uCScg andere it grades upnic sandstonech conglomeves. Well beddand ash tuff to of the section

illi horizons. P

his unit alsoother units sucpolymictic coMesozoic sec

(?)” above).

n the upper th pillowed, ies contain

may display f the rock. coarse and

ar. Quartz, mprise up to rbonate and lasts, which milar units, dark brown

parts of the

ni Group in ic boulder rending belt e it probably

maroon to ps and cliffs e beautifully unit may be ported by a

cke. In order clast types

dspar-phyric and augite-ic green to (commonly hornblende

sely bladed wacke, pink granodiorite, e. The latter of ~220 Ma

ctions up to along strike d uCSt on pwards into

e and then erate with ded maroon,

plagioclase n and these

Planar, well-

occur as ch as augite onglomerate ctions (see

Geological Fieldwork 2010, Paper 2011-1 47

D

asboup~1wplcocmalriccobaupslladeLa

Khy

hyfebrchto

frdiinoclo“fastraofcrsewstyR

L

Dco

rococrmormdecobe

Dacitic ash flo

Crowded tash tuff comprisoulder conglompper layer atta130 m. It is a

weathering, relagioclase andomprise 35-40m diameter (Fltered biotite (ch, flattened fompacted durinanding is coppermost 1-3 ightly recessiv

apilli crystal etermination frate Triassic, ~2

K-feldspar meypabyssal ro

Texturally ypabyssal rockeldspar megacroad region wharacterized byo 25% of the ro

Locally, thragmental rockikes cut contemntrusive, extruccurrence is leocally display flowers” whichsh cloud or seachytic, crowdf vesicular glarowded K-feldeveral slight va

west-trending swtyle copper mi

Rocks”).

ate Triassic

Dark brown aonglomerate

Dark browounded, finelyonspicuous pinrystals derived

most places therange. Clasts

matrix of immaetrital biotite onglomerate pedded wacke (F

ow

abular feldspase two layers nmerate unit (

ains a thicknesa maroon and psistant unit. d lesser, co% of the unit

Figure 14b) co(~3%) and spafragments mayng partial welonspicuous inm of the uni

ve probable aash tuff. A

from a sample 220 Ma age (N

egacrystic tuocks

diverse tufks containing frysts are inte

within east-centy abundant detock. e K-feldspar ps clearly exist

mporaneous strsive and immss obvious (Fig

delicate glomh are unlikely tedimentary envded K-feldsparass (i.e. chilledspar porphyrariants of K-fewarms, some oineralization (s

c to Early Ju

nd orange-we, wacke and

wn conglomeray tabular fenk-orange syed from the une unit is carbare typically

ature sandstoneup to 1.5 c

passes laterallyFigure 16a) an

ar and quartz-ear the top of tFigure 14a).

sses of betweepinkish to greMedium gra

arser K-feldswith quartz e

omprising ~5%arse titanite. S

y have been pulding in an asn some fragit is a tan weairfall and rew

preliminary of this unit h

N. Joyce, unpub

uff, breccia a

ffaceous, fragfragments of syermittently exptral 104B/14Etrital biotite, c

porphyritic anas clastic dikesrata, the distinc

mature epiclastgure 15a). Hypmeroporphyritito have been prvironment. Somr porphyry disped; Figure 15bry comprises

eldspar megacrof which displsee later sectio

urassic

weathering coal

ate is dominaeldspar-phyric nite and coars

nit described pbonate-altered

supported by e containing ascm diameter. y or verticalld in places is tu

-phyric dacite the polymictic The thickest,

en ~80 m and ey and blockyained tabular spar together eyes up to 0.5%, with lesserSome crystal-umiceous and sh flow. Flow gments. The eathering and worked lithic isotopic age

has returned a blished).

nd

gmental and yenite and K-posed over a . This unit is

comprising up

nd biotite rich s. Where such ction between tic modes of pabyssal units ic K-feldspar reserved in an me bombs of play a mantle

b). This same one of the

rystic dikes in lay porphyry-on: “Intrusive

ated by well-clasts and

se K-feldspar previously. In and weathers a distinctive

s much as 5% Locally the

ly into well-uffaceous

Figure 14alight pink licooling unitan weathe

Figure 14b

with pinkcrystals. fragments

a. Polymictic conthic lapilli crystalit). An unconformering reworked tu

b. Close-up of qu

nk lapilli that Wacke layers

s. One distincti

nglomerate (abovl ash tuff (markin

mable contact is uff (at base of ice

uartz-phyric daci

include megs commonly ive fossilized p

ve ice axe) overling top of ash flowmarked by a layee axe).

te ash tuff.

gacrystic K-fecontain coaly plant includes a

ies

w er of

eldspar plant an

48 British Columbia Geological Survey

Ficr

de+5

Le

H

eaanM20Hneunapinrehalofowon

Fifrodereles

gure 17. Chloriterystal ash flow tuf

eterminations f.8

/-1.5 Ma and 1ewis, 2001).

oodoo tuff The young

astern Hoodoo nd wind-sorted

Mountain volca000). Flows w

Hoodoo Mountaear the toe nconformably phanitic and scn the high ridgeelicts of a presas not been remower elevation or glacier exten

work did not inn rock package

gure 18. Lapilli som the extinct Hoerived soils cap mestrict glacial ice ess than ~1240 m

e-altered hornbleff.

from the Betty 187.7 +5.3/-4.4 M

est volcanic rMountain are

d scoria of the anic complex (which have eain volcano areof western Toverly polydefcoriaceous lapies in the westesumably once cmoved by rainextent of thesents at the time

nclude such maes of importanc

sized, pumiceousoodoo Mountain many of the ridgeextents at the tim

m (less than 240 m

ende ±biotite and

Creek FormatMa (U-Pb, abra

rocks identifiea are flows, unca. 28 to 180

(Figure 18; Edemanated frome exceptionallyTwin Glacier formed rocks. illi and ash oc

ern part of the acontinuous blan, wind or ice.e relicts could pe of eruption; apping, as we ce for mineral e

s scoria, probablvolcano. These

es in western 104me of eruption to m above its curre

d feldspar

ion are: 187.7 aided zircons;

ed within the n-lithified soil 0 Ka Hoodoo dwards et al., m the extinct y well exposed

where they Tan to brown

ccupy hollows area and form anket where it Mapping the provide limits however, our have focused

exploration.

ly originating deposits and 4B/14E and an elevation of

ent level).

Preliminasamples cEdwards error limVilleneuv

INTRUSThre

cut stratithese, deRiver valthe Verrevolumino

Verrett p

Grapvalley. W(2000) whHoodoo Mtan and ruoutcrops. intergrowturbid duAnhedral rock. In pcataclasisand int?Carbonifangle anadjacent correlatedsuite (LogCarbonifeHoodoo mage. If theVerrett PlAn isotopis pending

Figure 19.age. Note clight 4 mm

ary 40Ar/39Ar acollected at Het al. (2000) a

mits on persve, 1998).

SIVE ROCe main intrusivigraphy withineformed granitlley and an unett River to T

ous (Figure 3).

pluton - grap

phic granite is eWe follow theho called it theMountain map rust weathering It is compose

wn quartz and Kue to alteratiol pyrite grains places the bodys. Contacts witrusive. Its ferous volcani

nd locally disto country roc

d with the Latgan et al., 200erous volcanicmap area (Figese contact relaluton must be pic age determg.

. Verrett pluton gclastic texture alfield of view.

age determinaHoodoo Mountas ranging fromsonal commu

KS ve units and sen the Hoodoo te exposed inndeformed pluTwin River, a

phic granite

exposed in thee nomenclature Verrett Plutonarea, the Verr

g, forming bloed mainly of sK-feldspar (Figon to white m

locally comprdy appears clasith adjacent un

northern ic and sedimensplays a narrck. Verrett plute Devonian F00). It is undatc rocks, as itgure 3), it canations are corrat least as youn

mination from a

graphic granite ofong left margin i

ations from votain are reportm 28 to 1800 Kunication from

everal suites ofMountain are

n the upper Vuton extendingare by far the

e upper Verrettre of Logan n. Within the e

rett pluton is wcky to low, rosubequal amougure 19). Felds

mica and carbrise up to 3% stic, due to strunits are both fcontact cro

ntary bedding arow chilled muton was tenta

Forrest Kerr plted, but if it int appears to

nnot be Devonrectly interpreteng as Carbonifa sample of th

f interpreted Devn this cross pola

olcanic ted by Ka (no m M.

f dikes ea. Of Verrett g from e most

t River et al.

eastern white to ounded unts of spar is

bonate. of the

uctural faulted osscuts at high margin atively lutonic ntrudes in the

nian in ed, the ferous.

his unit

vonian arized

50 British Columbia Geological Survey

Biotite-ric

Dark clast- ±xencut across and easternmay be plublocky, hPhenocryst5%, K-felapatite andfeldspar (±occurring modes: oldpleochroic expanded second arpleochroic commonlymedium gpleochroic euhedral bglomerocryOutsized, b

Figure 20a. xenocryst of

Figure 20b.matrix.

ch diatreme

grey-brown wnocryst-rich bi

Mesozoic andn 104B/14E. Wucked from rubhighly compats include: biotdspar 5% witd opaque grain±feldspathoidsas patches. B

dest are coarscrystals alte

basal plates wre medium

elongate ay kinked or wgrained, zoned

crystals that booklets. Pyroxysts, euhedral bright green py

Dense and comf bright green pyr

Where weathere

weathering diiotite syenite (d Paleozoic stWhere weatherbbly debris, buact, and diftite ~25%, diopth minor aegirns. Matrix min

(?)) and up Biotite occursse grained darered by carbowith abundant

grained, goldand ragged warped, yound, dark browcommonly oc

xene is brightcrystals and

yroxene crystal

mpact biotite syenroxene, probably

ed, milled clasts

ike-like bodie(Figures 20a, trata within cered, rounded ct fresh outcropfficult to bpsidic (?) pyrorine and acces

neralogy is 40%to 20% carbo

s as three disrk brown to bonate and haopaque inclusden to greencrystals that

ngest are finewn to dark gccur as clustert green and occrystal fragm

ls are interprete

nite containing a y chrome diopsid

fall from the intru

es of b, c)

entral clasts ps are reak.

oxene ssory % K-onate stinct black aving sions, n-tan

are e- to green rs of ccurs

ments. ed

large

de.

usive

Figubiotitphendiopssamp

as ccrysidenfeldCarldomindiemp

assodikepyrotuffameg

Mesgra

melathat Verrinteralter(Figand alterand com

melamarphasleucRivemelaage.lithoas E

ure 20c. Photomite (Bt1, 2, 3), a manocryst of aegirinside (Di). Plane pple MMI10-18-9.

chrome diopsidstal disequilibrntification awadspar phenocrylsbad twins

minantly pink icating signiplacement.

Biotite-rich dociated with Kes. These dikoclastic eruptifaceous equivgacrystic tuff an

sozoic to Ternodiorite

Light to darkano-granodiori

extends northrett. Hornblergrown forminrnating hornb

gures 21a, b). Fboth hornblen

red. Fine miaroquartz and in

mmonly occurs No age has

ano-granodiorirgin of the Twse of the plutcocratic granoder pluton as Eoano-granodiori. A persistentologically simiEarly Jurassic.

Bt1

Bt2

Bt3

icrograph showintrix of K-feldspar

ne (Aeg), and a xpolarized light vi.

de xenocrysts; rium is seen aits microana

ysts range up tor glomero

syenite and mificant milli

diatreme dikesK-feldspar megkes probably ions as evidvalents founnd related rock

rtiary varitex

k grey, blockyite forms an th from the soende and plang fine graineblende and quFeldspar may nde and subordolitic cavities mnfilled with chnear the margibeen determi

ite; however, iwin River plutoton which hasdiorite. Previoocene in age. Yite are interpret set of severilar and cuts st

Bt2

Kf

ng multiple gener (Kf) and carbonxenocryst (?) fragew of ~2 mm fiel

although no in thin sectio

alytical investito 1.5 cm andocrysts. Xenmay be highling during

s are commongacrystic dikes

occupied venenced by the

nd in the ks.

xtured melan

y weathering irregularly-sh

outheast flankagioclase are ed to pegmatituartz-feldspar-be altered to w

dinate biotite amay be lined whlorite. Secondins of accessorined for the vit conforms to on and may bs been intrudeous maps showYoungest rocketed to be of Lral metre thictrata that may b

Bt3

Di

Cc

Cc

rations of

nate (Cc), a gment of ld of view of

evidence of on. Positive igation. K-d may form noliths are ly spherical

diatreme

nly spatially s or breccia nts feeding e extrusive

K-feldspar

no-

hornblende haped body k of Mount randomly

tic zones or -rich layers white mica, are chlorite-

with feldspar dary calcite ry titanite. varitextured the eastern

e an earlier ed by more w the Twin ks cut by the Late Triassic ck dikes is be as young

Aegc

Geological Fieldwork 2010, Paper 2011-1 51

Fipeho

Fico

E

biplRRex

anhoeuoscounscgrThplmmna

gure 21a. Textuegmatitic zone wornblende within

gure 21b. Textuompositional ban

ocene Twin

Light grey iotite granodioluton; the large

River pluton, iRiver. A comxposed 15 km f

The most and pepper granornblende (5-1uhedral biotitscillatory reveontent of ~An2niform with thcreens and coranodiorite, whhermal metamluton extends

mapped contactmineralized wi

ative gold.

ral variability in hith intergrowths otexturally diverse

ural variability in hding and includin

River granod

to white weathorite forms a 5est in the map at extends from

mpositionally farther to the nabundant phasenodiorite that 0%, some wit

te booklets erse zoned w27-30. Composithe exception oontact zones, hich may be x

morphism attrifor several

ts. Schistose roth chalcopyrit

hornblende granoof K-feldspar plae melano-granod

hornblende granng pegmatitic zo

diorite

hering, blocky0 km2, northwarea. Herein cam Mount Versimilar, satell

northwest. e is a mediumcontains blackth biotite in co(10-15%). Pl

with an averation of the bodf contorted ho

especially wxenoliths-rich ibuted to the hundred met

ocks south of tte and possib

odiorite: gioclase and diorite.

odiorite: nes.

y, hornblende-west-elongated alled the Twin rrett to Twin lite stock is

m grained, salt k and vitreous ores) and sub-lagioclase is age anorthite dy tends to be ornblende-rich with melano-(Figure 21c). Twin River

tres from its the pluton are bly traces of

Figure 21ccontact zonxenoliths o

ECONO

PreviouMine

area in thone ton s2.05 gramcopper (CfocussingdiscoveriemineralizSmelting vended th(Gifford, Reg/StonJohnny Msilver, 2kilogramsveins at milled beMINFILEResourceapproximproperty, Between32.093 msilver andmillion to

NorthgeologicaNewmontin 1972. and in thiron skamegacrysshowingsMcLymoncover aucovering

c. Textural variabne with Twin Riv

of hornblende gra

OMIC GEO

us Exploratieral claims werhe early 1900sshipment of J

ams gold, 1.3Clothier, 1918

g primarily soues of high gr

zed float in 1Ltd. (Pickaxe)

he Inel proper1980) who ex

nehouse properMountain Mine2.81 million s of copper frothe Stonehou

efore shutting dE, 2010). At es Corp. and mately a million

about 5 km no1991 and 1

million grams d 249 276 kiloonnes of ore (Bh of the Iskutal mapping t Mining CorpIt was the era

his region effoarn mineralizstic syenite ins. Gulf Intent claims souuriferous skar

the Dirk and

bility in hornblendver granodiorite (anodiorite.

OLOGY

tion re first recordes followed sho

Johnny Mount37 kilograms 8). Subsequenuth of the Iskurade auriferou1954 by Huds). In 1969, R. G

rty to Skyline xplored and devrties. From 198e produced 4.3grams of go

om steep dilatuse deposit frdown due to loabout the sa

Cominco Ln tonnes of 27orth of the Joh999, the Snipof gold, 12.18ograms of cop

BC MINFILE, 2ut River, a ma

program waporation of Cana of copper po

orts were direczation associantrusions on ernational Miuth of Newmorn mineralizad Newmont L

de granodiorite: light matrix) is ric

ed for the Iskutortly thereafterain ore that ysilver and 1

nt exploration ut River began

us massive suson Bay MiniGifford restakeExploration Lveloped the In88-90 and 19934 million graold and 1 00tational quartz-rom 225 247 tow metal price

ame time, DelLtd. had delin7 g/t Au on thehnny Mountain p deposit pro83 million grapper from abo2010). ajor exploratioas undertake

nada Ltd. (Neworphyry explo

cted towards cated with fethe Dirk and

inerals stakedont Lake in 19ation. Recent Lake areas has

ch in

t River r by a

yielded 2.45%

work n with

ulphide ing & ed and

Limited nel and 93, the ams of 08 000 -pyrite tonnes es (BC laware neated e Snip Mine.

oduced ams of out 1.2

on and n by

wmont) ration, opper-

eldspar d Ken d the 986 to

work s been

52 British Columbia Geological Survey

conducted by Romios Gold Resources (Ray, 2006; Bernales et al., 2008; Chadwick and Close, 2009).

Late Triassic Copper Mountain Intrusive-Related

Copper, gold and silver mineralization at the Dirk, Telena and Birthday Jim prospects is related to a regionally extensive Latest Triassic alkaline magmatic event, the Copper Mountain Plutonic Suite (Woodsworth et al., 1992). This magmatic event is causative to porphyry mineralization along the length of British Columbia. In the northwest, related mineralization is found at Galore Creek, Red Chris and GJ. In central and southern BC, related deposits include Mount Polley, Afton and Copper Mountain.

Dirk Showing (MINFILE 104B 114)

In 1972, Newmont carried out geological mapping, airborne and ground magnetometer surveys and drilled six holes totalling 93.87 m. Three holes were drilled at each of the Dirk and Ken claims using a Winkie drill and “A” drill string (the Ken zone is located 5.5 km east of the Dirk on NTS map sheet 104B/15, east of the study area that we report on here). It was concluded then that the Winkie drill was an ineffective tool for sampling these zones (Costin, 1973). In 2009, Romios Gold Resources conducted followed up geological investigations (Chadwick and Close, 2009) and sampling of the mineralization on two of the known mineral showings: the Dirk and Telena zones, which are separated by a kilometre-wide expanse of glacier.

The Dirk prospect occupies the eastern margin of an alkaline intrusive center more than 3 by 4 km in size. The intrusive centre is a swarm of easterly-trending sills and dikes as well as stock-like bodies of texturally variable, porphyritic and equigranular syenite containing orthoclase ±pseudoleucite. K-feldspar porphyry bodies are identical to the Late Triassic "rhomb porphyries" of the alkaline feldspar porphyry intrusive suites at Galore Creek, located 40 km to the northwest. Crystallization ages of the intrusions at Galore Creek range from 210.2 ±1.0 Ma (U/Pb, titanite; Mortensen et al., 1995) for a syn-mineral dike to 208.8 ±0.8 Ma (U/Pb, zircon; Logan, unpublished) for a post-mineral dike. The Dirk intrusions, like those at Galore, are silica-under saturated, syenite and foid-bearing syenite characterized by centimetre-scale megacrysts of orthoclase and smaller phenocrysts of biotite, sodic pyroxene, hornblende, apatite, magnetite, and titanite. They are variably altered, containing assemblages of andradite garnet, epidote, clinozoisite, secondary biotite, chlorite, calcite and anhydrite (?). Diatreme bodies containing breccia fragments of distinctive porphyritic syenite and bright green pyroxene form part of this magmatic suite and are cut by younger syenite dikes containing coarse orthoclase crystals.

The main Dirk showing is an east trending eight metre wide skarn zone of patchy bornite, covellite and

chalcopyrite ±pyrite mineralization replacing limestone adjacent to pink, potassium feldspar-phyric syenite dikes. Sulphides occupy millimetres thick veinlets and irregular patches locally with magnetite and/or andradite, epidote and albitic (?) alteration. Metal assemblages of economic interest include chalcopyrite ±gold. Alteration assemblages (i.e. magnetite, specular hematite, andradite and epidote) infer a highly oxidizing character of the main hydrothermal event. Late stage iron carbonate and barite veins are common at the Dirk and Telena zones. Eight, 1 m chip samples taken along a north-south traverse across the main Dirk showing returned 2.9% Cu and 0.64 g/t Au (Chadwick and Close, 2009). Additional copper-gold mineralization has been recognized 200 m southeast of the main zone and a 3.0 m chip sample from this mineralized section assayed 6.21% Cu and 0.57 g/t Au (Chadwick and Close, 2009). A sample collected during the course of our mapping contained >1% Cu, 5 ppm Ag, 0.6 ppm Au and 0.38% Zn (see sample 10JLO-254, Tables 1 and 2).

Telena Showing

Mineralization at the Telena showing is described as a 40 by 40 m cliff exposure of disseminated and vein chalcopyrite with intermittent bornite-bearing breccias within a syenite porphyry (Chadwick and Close, 2009). A reported grab sample from the Telena Zone assayed 2.07% Cu and 0.97 g/t Au. Two samples were collected during the course of our mapping. These are representative of the two ends of the spectrum of mineralized K-feldspar porphyritic rocks. One sample was collected from largest of many irregular patches and veins of semi-massive chalcopyrite (~0.25 by 1.1 m) within a strongly copper-stained, brecciated and skarnified coarse K-feldspar and calcite amygdaloidal porphyry. A second sample was collected from a relatively poorly mineralized dike at least 4 m thick, which cuts across the unit from which the first sample was collected. This dike contains medium to coarse K-feldspar phenocrysts. Notable results from analysis of these two samples are: Cu, >10 000 ppm, 1058 ppm; Au, 4.1 ppm, 0.1 ppm; Ag, 15.5 ppm, 0.7 ppm; Pd, 64 ppb, 27 ppb; Pt, 21 ppb, 3 ppb (samples MMI10-18-11 and MMI10-18-11b, Table 1).

About 650 m southwest of the Telena is a 2 km long, west-trending nunatak. It largely underlain by an east-northeast striking dike swarm of calc-potassic altered megacrystic potassium feldspar syenite dikes which abut against and intrude a large olistostromal block of thick bedded recrystallized limestone forming the eastern end of the nunatak. Brecciated, white orthoclase flooded syenite porphyries overprinted and replaced by brown or green euhedral zoned andradite garnet, anhydrite, traces of malachite and late carbonate attest to a vigorous magmatic/hydrothermal centre.

Geological Fieldwork 2010, Paper 2011-1 53

Tabl

e 1.

Sel

ecte

d el

emen

ts fr

om In

duct

ivel

y C

oupl

ed M

ass

Spe

ctro

grap

hic

anal

yses

(IC

PM

S) o

f sam

ples

col

lect

ed in

the

Hoo

doo

Mou

ntai

n ar

ea. F

or e

ntire

da

tase

t see

Mih

alyn

uk e

t al.

(201

1b).

Sam

pleN

umbe

rLa

titud

eLo

ngitu

deLa

b Nu

mbe

rA

gA

sA

uBa

BiC

dC

eC

oC

sC

uFe

Ga

HgK

Mn

Mo

PbPd

PtS

SeTe

ThY

ZnZr

Dete

ctio

n Li

mit

20.

10.

20.

50.

020.

010.

10.

10.

020.

010.

010.

15

0.01

10.

010.

0110

20.

020.

10.

020.

10.

010.

10.

1

Mea

sure

uni

tPP

BPP

MPP

BPP

MPP

MPP

MPP

MPP

MPP

MPP

M%

PPM

PPB

%PP

MPP

MPP

MPP

BPP

B%

PPM

PPM

PPM

PPM

PPM

PPM

10JL

O-1

6156

.909

3-1

31.0

831

6212

126

037

.127

.950

.11.

971.

4131

.717

.10.

3669

.37

4.3

7.1

900.

1687

90.

6616

.3<1

04

2.75

1.6

0.18

2.6

1020

3.4

2.2

10JL

O-1

6156

.909

3-1

31.0

831

6212

127

636

.624

.750

.22.

051.

3831

.517

.10.

469

.59

4.38

7.1

700.

1589

40.

6117

.28

<10

42.

741.

30.

22.

79.

9321

1.1

2.4

10JL

O-1

8256

.881

9-1

31.0

340

6212

238

3923

.264

03.5

22.4

0.26

0.08

5.4

12.1

0.04

5153

.48

6.63

4.8

171

<0.0

116

982.

051.

89<1

04

0.23

0.3

0.05

0.6

7.94

33.1

5.4

10JL

O-2

5456

.871

3-1

31.0

280

6212

350

4920

8.7

625.

311

.50.

4810

2.9

602.

50.

11>1

0000

.00

23.3

63.

929

570

<0.0

123

925.

0722

.248

<20.

042.

30.

260.

22.

0238

19.3

1.3

10JL

O-2

7856

.707

1-1

31.1

140

6212

423

534

85.3

2113

.955

.553

.39

1.68

1.8

102.

0438

1.68

14.7

86.

555

0.98

335

9.3

516.

24<1

0<2

5.05

33.4

18.0

80.

23.

0521

90.

3

MM

I10-

1-05

58.7

571

-133

.705

762

125

160.

67.

427

0.03

0.12

0.4

20.5

0.09

8.09

3.83

7<5

0.03

1523

0.12

3.32

<10

<20.

08<0

.1<0

.02

<0.1

5.06

37.3

<0.1

MM

I10-

12-0

856

.821

0-1

31.1

433

6212

674

9711

.117

54.8

61.9

1.87

3.34

5.7

20.4

5.28

1567

.05

6.9

12.9

542.

4510

191.

36.

38<1

0<2

1.88

1.6

0.45

0.7

8.86

184.

30.

9

MM

I10-

12-1

256

.817

5-1

31.1

558

6212

710

14.

36.

615

1.4

0.08

0.07

16.5

9.5

1.44

38.5

3.29

2.1

120.

210

073.

412.

73<1

0<2

0.33

<0.1

<0.0

22.

510

.39

60.1

0.3

MM

I10-

13-0

756

.828

1-1

31.1

684

6212

824

5.3

2.8

17.3

<0.0

20.

313.

80.

9<0

.02

23.5

70.

363.

630

0.01

548

0.12

5.13

<10

<20.

03<0

.1<0

.02

0.5

1.84

66.

3

MM

I10-

13-1

256

.832

1-1

31.1

570

6212

916

83.

12.

161

.60.

120.

031.

627

.90.

529

.56

2.81

0.5

636

0.19

70.

880.

77<1

0<2

2.96

0.1

<0.0

21

1.32

3.5

5.4

MM

I10-

14-0

956

.747

3-1

31.0

294

6213

010

393.

16.

711

1.2

0.28

0.05

8.2

12.3

3.07

233.

653.

267.

714

0.63

921.

016.

5310

21.

950.

70.

260.

51.

9517

.81.

1

MM

I10-

16-1

056

.979

7-1

31.0

662

6213

158

43<0

.15

717.

60.

3814

.01

16.3

6.4

0.14

1616

.02

1.8

4.8

1557

0.06

147

0.47

33.3

4<1

0<2

0.04

2.4

<0.0

20.

37.

1240

44.1

1.4

MM

I10-

16-1

0b56

.979

7-1

31.0

662

6213

259

700.

34.

674

20.

3714

.47

16.6

6.5

0.14

1668

.12

1.84

4.9

1564

0.06

146

0.43

33.0

321

<20.

042.

3<0

.02

0.3

7.53

4168

.11.

3

MM

I10-

16-1

0b56

.979

7-1

31.0

662

6213

262

23<0

.14.

576

10.

3914

.62

17.1

6.6

0.16

1719

.17

1.91

5.3

1644

0.06

153

0.48

34.8

138

<20.

042.

3<0

.02

0.4

7.69

4297

.51.

5

MM

I10-

18-0

756

.881

1-1

31.0

332

6213

341

78.

215

3.1

112

0.4

0.04

6.7

25.1

0.09

4474

.48

8.03

0.7

1497

0.03

633

3.75

1.64

<10

<20.

750.

50.

08<0

.15.

49.

31.

1

MM

I10-

18-1

156

.860

4-1

31.0

384

6213

415

522

208.

441

10.6

55.3

2.08

0.23

30.1

377

0.37

>100

00.0

015

.92

11.2

469

<0.0

123

4922

.65

15.8

964

211.

5728

.61.

130.

515

.92

120.

22.

5

MM

I10-

18-1

1b56

.860

4-1

31.0

384

6213

573

710

.513

6.8

13.7

0.55

0.18

60.4

74.8

1.16

1058

7.18

4.2

920.

0532

132.

1212

.427

32.

275.

80.

331.

433

.68

543

MM

I10-

20-1

256

.820

1-1

31.0

190

6213

616

5416

.980

.814

5.3

2.41

0.18

4.5

36.7

1.22

584.

014.

982.

214

40.

3416

314.

145.

14<1

03

1.31

11

0.2

7.46

42.8

0.9

MM

I10-

20-1

2b56

.820

1-1

31.0

190

6213

715

657

63.2

736.

630

.849

.50.

222.

537

.80.

3724

90.9

211

.72

8.4

137

0.17

418

24.9

79.

33<1

0<2

5.94

7.3

28.4

70.

43.

6177

.91.

3

MM

I10-

20-1

356

.820

8-1

31.0

201

6213

844

123

.7<0

.246

.10.

410.

086.

66.

90.

6110

64.3

92.

390.

720

0.19

1713

1.48

5.1

<10

<20.

530.

70.

050.

29.

1715

.10.

4

MM

I10-

22-0

656

.821

6-1

31.0

214

6213

910

03.

22.

412

4.3

0.06

0.04

27.

30.

1631

1.75

2.86

0.4

80.

0938

71.

51.

21<1

0<2

0.59

0.2

0.02

<0.1

1.73

6.3

0.3

MM

I10-

24-0

356

.759

8-1

31.1

858

6214

026

06

6.7

46.2

0.07

0.07

2.9

17.4

1.22

249.

872.

253.

718

0.29

393

0.83

9.72

<10

40.

610.

30.

030.

34.

0723

.61.

3

MM

I10-

24-0

456

.706

7-1

31.1

142

6214

130

790.

236

8.5

128.

32.

430.

055.

231

.18.

0820

00.9

47.

1313

.1<5

2.76

701

88.1

61.

8113

<21.

784.

61.

480.

53.

8774

.30.

4

MM

I10-

24-0

556

.707

0-1

31.1

141

6214

271

3922

.888

5.2

78.5

15.6

50.

236.

210

.74.

5941

51.7

24.

166.

918

1.57

454

25.0

12.

3<1

02

2.22

7.7

5.96

1.3

9.11

43.5

0.5

MM

I10-

24-0

656

.678

5-1

31.0

937

6214

354

9519

7.9

584.

632

31.8

10.

265.

121

.32.

5715

28.4

214

.86

8.7

220.

9942

613

8.42

10.8

411

2>1

0.00

35.4

7.4

0.5

5.89

41.1

0.9

6214

416

1965

.329

.527

5.5

0.3

0.76

27.9

49.4

0.56

175.

557.

619.

536

90.

0516

040.

9223

6.26

<10

<2<0

.02

0.7

0.34

3.6

13.0

435

0.4

3.2

STD

DS7

1020

51.7

87.6

425.

25.

16.

4139

.99.

66.

5910

3.9

2.41

4.8

219

0.46

634

22.2

874

8339

0.21

3.3

1.39

56.

2339

35.

9

BLK

<2<0

.1<0

.2<0

.5<0

.02

<0.0

1<0

.1<0

.1<0

.02

<0.0

1<0

.01

<0.1

<5<0

.01

<1<0

.01

<0.0

1<1

0<2

<0.0

2<0

.1<0

.02

<0.1

<0.0

1<0

.1<0

.1

Stan

dard

BCG

S till

Stan

dard

DS7

Blan

k

Refe

renc

e M

ater

ials

54 British Columbia Geological Survey

Tabl

e 2.

Sel

ecte

d el

emen

ts fr

om In

stru

men

tal N

eutro

n A

ctiv

atio

n A

naly

sis

(INA

A) o

f sam

ples

col

lect

ed in

the

Hoo

doo

Mou

ntai

n ar

ea. F

or e

ntire

dat

aset

see

M

ihal

ynuk

et a

l. (2

011b

).

Sam

pleN

umbe

rLa

titud

eLo

ngitu

deLa

b Nu

mbe

rA

uA

gA

sBa

Ca

Co

Cr

Cs

FeHf

HgM

oNa

NiRb

SbSc

SeTh

UW

ZnLa

Ce

NdSm

EuTb

YbLu

Mas

s

Dete

ctio

n Li

mit

ppb

ppm

ppm

ppm

%pp

mpp

mpp

m%

ppm

ppm

ppm

%pp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mpp

mg

Mea

sure

uni

t5

52

100

15

102

0.02

11

50.

0550

300.

20.

15

0.5

0.5

450

13

50.

10.

20.

50.

20.

05

10JL

O-1

6156

.909

3-1

31.0

831

6212

1<

5<

542

2000

< 1

1450

< 2

4.41

< 1

< 1

132.

32<

5014

02.

711

.3<

55.

3<

0.5

< 4

290

1840

< 5

2.5

< 0.

2<

0.5

1.5

0.32

35.2

10JL

O-1

8256

.881

9-1

31.0

340

6212

268

10<

535

700

1214

70<

214

.4<

1<

1<

50.

05<

50<

302

5.8

< 5

< 0.

5<

0.5

139

706

< 3

< 5

1<

0.2

< 0.

51

0.14

36.3

10JL

O-2

5456

.871

3-1

31.0

280

6212

356

0<

523

850

0<

162

360

< 2

51.5

< 1

26<

5<

0.05

< 50

< 30

6.4

0.7

11<

0.5

< 0.

511

4520

4<

3<

50.

3<

0.2

< 0.

5<

0.2

< 0.

0545

.2

10JL

O-2

7856

.707

1-1

31.1

140

6212

419

8025

9012

002

1022

04

13.2

22

< 5

0.34

< 50

< 30

1.2

11.6

251.

42.

99

240

714

171.

40.

7<

0.5

1.4

0.29

45.2

MM

I10-

1-05

58.7

571

-133

.705

762

125

< 5

< 5

< 2

< 10

011

2213

0<

24.

75<

1<

1<

51.

78<

50<

30<

0.2

24.6

< 5

< 0.

5<

0.5

< 4

< 50

18

< 5

0.7

0.5

< 0.

52

0.3

33.1

MM

I10-

12-0

856

.821

0-1

31.1

433

6212

624

009

1814

00<

122

406

7.01

2<

1<

51.

96<

50<

309.

818

.6<

53.

83

< 4

< 50

1434

< 5

3.3

< 0.

2<

0.5

2.7

0.41

34.5

MM

I10-

12-1

256

.817

5-1

31.1

558

6212

7<

5<

5<

240

04

1050

< 2

3.31

1<

1<

50.

25<

5050

1.5

13.6

< 5

4.1

3.1

< 4

8012

2514

2.3

0.7

< 0.

52.

40.

2736

.3

MM

I10-

13-0

756

.828

1-1

31.1

684

6212

8<

5<

532

300

11<

510

0<

22.

121

< 1

< 5

0.16

< 50

< 30

37.

7<

52.

5<

0.5

< 4

607

12<

51

0.4

< 0.

50.

6<

0.05

42.3

MM

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Geological Fieldwork 2010, Paper 2011-1 55

B

kmberenoMnopogrlimsiricm(ulatharlimMofthmmansanosa3.

E

V

sosetupebr

Fiphheoc

Birthday Jim

The Birthdam north of the een known at ecorded duringorth from

Mineralization iorth-dipping olylithic volcarained siltstonmestone. Intrulls of fine graich biotite phyr

megacrystic syeunits describedaminated and dhe diatreme, bure more diffumestone xenol

Mineralization of limestone xehe syenite

mineralization imagnetite, andrand malachite (amples of specotable of the anample 10JLO-.8 ppm Ag and

Early Carbon

Verrett rhyolitAn unnam

ource of Verretedimentary secuffite containineperite sills thareccia units. Pr

gure 22a. Skarnhotomicrograph oematite which is ccurs outside the

Showing

ay Jim showingDirk. Specularthis locality fo

g property scalthe Dirk pis set in a pacvolcaniclastic anic conglomne, cherty a

uding the beddned pink weath

ric syenite and enite porphyryd previously). displays chilledut where it intruse because iths and is oveoccurs as veinenoliths within

contact, wis dominated badite garnet an(Figures 22a, cularite-chalconalytical result182 (Table 1)

d 6.4 ppm Au.

niferous - V

te ed east-flowintt River. Northction compriseng sulphide cat pass up sectreliminary U-P

n mineralization aof reflected light venclosed by late

e ~5 mm field of v

g is located apprite skarn mineor nearly 40 yle mapping whprospect (Cockage of south

rocks, inclumerate, sandsto

argillite and ded sequence ahering syenite a coarse potas

y clast-dominaThe syenite isd margins wherudes limestonthe dike has

erprinted by skns and patchy n the syenite owithin limestby specular hend epidote withb). We collecpyrite mineralts were those owhich returne

VHMS

ng glacier is h of this glaciered of well belasts (Figures tion into rhyol

Pb age determin

at the Birthday Jiview of bladed s chalcopyrite. Acview.

proximately 1 eralization has ears, and was hich extended ostin, 1973). hwest-striking, uding coarse one and fine

fossiliferous are dikes and and xenolith-

ssium feldspar ated diatreme s locally flow ere it intrudes e the contacts s assimilated arn alteration. replacements

or adjacent to tone. Skarn ematite, lesser h chalcopyrite cted two grab lization. Most obtained from ed 0.5 % Cu,

the northern r is a volcano-dded rhyolite 23a, b) and

lite lapilli and nations on

m occurrence: pecular

ccessory pyrite

Figure 22bquartz and

Figure 23a

zircons s~340 Ma rhyolite Sulphide occurringbreccia zoveins of envelopedOn its wmodified volcanic relicts of

b. Skarn minerald hematite replac

a. Well bedded r

separated from(the same prein the northeveins are com

g as irregular ones (Figure 2chlorite-carbond by decimetr

western side, thcontact withsediments. A

f a barite-chal

ization at the Birce colonial corals

hyolite tuffite wit

m this rhyoliteeliminary age aeast corner o

mmon within thpyrite-chalcop

23c) and as 1 tnate-euhedral

re wide carbonhe succession h rust, tan aAt this contaclcopyrite layer

rthday Jim occurrs.

h sulphide clasts

indicate an aas determined fof the map she overlying rhpyrite veins ito 5 cm thick, pyrite ±chalco

nate alteration shares a struct

and black turct are fault-sr up to ~5 cm

rence:

s.

age of for the sheet).

hyolite, in late planar

opyrite halos. turally

rbiditic striated

thick

56 British Columbia Geological Survey

Figure 23b.

Figure 23c. lesser chalc

(Figure 24Approximastrata the smaroon interbeddeSome jasppyrite andlayers coul

Baritelayers are If the Fe-rithey repenvironmesignificant within the be related strike lengt

Andrei rhPerhap

encounteresign of havoccurs in aflows and h

Well bedded rhy

Well bedded rhyopyrite.

4a) at the struately 100 m asection become

tuffite contd with irregulperoid boulded chalcopyrite ld not be found, chalcopyriteall features ofich tuff – jaspe

present activent in which ch

mineral explstratigraphy aband, if so, rep

th.

hyolite ps the mosted during the 2ving been looka section of felshyaloclastite, a

yolite tuffite is loc

yolite tuffite with

uctural base ofabove the contes more tuffaceaining magnar jasperoid lars contain str(Figure 24c)

d in place. e, magnetite f productive Ver layers are e

ve subaqueohalcopyrite is loration targetbout 1.5 km topresents a targ

t inconspicuo010 mapping cked at previousic flows and tand immature v

cally brecciated.

infillings of pyrite

f the rhyolite tact with turbi

eous with greennetite-rich laayers (Figure 2ratiform layer), but chalcop

layers and jaVMS environm

xhalative in orous hydrothe

accumulating,t. Jasperoid lao the southeast get with signif

ous mineralizcampaign show

usly. Mineraliztuff, pillowed mvolcanic sedim

e and

tuff. iditic n and ayers 24b). rs of pyrite

asper ments.

rigin, ermal , and ayers may

ficant

ation ws no ation

mafic ments

Figugrainbarit

Figubeddlayer

inCarbmapprelMinchalcoveglomfeldblac

ure 24a. The struned turbiditic sedtic argillite with ch

ure 24b. Stratigraded tuffite with mrs.

the northeastboniferous agepped by (Logliminary isotoneralization lcopyrite and ellite-bornite merocrysts or dspar-phyric unck, irregular qu

ucturally modifieddiments and coarhalcopyrite (inse

aphically above tmagnetite-rich lay

t part of thee is indicated gan et al., 20opic age dete

consists of d millimetre

as intergxenoliths (?) nit (Figures 2

uartz veinlets lo

d contact betweerse rhyolite tuff is

et).

the turbiditic sectyers as well as ja

e map area. by extension

000) as well rmination of

f finely dto centimetre

growths witin a medium

25a, b). Millimocally cut the u

en fine s a layer of

tion is well-

asperoid

An early of geology as a new ~340 Ma.

disseminated e clots of th mafic grained K-

metre-thick, unit. Copper

Geological Fieldwork 2010, Paper 2011-1 57

pistacite, apleochroic member ofthe vein reimpart the halfnium asample MM

STRUCTZones

identified However, of more ththe regionwhere two

Folds, foPartiti

can be obsof these doaxial zonNortheast-presumablyare interpre

On tpenetrativesedimentarpervasivelylocally schfoliation ipreserved folding of by developstretching tectonites. limestone-clasts haveopen to tdevelopme

Timinschistosity east of theLogan et awhich affestrata affecbe Triassiccontrol fointerleavinthrust faultconstrainedpluton thatage of S2 strata do no

Some intrusion orestricted tElsewhere,

as opposed to th(magenta to y

f the epidote feveals only mipale pink colo

and zirconium (MI10-13-7, Tab

TURAL GE of foliated, foat various scthe strongest pan a square kil

ns south and wphases of fold

oliation andoning of strain

served on the riomains can be nes of maiverging thrusty syn-kinemateted to root benthe nunatak e fabrics arery rocks. In y recrystallizedhistose. Strongis shallower

bedding indithe stratigraphpment of stron

lineation, loL-tectonites

bearing congle aspect ratios tight recumbeent. g and conditiohave not bee

e map area Lal. (2000, Figurect pre-mid Ccted at Twin Gc (Kerr, 1935;or strata at ng of foliated anting cannot be d as pre-Eocet appears to ho

is not constrot appear to prschistose fabri

of the Twin Rito a zone withi, fabrics wi

he optically poyellow) piedmfamily. Trace einor Mn-enrichour), but relativ(0.19 and 6.3 pble 1).

EOLOGY olded and faultcales throughopenetrative fablometre are genwest of the T

ding are display

d schistosityn into elongateidges east of Texplained by tnly northwets and duplexic with northwneath the foliatbetween the

e developed these areas

d to such an eg to moderatelthan or sub-picating local hy. S1 is commng to intense, ocally with L

are spectacullomerates whof >>10:1. S1

ent F2 folds

ns leading to then firmly estabLogan and Koyre 2; 1994) recarboniferous rGlacier nunata Fillipone andthe nunatak

nd non-foliatedruled out. Min

ene, the age oornfels the S1-rained as the hreserve F2. ics were develoiver pluton, buin ~500 m of tithin regional

ositive and stroontite, the Mnelement analyshment (which vely high valuppm, see Hf an

ed rocks have out the map rics affecting anerally restrictTwin River plyed.

y e, foliated dom

Twin Glacier. Stheir position inst-trending f

x zones whichwest-trending fted rocks.

e Twin Glacin the volc

s, the rocks extent that theyly strong, steeparallel to poupright isocl

monly accompasteep to dow

L>S, forminglarly preserveere the limes1 is overprintewith minima

he formation oblished. Northyanagi (1994)cord similar farocks; whereasak are suspected Ross, 1989).

are lacking d strata by comnimum age of Dof the Twin R-L1 tectonites.hornfelsed Tri

oped in responut these fabricthe pluton contlly foliated

ongly n-rich sis of

may ues of nd Zr,

been area. areas ed to luton

mains Some n the folds. h are folds,

ciers, cano-

are y are p S1 oorly linals anied

wndip g L-ed in stone ed by l S2

of the h and ) and abrics s the ed to Age and

mplex D1 is River The

iassic

nse to s are tacts. rock

outcmapmarempof co

Fol

relatglidpartcherclaywellthruapprcom~3 asymwellthru

Figudispl

Figustrat

crops are cut bp scale, regionrgin of the intruplacement wasountry rocks.

lds and thruThrust faults

tively incompede horizons ticularly concerty strata of prystone of presul bedded calca

ust faulting; anreciable as a

mplex, thrust-rekm east of

mmetry withinl as the geom

usts mainly verg

ure 27a. A cliff falays an incised th

ure 27b. An interta.

by the pluton nal foliation teusion. Such rel in part accom

ust belts are best displetent strata whand décolle

entrated withiresumed Middumed Carboni

areous wacke hnd thrust offset

several hundelated deformaTwin Glacier

n both the footmetry of beddirged to the nort

ace between the hrust belt.

rpretation of the d

and related diends to wrap lations suggest

mmodated by d

ayed within which presumabments. This in two units:

dle Triassic ageiferous age. Nhas also been dts within this udred metre-lonation has been

(Figures 27atwall and hanging cut-offs, sth and east.

clouds east of Tw

deformation disp

ikes. At the around the

t that pluton ductile flow

well bedded, bly acted as

strain is sooty and

e and chert-Nevertheless, deformed by unit must be ng zone of n developed a, b). Fold gingwall, as suggest that

win Glacier

played by the

Geological Fieldwork 2010, Paper 2011-1 59

L

Th1 cofaG

A

AroGcaorTralzoarobin

winsothatHfasianacvedesu

thfaTrwmthstorotetpr

V

antha kimstve

ate faults Two major

he apparent ofkm, and as su

ontinuation of aults are named

Glacier fault and

Andrei GlaciNumerous

Andrei Glacier Foughly parallel

Glacier. This arbonate (Logrange-weatheririassic age to tltered, 1 to 2 mone where theyre probably rbserved cuttinnterpreted to be

Several setswithin the faulndicating compouth-side-downhe slickensides t any time,

However, the dault flutings wgnificant faultnd most of the cross the faultertical displaceepending uponub-Late Triassi

The opposihe inferred norault where polyriassic age tha

with Early Permmotion on the fhe fault displactrata). Southearthogonal to thther faults bout al., 2000), sredates the New

Verrett-IskutThe Verrett

ngle fault withhe southeast flaPaleozoic marilometre north

marble dips moteepens. Based ertical where i

r brittle-ductileffsets on these ch they impartstratigraphic ud after nearby d the Verrett-Is

ier fault fault strands Fault are expol to the northeafault juxtapoan et al., 20ing conglomethe southwest. m thick dikes hy display ghosrelicts of orthng Triassic stre of Late Triasss of minor strult zone includ

ponents of subhn-normal moti

are minor feaeven in respowndip slicken

with ~10 cm ot motion. The

Late Triassic t, perhaps as mement. Actual

n how much seic erosional evete sense of relrthwest extensymictic congloat lay northeasmian strata sofault may haveed previously dast extensionshe northeast-treunding the Newsuggesting thatwmont Lake G

t fault t-Iskut fault (V

h a gently arcuaank of Mount Vrble unit that ish of the fault,oderately west

upon its map intersected by

e faults have bfaults are infert a significant c

units and minergeographic feaskut Fault.

that together osed and orientastern margin ses Middle C00) to the noerate of preOrange, strong

have intruded ated, coarse phe

hoclase. Similrata to the sosic age. uctures have bding two setshorizontal-dextion. We acknatures that mayponse to glacnsides are sup

of relief and mentire Upper Csection appearmuch as 3 kmoffset could

ction was remoent. lative offset issions of the Aomerate of prest of the fault uthwest of thee been either sdeformed strat of the Andrending McLymwmont Lake gt the Andrei

Graben.

V-I fault) is a ate ~east-trend

Verrett, the V-Is ~200 to ~450, relict layerin. Nearer the fpattern, the mathe VI fault.

been mapped. rred to exceed control on the ralization. The atures: Andrei

comprise the ted northwest, of the AndreiCarboniferous ortheast, with esumed Late gly carbonate-along the fault enocrysts that lar dikes are outh and are

een identified s slickensidestral as well as

nowledge that y have formed cial rebound. erimposed on

may represent Carboniferous rs to be offset

m of apparent be much less oved during a

displayed byAndrei Glacier esumed Upper

is juxtaposed e fault. Thus, scissor-like or ta (e.g., folded rei Fault are

mont fault and graben (LoganGlacier Fault

discrete, high ding trace. On I fault cuts off

0 m thick. One ng within the fault, layering arble is nearly South of the

fault and band of mthe fault sinistral ofault, the to the true

Farthbiotite grain 104B/1appears lineamentbelow 12sandstone300-500 the fault (sources). constraineabout 145

WHERE

Westbottom, tQuaternarto trend does not Iskut rivedeflect nothe Rockmost likefrom theRecent laRiver alluof the floboth aeresponses(2009), W

Figure 28.southeast fRiver). Folhighly irregdashed linecontact surcorner of thband.

to the east inmarble outcrop

at a point woffset. If the m1800 m of appe horizontal coher east, the Vanite and Devo15 (Logan et alto follow a t trending ~25200 m. In thie” and mafic tm and envelop(see Figure 2 a

Amount oed because the50 m of appare

DOES THE W

t of its intersethe VI fault iry sediments. directly west offset a belt oers (see Figurorthwest-ward

k and Roll depely fault trace e river gravelava flows of Houvial fan deposows and clay-reromagnetic s on geophys

Walcott, (2009)

. A view to the weflank of Mount Vlowing the V-I fa

gular trace of thee) is interpreted rface with the stehe photo is the n

n 104B/15 (Lops can be extr

which would inmarble is verticparent sinistral omponent of ofVI fault juxtapono-Mississippl., 2000). To th

well-defined,50°, until it iis area, adjacetuff with a comped by argillitand Mihalynuk

of offset cane unit contacts ent sinistral mo

WESTERN V

ection with theis masked by However, the across the Iskf limestone bere 3). Instead,towards the “S

posit (Figure 3beyond its pos is obscuredoodoo Mountasits. Strong marich layers in and airborn

sical surveys ) and Dvorak (

est along the VeVerrett (photo tak

ult is a strong toe eastern marble as due to interseeep topography. northern continua

ogan et al., 20rapolated to intndicate ~1800 cal where cut offset is likely

ffset. poses Late Devpian tuffaceoushe west, the V-, glacially scis lost at elevent units of “mbined thicknte are also offk et al. 2011 fonnot be preare not expose

otion is indicate

V-I FAULT GO

e Iskut River the vegetatioVI fault is un

kut River becaetween the Cra it is interpreSulphide Ridg3). Farther weoint of re-emerd by Quaternain, or by the Hagnetic susceptthe gravels ob

ne electromareported by

1991). Howeve

errett-Iskut fault oken from above Vpographic lineamcontact (highligh

ection of a subveIn the upper righ

ation of the marb

000), a tersect m of by the

y close

vonian s rocks -I fault coured vations “quartz ness of fset by or data ecisely ed, but ed.

O (?)

valley on and nlikely ause it aig and eted to e” and

est, the rgence ary to

Hoodoo tibility bscure

agnetic Jones

er, a

on the Verrett ment. A hted by ertical ht

ble

60 British Columbia Geological Survey

break in the aeromagnetic responses in the survey reported by Jones (2009) may respond to a fault trace B on Figure 3 that is deflected slightly to the north. Minimal deflection of the fault is shown by the fault trace A option.

HOW MUCH OFFSET ON V-I FAULT (?)

The displacements of marble bands and quartzose sandstone indicate an average sinistral offset of ~1600 m in the eastern part of the Iskut River valley. Alternatively, decreasing sinistral offset along the fault to the west, as could be inferred from the data, may result in westward decrease of apparent motion by as much as 350 m per 5 km. Hence, the northern continuation of the “Sulphide ridge” stratigraphy could intersect the fault about 10 km west of the offset quartz-rich sandstone. At this point ~750 m of apparent sinistral offset might be inferred. Constraints on the vertical component of motion on the fault are lacking.

WHERE IS THE NORTHERN ROCK AND ROLL (?) Modelled offsets and locations of the western V-I

fault extension have significant implications for identification of a northern continuation of the strata that host the Rock and Roll deposit. Before speculating on the continuation of the Rock and Roll host strata north of the Iskut River Valley, it is necessary to consider several caveats:

1) The mineralization at the Rock and Roll deposit may not have a northern extension. Although the Rock and Roll deposit appears to be stratiform, a syngenetic origin has yet to be unequivocally established (e.g. Mihalynuk et al., 2010). Even if the mineralization is stratiform, it may not have had sufficient lateral continuity to outcrop to the north.

2) A northwestern extension of Rock and Roll, if it ever existed, may have been located above the present erosional surface unless the folds that deform the prospective stratigraphy remain approximately horizontal on average or plunge northwestward.

3) Units on “Sulphide Ridge” while complexly folded, display relatively simple bounding surfaces and intersection of these bounding surfaces with present day topography have a relatively consistent northwest trend. In this analysis it is assumed that this trend persists beyond the V-I fault extension.

In the simplest case scenario, barring any of the complication noted above, a potential extension to the Rock and Roll mineralization could be somewhere between the two localities marked by the thick blue and red lines on Figure 3. This supposition needs to be tested by constraining the location of carbonate belt north of the VI fault, particularly because the axis of mineralization

along “Sulphide ridge” is consistently between 350 and 450 m northeast of this contact.

SUMMARY Parts of the southern Hoodoo Mountain sheet were

first mapped at a reconnaissance scale by Forrest Kerr between 1926 and 1929. Yet, despite the high mineral potential of the adjacent areas, the northern 2/3 of the sheet was never systematically mapped prior to the work presented here. This report is a synopsis of 2.5 weeks of intensive field investigation that established a geological framework for the eastern Hoodoo Mountain sheet, and extended that framework southwards into the Iskut River valley, where a wealth of geological data exists in industry reports.

Our mapping revealed that the regional geological contacts formerly extrapolated through the Hoodoo Mountain area (Massey et al., 2005) inadequately represent its geological complexity and high mineral potential. As a result, significant mineral prospects, such as the Dirk, which has been recognized since at least 1972, lacked regional geological framework around which a district exploration program could be established.

Even though our mapping was limited by budgetary constraints, it provides enough detail for first order predictive metallogeny, and directions for future mineral exploration work. For example:

• Modelled offset on the V-I fault provides an exploration target for the northern extension of strata that host the Rock and Roll deposit. Future work should include detailed structural analyses aimed at constraining the displacement on units in the western Hoodoo Mountain area, including the vertical component of motion on the V-I fault.

• Recognition of a corridor of alkalic intrusive/volcanic “centres” permits us to pose the question of how extensive are mineralizing systems within the corridor? Alkalic rocks hosting mineralization at the Dirk are analogous to mineralizing intrusions at the Galore Creek deposit. Future work should address characteristics specific to mineralizing intrusions and their extents within the corridor.

• Our work outlines a bimodal submarine volcanic succession of Carboniferous age that contains indications of an active VMS mineralizing system of regional extent. Future exploration work will need to evaluate the significance and distribution of newly discovered primary Cu-Ag-Zn mineralization in both the Andrei rhyolite and the Verrett Creek rhyolite separated by ~20 km.

We will attempt to address some of these questions with targeted laboratory work, but others await the future work of explorationists and regional mappers in the eastern Hoodoo Mountain area. Some answers may lie in

Geological Fieldwork 2010, Paper 2011-1 61

the western Hoodoo Mountain area, parts of which STILL lack regional geological mapping.

ACKNOWLEDGMENTS This project would not have been possible without

the financial assistance of our project partners: Pacific Northwest Capital, the Geological Survey of Canada GEM initiative, and the University of Victoria (British Columbia Ministry of Energy, Mines and Resources Partnership Fund). This project is also funded in part by an NSERC Discovery grant to Stephen T. Johnston. Safe and courteous helicopter support was provided by Jim Beise of VIH Helicopters Ltd. Renaud Soucy la Roche ably assisted with field work. Comfortable accommodations were arranged by David Jensen and others of Skyline Gold Corp. We are especially grateful for the excellent camp cuisine and maintenance all attributable to Esther Nagli of Rugged Edge Holdings Ltd.

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