CHAPTER 7: MINERALISATION AND METAL ZONATION · 2014. 11. 18. · Chapter 7 -Mineralisation and Metal Zonation CHAPTER 7: MINERALISATION AND METAL ZONATION 7.1 Introduction The Fenton

Chapter 7 - Mineralisation and Metal Zonation

CHAPTER 7: MINERALISATION AND METAL ZONATION

7.1 Introduction

The Fenton Creek zone is consists of two Zn-Cu +/- Pb massive sulphide lenses. The

upper lens is the thickest and most massive of the ore body and ranges from 5 to 20 m

(apparent thickness). The lower lens is 3 to 10m of (apparent thickness) and dominated by

disseminated sulphide mineralisation. At least three different styles mineralisation have

been identified including (1) Disseminated sulphides which occur within and proximal to

the ore lenses (2) Semi-massive sulphides and (3) Massive sulphides which constitute the

ore lenses. Ore mineralogy of these different styles indicate that pyrrhotite» sphalerite>

chalcopyrite> galena. Tetrahedrite and boumonite are associated with galena.

Petrographical evidence is in agreement with the metal zonation which indicate that along

section 400N two general zones can be discriminated (1) iron + zinc + copper zone

which correlates well with the upper lens and part of the lower lens and (2) iron + lead +

gold + silver zone which is correlates with the lower lens.

This chapter endeavours to characterise the mineralisation styles, mineral/metal

associations and metal zonation along section 400N and then use this information to

compare metal zonation from section 300N and 500N.

7.2 Methods and Data Processing

Interpretation of the mineralisation and metal zonation is based on a total of 107

representative hand samples taken along section 400N and 470 assay results from samples

collected along sections 300N, 400N and 500N ofthe Fenton Creek zone.

Representative samples used in the description of the mineralisation have been taken

from the same 107 samples collected along section 400N and used to describe the local

geological units. Samples were cut on a diamond saw, photographed, and described.

From the 107 specimens, 45 representative samples were made into polished thin sections

and 10 ofthese polished thin sections were used for ore petrography.

Assay samples were collected from intervals of visible mineralisation by Hudson Bay

Exploration And Development Company employees and consisted 'h split or sawed NO


sized diamond drill core of intervals ranging from 30 to 200cm with an average of 100cm

(Gilmore et aI., 1999). The samples were then sent to Hudson Bay Mining and Smelting

Company Limited, where they were crushed with a steel jaw crusher, split and then

pulverised using a chrome-steel disc mill. Sample is then fluxed into a bead that is digested

using aqua-regia acid and then analysed using ICP and AA methods. Elements assayed

for include iron, copper, zinc, lead, arsenic, silver and gold. All elements with the exception

of arsenic have been grided and contoured along section using Surfer 7.0, a surface/

subsurface mapping program.

Metal zonation and characterisation was determined using the combined results of the

contoured assay data and the ore petrography from section 400N. Contoured assay data

from section 300N and SOON have been included in Appendix G as a means of comparison

between sections; however, no ore petrological studies were conducted on these sections

in this study.

7.3 Mineralisation

The ore in the Fenton Creek zone occurs as two main strataform massive sulphide lenses

ranging in thickness from 3 to 25m. The lenses have a parallel dip approximately 35 to 55°

to the west and can be traced over at least 3 sections a distance of 300m (Figs. 3.3, 3.4

and 3.5). The upper ore lens is located along the transition between biotite-plagioclase

and/or amphibole-plagioclase schists (probable basic igneous rocks) and metapelites,

whilst the lower lenses are hosted within the minor metapelite and quartz-muscovite

sillimanite schist of the footwall (probable acid igneous rocks). The lenses are separated

by a non-mineralised gap that ranges from 5 to 20m except in region intersected by diamond

drillhole Har021 on section 400N where the lenses almost join to form one lens.

Three styles of mineralisation have been recognized along section 400N of the Fenton

Creek zone: (1) disseminated sulphide pyrrhotite +/- sphalerite, chalcopyrite, galena and

graphite (2) Semi-massive sulphide psuedo breccia pyrrhotite +/- sphalerite, chalcopyrite

(3) massive sulphide pyrrhotite +/- sphalerite & chalcopyrite.

7.3.1 Disseminated sulphides

Three types of mineral associations exist within the disseminated style mineralisation (A)

Pyrrhotite +/- chalcopyrite-sphalerite, (B) Pyrrhotite +/- galena-chalcopyrite (C) Pyrrhotite

+/- graphite-chalcopyrite-sphalerite. In general type A and B are found proximal to the ore

bodies, while type C is very often within the ore position. Contacts are often sharp near the

116

Chapter 7 M Mineralisation and Metal Zonation

semi-massive and massive mineralisation and gradational away from the ore lenses. The

rocks hosting the disseminated mineralisation range in composition and degree ofalteration

from biotite-plagioclase schist to metapelite.

Type A - Pyrrhotite +/- chalcopyrite-sphalerite

Type A mineralisation is characterised by disseminated pyrrhotite with minor amounts of

chalcopyrite, and sphalerite. This style of mineralisation is typically found proximal to the

ore lenses within beddedlwell foliated biotite-amphibolite-plagioclase schists with variable

amounts of pelitic material. Pyrrhotite occurs as variable sized dissemination and blebs

that increase in size and density as pelitic content of the host rock increases (Fig. 7.1).

Chalcopyrite is a minor component of this mineralisation type and occurs as small

disseminations (Figs. 7.1 E-G) while sphalerite exhibits similar characteristics to the

pyrrhotite with disseminations becoming coarser and more frequent towards the ore lenses

(Fig 7.10).

Type B Pyrrhotite +/- galena-chalcopyrite

In hand specimen type B mineralisation consists of disseminated pyrrhotite and galena

(Figs 7.2Aand 7.2 0). This style of mineralisation is also found proximal to the ore lenses

predominantly within clinopyroxene-plagioclase schists of the footwall. In thin section the

mineralogy is pyrrhotite, galena, chalcopyrite +1- bournonite and tetrahedrite. Within the

two representative samples of the type B mineralisation pyrrhotite is often intergrown with

galena and chalcopyrite with sutured boundaries. Accessory minerals include bournonite

(PbCuSbS3), tetrahedrite (Cu, Fe)12Sb.S13 and an unidentified mineral possibly a nickel or

copper sulphides occur in close association to the galena and chalcopyrite are not seen in

other mineral types (Figs. 7.2 E-G).

Type C Pyrrhotite +/- graphite-chalcopyrite-sphalerite

Type C mineralisation is characterised by disseminated graphite, chalcopyrite and

sphalerite with disseminated to semi-massive pyrrhotite. This style of mineralisation is

typically found immediately proximal to the massive sulphide lenses within metapelite (Figs

7.3A-0).ln thin section the mineralogy pyrrhotite, fibrous graphite, chalcopyrite, sphalerite

with late pyrite replacing some of the pyrrhotite. The pyrrhotite often occurs as porphyroblasts

which a have inclusions ofgraphite and chalcopyrite (Fig 7.3 E) and as lone disseminations.

117

Figure 7.1 Type A - Disseminsated po +/- sph-cpymineralisation.A) Foliated biotite(biot)-K-feldspar(Kfs)-Sillimanite(Slm} schist(probable basic igneous rock) with disseminatedpyrrhotite(Po)-chaIcopyrite(Cpy)-sphalerite(Sph) mineralisationalong foliation. Sample H25866 drillhole Har043 (396.40m).B) Foliated clinopyroxene(Cpx)-plagioclase(Plag) schist(probable basic igneous rock) with disseminatedp yrrhot ite (Po)+ I-c ha leo py rite (C py)-sp ha Ie r ite(Sph)mineralisation. Sample 75602H drillhole Har021 (358.75m).C) Strongly foliated semi-metapelite with disseminated to stringerpyrrhotite(Po) +/- chalcopyrite(Cpy)-sphalerite(Sph)mineralisation. Sample 75506H drillhole Har010 (109.02m).D) Metapelite with semi-massive pyrrhotite(Po) +1chalcopyrite(Cpy)-spha lerite(Sph) mineralisation Sample75516H drillhole Har018 (188.73m).E-G) (E) Sample H25866 (10x), (F) Sample 75602H (5x) and(G) Sample 75506H (5x) showing compositions of granoblasticpyrrhotite(Po) +1- chalcopyrite(Cpy)-sphalerite(Sph)disseminations (Note the reduction in inclusions within thesulphides as the samples become increasingly pelitic) (reflectedlight).


118


..Gal

,,~

Gal.,

\~ '.,/ ,..

~

Figure 7.2 Type B - Disseminated pyrrhotite +/galena-chalcopyrite-sphalerite

A) Weakly foliated clinopyroxene(Cpx)-plagioclase(Plag) schistwith d issemin ated pyrrhotite(Po) +/- ga lena (Gal)chalcopyrite(Cpy)-sphalerite(Sph). Sample 75535H drill holeHar044 (481.51 m).B) Sample 75535H showing pyrrhotite(Po) and galena(Gal)aligned along a weak foliation (5x magnification, reflected light)C) Twinning in bournonite(Bo) crystal associated withpyrrhotite(Po) and galena(Gal). Sample 75535H (10xmagnification, reflected light with angled polarizer).D) Granoblastic clinopyroxene(Cpx)-plagioclase(Plag) schistwith blebs of pyrrhotite(Po) and disseminated chalcopyrite(Cpy)sphalerite(Sph). Sample 75526H drillhole Har021 (319.75m).

E) Galena(Gal), pyrrhotite(Po), bournonite(Bo) from sample L ~~_~~~~~~U75535H (20x reflected light).F) Galena(Gal), bournonite(Bo). chalcopyrite(Cpy) andsphalerite(Sph). Sample 75535H (20x reflected light).G) Tetrahedrite(Tet), pyrrhotite(Po), gale na(Ga I),chalcopyrite(Cpy) and an unidentified mineral possibly bornite.Sample 75535H (40x reflected light).

119


The characteristic graphite occurs as inclusions within cordierite poikioblasts (Fig. 7.3 G)

and as discrete grains along a weak foliation. Chalcopyrite and sphalerite occur as

disseminations and blebs throughout this type on mineralisation.

7.3.2 Semi-massive sulphides

The semi-massive sulphide mineralisation is dominated by pyrrhotite +/- sphalerite and

chalcopyrite. This style of mineralisation is found within the ore lenses and is often hosted

by c1inopyroxene-amphibole-plagioclase schists. As previously mentioned the contacts

between the semi-massive sulphides and the disseminated sulphides are often sharp (Fig.

7AA). Within this mineralisation style pyrrhotite is 25 to 30% ofthe rock and often fonms the

matrix with lesser amounts of sphalerite. Chalcopyrite occurs as disseminations within

defonmed and subrounded clasts of host rock fonm a moderately developed durchbewegung

fabric.

In thin section the mineralogy of the semi-massive sulphide is comprised of large 0.5 to

1cm recrystallized granoblastic mosaics of pyrrhotite and sphalerite both of which often

having inclusions chalcopyrite. Minor pyrite has also been noted in some samples and is

interpreted to have formed as a late alteration mineral associated with the breakdown of

pyrrhotite to pyrite. Trace arsenopyrite has also been observed as discrete subhedral grains

within the pyrrhotite.

7.3.3 Massive sulphides

The massive sulphide mineralisation as the name suggests is consists of> 40% massive

sulphide. Due to metallurgical testing few samples of the truly massive sulphide were

available for study along section 400N. The samples that were collected are composed of

massive pyrrhotite +/- sphalerite and chalcopyrite (Figs. 7.6 B-D). The host rocks forthe

most part have been replaced by sulphide the remnant remains consist of a biotite

clinopyroxene-carbonate rich metamorphic rock most likely of basic igneous origin. The

contacts of this style of mineralisation are often sharp and sometimes incorporate brecciated

host wall rock (Fig. 7.6A)

In thin section the massive sulphide comprises granoblastic mosaics of pyrrhotite, sphalerite

and chalcopyrite that often display annealed textures. The pyrrhotite is often very coarse

relative to the more highly variable grain size reflected in the sphalerite and chalcopyrite

(Wells, 2000) (Figs. 7.6A-D). Chalcopyrite most often occurs along the boundaries and as

small inclusions within sphalerite (Fig 7.6 E-F). The sphalerite is dark brown to reddish-

120


Figure 7.3 Type C - Graphitic pyrrhotite +/chalcopyrite-sphalerite mineralisation.A) Graphitic metapelite with disseminated pyrrhotite(Po) +1- .. ,.. r-L.Ao<-

chalcopyrite(Cpy) and sphalerite(Sph). Sample 755D7H drillhole '.J;.I~''''· .~--

HarDi0 (119.6m).B) Graphitic metapelite with pyrrhotite(Po) and graphite(Graph)orientated along the foliation Sample 756i5H drill hole HarD44(474.90m).C) Graphitic metapelite with semi-massive pyrrhotite(Po) +1sphalerite(Sph)-chalcopyrite(Cpy) mineralisation. Sample75507H HarDi0 (ii9.6m).0) Graphitic metapelite with semi-massive to massivepyrrhotite(Po) +1- chalcopyrite(Cpy) mineralisation. Sample ~~~~ ~!!'l

75520H drillhole HarOi8 (2i5.73m).E) Fractured porphyroblast of pyrrhotite(Po) with inclusions ofchalcopyrite(Cpy) & graphite(Graph). Sample 75507H drillholeHarDi0 (2.5x magnification, reflected light).F) Grain of pyrite(Py) showing distinctive birds eye textureindicative of replacement of pyrrhotite(Po). Sample 75507H (40xmagnification, reflected light).G) Inclusions of graphite(Graph) within a cordierite poikioblast(dashed circle) and as larger discrete grains. Sample 755D7H(5x magnification, reflected light).

121

Figure 7.4 Semi-massive pyrrhotite +/- sphaleritechalcopyrite mineralisation

A) Sharp contact of a semi-massive pyrrhotite(Po) +/sphalerite(Sph)-chalcopyrite(Cpy) with foliated mineralisedmetapelite from drillhole Har044 (474.5m).B) Sphalerite(Sph) rich semi-massive sulphide from sample75534H drillhole Har044 (465.22m).C) Semi-massive pyrrhotite(Po) -sphalerite(Sph)chalcopyrite(Cpy) specimen with weakly developeddUfchbewegung fabric. Note domains of finely disseminatedpyrrhotite(Po) & Chalcopyrite(Cpy) within coarserpyrrhotite(Po) -sphalerite(Sph). Sample 75611 H drillhole Har021(324.50m).0) Well developed durchbewegung fabric within semi-massivePo-sphalerite(Sph)-Chalcopyrite(Cpy) ore. Sample 75614drillhole Har044 (474.40m).E) Close-up of disseminated Chalcopyrite(Cpy) within thedeformed clasts. Sample 75614 drillhole Har044 (474.40m).


122


Figure 7.5 Zn-Cu massive sulphide ore

A) Sphalerite(Sph) rich matrix with disseminated pyrrhotite(Po) in the gangue. Sample 75534H (1.25x magnification, reflectedlight).B) Close-up of semi-massive sphalerite(Sph) containing inclusions of pyrrhotite(Po) and chalcopyrite(Cpy). Sample 75534H(5x magnification, reflected light).C) Copper rich clast with inclusions of chalcopyrite(Cpy) and pyrrhotite(Po). Sample 75532H (1.25x magnification, reflectedlight).0) Close-up of pyrrhotite(Po), chalcopyrite(Cpy). sphalerite(Sph) inclusions showing the interconnectivity between inclusions.Sample 75532H (2.5x magnification, reflected light).E) Iron rich cores in sphalerite(Sph) crystals. Sample 75534H (5x magnification, plane light).F) Chalcopyrite inclusions occurring along sphalerite(Sph) grain boundaries. Sample 75534H (10x magnification, reflectedlight).

123

(---

(

Figure 7.6 Massive pyrrhotite +/- sphaleritechalcopyrite mineralisation

A) Brecciated contact of pyrrhotite(Po)-sphalerite(Sph) massivesulphides. Sample from drillhole Har010 (154.25m).B) Massive granoblastic pyrrhotite(Po)+I-sphalerite(Sph) areSample 75527 Har021 (348.00m).C) Massive pyrrhotite(Po)+/-sphalerite(Sph) with quartz(Qtz)domains. Sample 75514 drillhole Har010 (157.08m).D) Massive pyrrhotite(Po) are. Sample 75513 drillhole Har010(154.08m).E) Typical massive ore of sphalerite(Sph) with numerousinclusions of chalcopyrite(Cpy) + pyrrhotite(Po) andchalcopyrite(Cpy). Sample 75527H drillhole Har021(348.72m)(5x magnification, reflected light).F) Massive pyrrhotite(Po) ore with minor sphalerite(Sph) andchalcopyrite(Cpy). Sample 75513 drillhole Har010 (154.08m)(1.25x magnification, reflected light).G) Twinning of granoblastic red/brown sphalerite(Sph) crystals.Sample 75514H drillhole Har010 (157.08m)(5x magnification,plane polarized light)


124


brown suggesting iron rich end member and often displays well developed twinning (Wells,

2000)(Fig. 7.6 G).

7.4 Metal Zonation

Pyrrhotite, sphalerite, chalcopyrite and galena are the major mineral species observed in

the ore lenses along section 400N and likely account for the bulk of the base metals (Fe,

Cu, Zn and Pb). Minor accessory sulphide minerals include tetrahedrite, boumonite, pyrite

and arsenopyrite that are only observed in minor amounts.

Grided and contoured assay data for base and precious metals along section 400N have

been generated to determine metal zonation (Figs. 7.7,7.8 and 7.9). The results of the

contouring indicate that Fe, Cu and Zn form roughly coincident anomalies which correlate

well with the upper ore lens along the entire section as well as the lower ore lens above the

large granitic intrusion Correlation between the various mineralisation styles, ore lenses

and metal zones are shown in Table 7.1.

Table 7.1 Table showing the corelations between ores lenes, style of mineralisation and the associatedmetals seen in the metal zonation.

Doninant Lens Mineral Types Mineralisation Style Metal AssociationUpper/lower lens A - Po +/- Cpv-Sph Disseminated lron-copper-zincLower lens B- Po +/- Gal-Cpv. Disseminated Iron-Iead-silver-aoldUpperllower lens C- Po +/- Graph-Cpv-Sph Disseminated Iron-copper-zincUpper lens Po +/- Sph-Cpv Semi-massive lron-zinc-copperUpper lens Po +/- Sph-Cpv Massive lron-zinc-copper

In detail, Fe distribution is fairly wide spread with a large halo of greater than 5%

encompassing most of the ore lenses. The highest values of +25% occur in the upper ore

lens in ddh Har021 and decrease down the dip ofthe lens. The Cu and Zn the follow same

trend as the Fe with highest grades of >0.6% Cu and>7% Zn focussed in ddh Har021 and

decrease in grade down dip (Figs 6.7 and 6.8).

In detail, the distribution ofAg is also widespread with values of 5g/t covering much of the

two lenses, however the highest grades of >35g/t occur immediately below the Fe, Cu and

Zn highs intersected by drillhole Har021 in the lower lens. Pb distribution is similarto that of

the Ag, however Pb appears more focussed and confined to the down dip portion of the

lower lens below the large granitic intrusion and is low to absent portions ofthe lenses that

are above the granitic intrusion. Au distribution is grossly coincident with that of Pb and to

a lesser extentAg, however, the highest values forAu appear intersected by ddh Har043

125


15

12.5

75

10

i

I30 I275

125 I

i22.5,,

I20 I

17.51

:500E .wOE

o C:~-SC-<:Ip-cDrb sl-'arf

o Qtz-b;ol-sil schist

D Ger-9mph metasediment

D aiot~f3 schrsf &; Amphibo lite_ Ofelense

o Ql..L-m use-sfI schl!.l

• Assay Sample Imerval

Generalized InterpretedGeological Legend

c::;] l.lu<Sl;eg

D Dok)mlteo Sandstone/regolith

o Gro11t c k1vus onJPG9m~tlt9

Har044/1

Legend

Muskeg

DolomiteSandstone/regolith

Granitic lnlrUSlOn/Pegmatlle

Gar· Sill schIst

Cpx.-scap,carb skarn

Qtz-blot-sllI schist

Gar-graph metasediment

B,oi-f••ch,st & Amphlbol~e

Ore lense

Qlz-musc-sill schist

5

Fe(%L

Figure 7.7 (A) Cross-section 400N shoWing the assay locations used in the gridding (8) Gridded andcontoured assay data for Fe overlayed ontop of interpreted geology from Section 400N. Data griddedusing a kriging method and a linear variogram model with anisotropy ratio of 3 and a preffered orientationof 50 degrees.

o126


2.5

5.5

3.5

4.5

1.5

0.3

0.6

0.2 !

6.5

0.4 I

0.5

0.85 1

Zn (%) IHar044//

Legend

Legend

MusKeg

Dolomite

Sandstone/regolith

GranitiC mlruslon/Pegmatlte

Gar-sill schIst

Cpx-scap-carb skarn

Otz-blot- Sill schist

Gar-graph metasediment

Blot-fs schist & Amphibolite

Ore lenseOlz~musc·slll SChiST

Muskeg

Dolomite

Sandstone/regol~h

Granitic intrusionlPegmauLe

Gar-sill schist

Cpx-scap·carb skarn

...) Qlz-brot·$111 schist

2i Gar-graph metasediment //U?I Blot-fs schIst & Amphibolite

I Ore tense

I QI,-muse-slli schist Har 044 0.15[1

! L-..---------::~__--_-----------------------------C-u-(:....°t<_0),--

Figure 7.8 Gridded and contoured assay data for (A) Cu and (B) Zn overlayed ontop of interpreted geologyfrom Section 400N. Data gridded using a kriging method and a linear variogram model with anisotropyratio of 3 and a preffered orientation of 50 degrees.

127


I!

0.65!

35

i0.551

45

I0.451

I1

55

:I , j

~251I ! iI i 15 i

0.351, I

I025'

I1°

15

1

0.05j

Pb (%) I

Har010

Har044

Har044

//

Legend

Legend

Muskeg

Dolomite

Sandstone/regolith

Gramtlc intrlls10nlPegmauie

Gar,sll~ schist

Cpx-scap-carb skarn

OIl-blot-sill schistGar-graph metasediment

8\01-1s schist & Amphtbollte

Ore lenseOtz-musc-si!1 schist

Muskeg

Dolomite

Sandstonefregollth

Granitic IntruSion/Pegmatite

Gar-sill schist

Cpx-scap-caro skam

Qtz-blot-sllI schistGar-graph metasediment

Biot-Is schist & Amphibolite

Ore lanseQlz-musc-slll schIst

15

IAg (flItJJ

._---------'''---''

Figure 7.9 Gridded and contoured assay data for (A) Pb and (B) Ag overlayed ontop of interpreted geologyfrom Section 400N. Data gridded using a kriging method and a linear variogram model with anisotropyratio of 3 and a preffered orientation of 50 degrees.

c128


002

iI

0.03

0.3

01

Au (gIl)

i0.01 1

._--------'-'-~(%) !

Har044

Har044

/j

/j

Legend

Legend

Muskeg

DolomiteSandstone/regol~h

GranftlC inlrusion/P€gmalJ~e

Gar-sill schrSl

Cpx-scap-carb skam

Qtz-btOt~Sll1schIst

Gar· graph metasediment

6iot-1s schist & Amphibolite

Ore lanseQtz-musc-siJ' schist

Muskeg

Dolomrte

Sandstone/regolith

Granitic Intruslon/Pegmatile

Gar·slll schist

Cpx·scap-carb skam

QtZ·bIO~~sill schIstGar-graph metasediment

Blot-Is schist & Amphibolile

Ore lense

Otz-musc-sJII schIst

Figure 7.1 OGridded and contoured assay data for (A) Au and (8) As overlayed ontop of interpretedgeology from Section 400N_ Data gridded using a kriging method and a linear variogram model withanisotropy ratio of 3 and a preffered orientation of 50 degrees.

129/

Generafized ImerpretedGeological Legend

~ Mus1::eg

CJ Ockxmteo SandstoneJre.C'o.Elh

L=:l Gra,it c inrrus onlP4;Qm;ltil.;,

G.lf-'3,j11 scht;;;t

o C~-SCoi>P-COl'"b sJ.'.on'

o Qt:;::-bio-f-sill Sct'HS

D Ger-grnph me18sediment

o Blol-f:,; ~dnst a.. Amph ibolite_ Oretensl!

o Qtz-mtJ$o,$illactli3-t

-30 E -' ODE

~.·.~"#"a~~ ·v- .~__ -~~.~

Generalized ImerpretedGeological Legend

c:J r.l uskeg

o Dolomite

o SoodS.1Oilelregclitfl

o Gro.,a c imrus OtllPIl7i£l.m:l1n~

Gar·sjll schi~l

o CpX.-~p-c.;:rt, ~v<)rr

o atz-Mat-sill $Chlst

Gar-gmptl. me1osedrne1ll

o BiGt-fs sch at & Amph ibo)jte_ Orelense

o Qt2-mus.c-anl schat

/1


110105100959085807570

,65;6055

,50'45'40

3530252015105o

Zn ratio100 x Zn/Zn+Pb

95

9085

80757065

i6055

504540

3530252015

10

5o

Cu rabo100 x Cu/Cu+Zn

Figure 7.11 Gridded and contoured assay data for (A) Zn ratio and (8) Cu ratio. As overlayed ontop ofinterpreted geology from Section 400N. Data gridded using a kriging method and a linear variogram modelwith anisotropy ratio of 3 and a preffered orientation of 50 degrees

130

Chapter 7 ~ Mineralisation and Metal Zonation

100m down dip from the highest Pb and Ag. In general terms Pb, Ag and Au coincide well

and correlate with the lower ore lens andlor are proximal to the Fe, Cu and Zn dominating

the upper lens (Table 7.1).

Examination of the kriged Zn ratio [100 x Zn/Zn+Pb] values and the Cu ratio [100 x CuI

Cu+Zn] values (Fig. 7.11) show a good correlation between low Zn ratio <25 and high Cu

ratio >80 focussed on drillhole Har043,which is located down dip from the best or grades

in Har021. This occurrence may represent an up flow zone along which hot hydrothermal

fluids could have travelled to be deposited further along in the region intersected by Har021 ,

however further investigations would be required to confirm such a claim. Previous

investigation by Huston and Large (1987) and Gemmell and Large (1992) on the Hellyer

VHMS deposit showed that in the Hellyer system Cu ratio values >5 highlighted the central

feeder zone to the system and that Zn ratio values greater than 67 corresponded to

temperatures less than 200°C and that Zn ratio values less than 61 corresponded to

temperatures of 240°C to 300°C. Using these results as a general guide it would appear

as though the region intersected by Har043 may have been the hot spot for the system

causing the mineralisation contained in the Fenton Creek zone.

Griding and contouring of assay data along sections 300N and 500N indicate similar results

to those seen along section 400N (Appendix G). In general Fe, Cu and Zn are all grossly

coincident with each other and correlate with the upper ore body. Ag, Au and Pb where

present are also generally coincident and correlate with the lower ore body. Lateral

correlation between sections indicate that Fe, Cu and Zn are highest grade in upper lens of

sections 400N and gradually decrease towards sections 300N and 500N. Comparisons

of Pb and Ag between sections indicate focussed distributions and higher values along

section 400N that decrease towards 300N and 500N. A property investigation with

mineralogical control is required to make further informed interpretations.

131

Chapter 7 R Mineralisation and Metal Zonation

7.5 Summary

Investigations into representative samples collected along section 400N indicate at least

three different types of mineralisation that include disseminated, semi-massive and massive

styles. The disseminated mineralisation can be further divided into three types of mineral

associations (A) Pyrrhotite +1- chalcopyrite-sphalerite, (B) Pyrrhotite +1- galena-chalcopyrite

tetrahedrite (C) Pyrrhotite +1- graphite-chalcopyrite-sphalerite. Spatially type B was

observed proximal to the semi-massive and massive mineralisation while type A and C

were observed both and proximal to the semi-massive and massive styles of mineralisation.

This observation in mineralisation styles is reflected in the metal zonation.

Grided and contoured assay data indicate that Fe, Cu and Zn form roughly coincident

anomalies which correlate well with the upper ore lens along the entirety of section 400N

as well as the lowerore lens above the large granitic intrusion. In general terms Pb, Ag and

Au coincide well and correlate with the lower ore lens and/or are proximal to the Fe, Cu and

Zn dominating the upper lens. Plotting of the Zn ratio and the Cu ratio indicate a potential

feeder vent intersect by Har043 and adjacent to the thickest portion of massive sulphide

intersected by Har021 on the Fenton Creek property.

132

Chapter 8 - Genetic Model and Discussion

CHAPTER 8: DISCUSSION AND GENETIC MODEL

8.1 Introduction

The aim of this chapter is to (1) briefly review the past and current genetic models proposed

for polymetallic Zn-Cu VHMS deposits in the Snow Lake Assemblage (2) summarize and

comment on the results of this study (3) propose a suitable genetic model for the Fenton

Creek Zn-Cu massive sulphide deposit (4) discuss exploration implications and suggest

future work to be completed on the Fenton Creek zone.

8.2 Previous Genetic Models

Two main genetic models have been proposed to explain the classical mound and sheet

like styled VHMS deposits of the Snow Lake Assemblage. The 'traditional' view of the

VHMS deposits of the Snow Lake Assemblage is that geochemically similar rhyolite

complexes and the well documented zones of hydrothermally altered rocks associated

with the VHMS deposits are a result of seawater-dominated geothermal activity by heat

from the Sneath Lake and Richard Lake synvolcanic tonalite intrusions (Walford and Franklin,

1982; Bailes, 1987). In the past this genetic model has been widely accepted and greatly

influenced the exploration for VHMS deposits in the region by focussing attention towards

the synvolcanic intrusions, rhyolite complexes and associated alteration.

Recently work by Bailes and Galley (1999) and Smye et al. (1999 has suggested that the

synvolcanic tonalite intrusions are only partly responsible for the generation of heat required

to set up a hydrothermal system and that mounting evidence also supports a genetic model

in which arc rifting may play an important role in the formation of VHMS deposits by

generating anomalously high heat flow, fracturing and fluid circulation. This relatively new

genetic model as applied to the Snow Lake district may have important implications for

future exploration of VHMS deposits in the region since it targets previously unfavourable

environments which might have been explored using the 'traditional' genetic model.

Chapter 8 ~ Genetic Model and Discussion

8.3 Discussion

The following section summarizes and discusses the significant findings of this study with

which helped to determine a suitable genetic model for the Zn-Cu massive sulphide lenses

found in the Fenton Creek zone.

1. Reinterpretation of geologic logs by the author with the aid of Iithogeochemical data

has divided the Fenton Creek stratigraphy into five generalized groups including

quartz-muscovite-sillimanite schist located in the footwall, biotite-clinopyroxene

plagioclase schist and amphibole-plagioclase schist located in the immediate

hanging wall, quartz-biotite-sillimanite schist in the upper hanging wall, metapelitic

sediments occurring in the ore horizon and in the upper hanging wall and flat lying

post kinematic granitic intrusions cross-cutting all lithologies. The results of this re

interpretation show that the Fenton Creek ore lenses are hosted between a felsic

footwall and mafic hanging wall, which may reflect a bimodal volcanic sequence.

2. Geochemical discrimination of the biotite-clinopyroxene-plagioclase schist and

amphibole-plagioclase schist found in the immediate hanging wall to the ore lenses

indicate that they are geochemically similar to arc-rift basalts found in the Snow

Creek Formation. This may support the notion that the Fenton Creek massive

sulphide was deposited in a rift environment.

3. Mass balance calculations of the footwall quartz-muscovite-sillimanite schist indicate

mass losses of 8g/1 DOg Si and 2g/1 DOg Na and minor mass gains of K. The results

of the mass balance calculations in conjunction with the mineral assemblage of K

feldspar-sillimanite-cordierite-anthophyllite +/- base metals suggest that the footwall

quartz-muscovite-sillimanite schist may have been subjected to weak sericite +/

chlorite alteration.

4. Interpreted hydrothermal alteration appears stratiform and confined to the footwall

and does not extent into the hanging wall. This suggests that the alteration may have

been synvolcanic with the deposition of the footwall rocks and that alteration ceased

prior to the deposition of the hanging wall.

5. Use of geologic logs and lithogeochemistry indicate large thicknesses of rhyodacitic

volcaniclastic rocks (+200m thickness) in the upper hangingwall to the ore lenses.

This suggests deposition from some type of a mass flow (Le. turbidite) along the

flanks of a subaqueous volcano or in arc rift environment.

134

Chapler 8 - Genetic Model and Discussion

6. Carbon isotopes indicate that the graphite in the metapelitic rocks which are often

associated with the ore lenses has a biogenic signature. This evidence suggests

the presence of organic life (Le. black smoker) near the deposition site and/or a

quiescent environment where carbonaceous debris could accumulate.

7. This study confirms previous work by Wells (2000) that mineral assemblages

observed in the pelitic and metabasic rocks indicate that the Fenton Creek zone

has been subjected to amphibolite facies metamorphism with moderate to high

pressures (in excess of 3000 bars) and with temperatures that range from 550° to

<725°C.

8. Study of the metal associations and zoning indicate that Fe, Cu and Zn form roughly

coincident anomalies which correlate well with the upper ore lens along the entirety

of section 400N as well as the lower ore lens above the large granitic intrusion. In

general terms Pb, Ag and Au anomalies coincide and correlate with the lower ore

lens and/or are proximal to the Fe, Cu and Zn dominating the upper lens. Cu and Zn

ratios indicate the higher temperatures in the Fenton Creek system along section

400N are intersected by drillhole Har043 down dip from the thickest part of the ore

lens intersected by Har021. This might also indicate the sight of a potential

hydrothermal vent.

9. Monazite dating of the non-foliated, undeformed flat lying post kinematic granitic

intrusions confirm an intrusive age near 1750Ma.

8.4 Fenton Creek Models

Geologic diamond drillhole logging, lithogeochemistry and carbon isotopes of the Fenton

Creek deposit support the interpretation of two sheet-like stratabound Zn-Cu +/- Pb, Ag,

Au rich massive sulphide lenses hosted within a mixed graphitic metapelite horizon between

a quartz-muscovite-sillimanite schist footwall and a biotite-c1inopyroxene-plagioclase/

amphibole-plagioclase schist hanging wall. Hydrothermal alteration thought to be associated

with massive sulphide deposition is represented by K-feldspar, sillimanite, muscovite,

cordierite and anthophyllite (interpreted sericite altered zone) is confined to the footwall

and does not appear to occur in the hangingwall.

Three potential styles of VHMS deposit types best fit the characteristics listed above for

the Fenton Creek Zn-Cu deposit (1) bottom fill brine pool VHMS (McDougall, 1984) (2)

Distal brine pool (Sato, 1972) (3) synvolcanic seafloor/subseafloor replacement style VHMS

135

,/,,-. Distal brine poot model/,/~, ~..:..~. (Sato 1972 Type I).ffj~~~~~~~~~~~~:~c

20rnL100m

. • no major FW alteration


Distal brine pool model after Sato (1972) showing theaccumulation of massive sUlphide through the mixingof hydrothermal fluid with sea water. Note the absence of the footwall alteration directiy beneath thedense brine pool.

Bottom fill brine pool model

____ ~_ ~MCDOUgal~g84a) Bottom fill brine pool model after McDougall (1984a)- ,-- - -- ---- showing the accumulation of massive sulphide

'w,;,' directly ontop of the footwall alteration.

week fW alteration

Rift related/replacement model modified after Large(1992) showing the accumulation of massive sul

~_Pil..;;;;;;;;;;;;;;::::;~~~1 phide by seafloor exhalation and/or sub-seafloor, ",,, replacement. Stratabound footwall alteration forms

• massive Pb-Zn ore

m massIve pyrlt&-Cu ore under the entire sulphide lense.~ stringer ore

Figure 8.1 - Generalized diagram showing three models used to explain the genesis of sheet or blanketstyle VHMS deposits which have stratabound footwall alteration (modified after Large, 1992).

(Blaise et aI., 1988; Franklin, 1990; Large, 1992) (Fig. 8.1). Though none of the deposit

styles can be ruled out completely, evidence from this study including geochemically identified

arc-rift related basaltic volcaniclastics/flows, thick sequence of rhyodacite volcaniclastics

and lack of a hydrothermal alteration in the hanging wall favours a synvolcanic seafloor

exhalative and/or sub-seafloor replacement style VHMS deposit in an arc rift environment.

An idealized schematic diagram modified after the replacement model proposed by Large

(1992) illustrates the several potential stages of development of the Fenton Creek massive

sulphide deposit (Fig. 8.2).

Regardless, of the accuracy of the genetic model; the Fenton Creek zone represents a

newly discovered massive sulphide deposit which shows many VHMS characteristics, some

of which are similar to the deposits found in the Snow Lake Assemblage and otherfeatures

which suggest it formed in a very different environment distinguish it from other deposits in

the region. Based on Iithogeochemical discriminations and a very generalized stratigraphy

of the Snow Lake Assemblage, the Fenton Creek zone may represent a new mineralised

horizon in the arc-rift volcaniclastics (Fig. 8.3).

136


A

VOlcanic MC Sequence?

Initial rifting and deposition of footwall rhyoliticvolcaniclastic detritus followed by continued riftingand infilling.

s,

Froctunng , . Shatabound fool\..oll alteration

Volconic MC Sequence?

Period of quiescence, deposition of carbonaceousmudstone followed by the deposition of massivesulphide and associated weak sericite +/- chloritealteration by sub-seafloor replacement and/orexhalation.

Deposition of basaltic flows and/or basalticvolcaniclastics from the Snow Creek rift basalt&preservation of the massive sulphide lenses.

\\\Volcanic Arc Sequence?

D. Deposition of rhyodacitic volcaniclastics interbeddedwith Snow Creek Rift basalt, ending with anotherperiod of quiescence and the deposition of asedimentary sequence of carbonaceous mudstone

~~~~~~~~~~~~:::===~~J /sandstone

Volcanic Nc Sequence?

Continued deposition of rhyodacitic volcaniclasticswith less frequent interbedded basalt Thissequence is followed by another basaltic unit ofmore substantial thickness.

JVolcanic MC Sequence?

r"'--"'---A../'--..A---"--"'---,,---,"'-J'.---'"-~./'-..~~-..A--A-

Cu-richHarmin Zn rich Fenton .I Creek Zone I Creek ZoneE,

Carbonaceous Metasediment

Unknown (Volcanic Arc Sequence?)

o Rhyolitic volcaniclastic (Footwall)

i r Rhyodacitic volcaniclastic

i ! Basaltic volcaniclastic (Hangingwall)

!"'~ ..'! Weak serictite +/- chlorite alteration

• Massive Sulphide

Figure 8.2 - Simplified schematic diagram illustrating the proposed stages of development of the FentonCreek zone based on a arc-rift genetic model and volcaniclastic input from various sources.

137


Mature Arc DepositsC Chisel Zn-CuGH Ghost Lake Zn-CuLO Lost Zn-CuPH Photo Cu-Zn-Au

~ SUlphidic layer

Copper dominant deposit

Zinc dominant deposit

Aphyric basaltt

Porphyritic basalt

Synvolcanic tonalite

Felsic breccia

Fe-basalt

Rhyolite

Dacite

Mafic volcaniclasticsPrimative Arc DepositsA Anderson Cu-ZnJ Joannie Cu-ZnLD Linda Zn-CuP Pot Zn-CuR Raindrop Cu-ZnRD Rod Cu-ZnRM Ram Cu-ZnS Stall Cu-Zn

Figure 8.3 - Schematic startigraphic section showing the potential location of the Fenton Creek zonerelative to the other major base-metal rich sulphide deposits of the Snow Lake Assemblage (modified afterBailes, 1999)

DoDD

•D•

8.5 Future Exploration

The discovery of the Fenton Creek poly-metallicZn-Cu massive sulphide deposit represents

a significant new mineral discovery in a previously unexplored stratigraphy. The implications

for further exploration and discovery are summarized below:

1 Assuming the Fenton Creek zone is hosted between rift fill mafic volcaniclastics of

the Snow Creek Formation and undetermined rhyolitic volcaniclastics, future explo

ration might be well advised to explore at this stratigraphic level along strike from

the Fenton Creek zone looking for evidence of similar deposits.

2 Continued use of electromagnetic geophysical techniques to target short strike length

(1 00-500m) conductors even in regions with significant graphite as the graphite is

o138

Chapter 8 . Genetic Model and Discussion

consistently found mixed in with massive sulphide ore.

3 As recommended by Wells (2000) and confirmed in this study K-feldspar staining

is a very effective means of visually identifying weak footwall alteration.

8.6 Future Work

It is recommended that the following work be considered if future development is carried

out on the Fenton Creek zone:

1. Uranium-lead dating of zircons from the quartz-biotite-sillimanite schist (hanging

wall rhyodacite) and/or the quartz-muscovite-sillimanite schist (footwall rhyolite). This

dating should allow for more confident determination of the stratigraphic position of

the Fenton Creek deposit and how it relates to other deposits in the Snow Lake

district.

2. Review and select a least altered precursor sample of the footwall and hanging wall

rhyolite/rhyodacite well away from the mineralised zones so to better characterise

the mass changes related to hydrothermal alteration. This may help to determine

further geochemical ore vectors and targeting parameters.

139

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CHAPTER 7: MINERALISATION AND METAL ZONATION · 2014. 11. 18. · Chapter 7 -Mineralisation and Metal Zonation CHAPTER 7: MINERALISATION AND METAL ZONATION 7.1 Introduction The Fenton