Geology and Mineralization of the Hoodoo Mountain Area ... · PDF fileF f p igure 3. Geology...
Transcript of Geology and Mineralization of the Hoodoo Mountain Area ... · PDF fileF f p igure 3. Geology...
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
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
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dard
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Stan
dard
Mea
sure
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dard
as
certi
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Blan
k
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renc
e M
ater
ials
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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