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Petrology of Serpentinized Metamorphic Olivine, Bird

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Petrology of Serpentinized Metamorphic Olivine, Bird Canadian Mineralogist Vol. 17, pp. 847-855 (1979) PETROLOGYOF SERPENTINIZEDMETAMORPHIC OLIVINE, BIRD FIVERSILL' MANITOBA C. J. A. COATS Falconbridge Nickel Mines Limited, Winnipeg, Manitoba R3l OMl R. BUCHAN Falconbridge Metallurgical Laboratories, Thornhill, Ontario L3T 4A8 AssrRecr tion, 3) formation de lames d'olivine m6tamorphi- que,'4) pseudomorphosepar lizardite.La formation The Archean Bird River greemtone belt in south- d" mumdtite, dolomite et calcite (en veinules tar- east Manitoba includes the lavered and differen- aivesl'au cours d'un m6tasomatismeintense Dr COr rocks in the basal partie cet assemblagede min6' tiated Bird River sill. Ultramafic 'West fait de la s6quence; portion of the sill at Maskwa contain talc, raux remplace la serpentinehdtive (2) et accom- magnesite, dolomite, chlorite, chrome spinel, mag- paene te d6veloppementde l'olivine en lames-(3)' netite and lizardite. Relict cumulus olivine tex- iis relations de'phasedu svstdmeCaO-MgO-SiOr tures preserv€d by magnesite are recognizable from HrO-CO, A 2000 bars, observ6essur le diagramme tle distribution of fine-grained magnetite inherited (calcul6) de la composition de la phase fluide en from the serpentinization of original olivine. Liz- ionction'de T, suggdrentque X(COr) excbde0'20 ardite is pseudomorphic after coarse-grained re' et placent- la temp6raturemaximale i - 515"C' geuerated olivine, with morphologes described as (Traduit Par la R6daction) rosettes, blades and "veins". The sill and surround- ing volcanic rocks at Maskwa are in the lower- INtnoouctroN amphibolite facies. From petrological evidence con- cerning the sill rocks, we infer the following se- The Bird River greenstonebelt in southeast- peri- quence of events: (1) intrusion of primary ern Manitoba comprises a suite of Archean (3) of dotite. Q) serpentinization. formation volcanic and sedimentary rocks bounded by bladed olivine and (4) lizardite pseu- metamorphic granitoid intrusions. It is 5-10 km wide and An integral part of this sequence is the domorphs. for 55 km, from Lac du development of magnesite. dolomite and late calcite itrikes east-west veins during pervasive COr metasomatism, replac- Bonnet in the west to the Manitoba-Ontario ing the early serpentine (2) and developing the border in the east. Principal geological studies bladed olivine (3). Reference to the calculated of the greenstonebelt are by Springer (1950), temp€rature-gas-composition diagram of CaO- Davies (1955), Butrenchuk (1970)' Karup- suggests that MeO-SiOz-HaG'{Or at 2000 bars Mdller & Brummer (1971), Juhas (1973) and is timiteO to greater than 0.20 and maxi XaCrOr) Trueman (L975). The volcanic pile is com- mum temperature to about 515'C. posed of a lower mafic sequence consisting-of basalts, porphyritic flow-basalts, hyalo- Sorvt"rlrns iillow bt"""ias, tuffs and amygdaloidal flow- "l^ti" sills of gabbro'. An Ir filon-couche diff6renci6 de Bird River se basalts, cut by stocks and flow- trouve dans la ceinture de roches vefies arch€en- upper felsic sequence is made up of nes du m6me nom, dans le sud-est du Manitoba' UunO"arhyolite, breccias, tuffs and quartz.por- A Maskwa Ouest. Ies roches ultramafiques i la base phyry, together with minor oxide-facies iron- dolomite, chlori- Au rn talc, magn6site, ioi*ution. Conglomerate, containing clastic te, spinelte"onti"nnent chromiflre, magn6tite et lizardite' L'oli- overlies pr6serv6es material from alL the above rock-types, vine'originelle est cumulative, i textures overlain by a se reconnaissent i the volcanic pile and is in turn pu. tu -ugoesite. Ces dernidres (Trueman el ia distribuiion de magndtite i grain fin qui date de sequenceof greywacke turbidites la serpentinisation. La lizardite, en rosettes,- lames al. I975). ou veinules, est pseudomorphe d'une olivrne re- The units of the greenstone belt, together constitude i gros grain. A Maskwa, le filon-couche with the bounding granitic bodies, the Maskwa ont recristal- et les roches volcaniques encaissantes i"f." q"-t" dioritt on the north side and the amphibolite inf6rieur' Nous con' lis6 dans le facids Lac-du-Bonnet quartz monzonite on the south cluons b la chronoloere suivante des 6v6nements: - *i4", t"t" emplacedin the time span 2'49 2'65 fj i"tt*ioo de p6ridotite primaire, 2) serpentinisa- 847 848 THE CANADIAN MINERALOGIST 'iWA..r.M .;.\!j1;{;;."..;:\ti:"sft #tS:>: f&++irsxd ot2 IE _ *tAsKwa oaaRlz t.-JJ ppp17g * lhd. groinedor 4 @NgroindOABEO Ftgr- 1. Geology of the Bird River sill in the Chrome-Page-Dumbarton area and location of the Maskwa West Ni-Cu deposit. Ga (Penner & Clark L97I). The metamorphic Pstnorocy oF THE Ur,tnewarrc Rocrs grade changes progressively from greenschist facies at Lac du Bonnet in the west to amphi- Ultramafic rocks of the Bird River sill have bolite facies at the interprovincial boundary. previously been studied from the Chrome and At the Maska West mine, located in an ap- Page properties (Trueman 1971) and from the proximately central position in the belt, the area south of the pu-nlu{sa mins (Juhas metaporphic grade is in the lower amFhibolite 1973). These will be reviewed briefly and com- facies (Juhas 1973, Trueman & Turnoct< tglS). pared to the ultramafic rocks forming the basal zone of the sill at Maskwa West (Fig. 1). Trrs BrRD Rrwn Srr,r, The Chrome and Page properties are located 8 km west and 6 km northwest of the Dum- The Bird River sill is a layered, differentiated barton mine, respectively. The grade of meta- ultramafic to gabbroic body emplaced within the morphism is in the greenschist facies. Serpen- yolcanic rocks of the lower mafic sequence. tinized peridotite near the baseof the sill at both Cross-faulted segmentsof the sill attain an our- the Chrome and Page properties consistsof oval- crop length of about 30 km in the Bird River shaped serpentine pseudomorphs after olivine belt and the average thickness is close to 1000 grains poikilitically enclosed in clinopyroxene, m. The sill is composed principally of a lower which constitutes approximately 30Vo of the peridotite unit and an upper hornblende-gabbro rock. The pyroxene exhibits extensivealteration unit, with less prominent layers composed of to tremolite, but this decreasesin intensity at pyroxenite, olivine gabbro, chromitite and anor- higher stratigraphic levels. Subhedral grains of gabbro. thositic The attitude of the compositional chromite are incorporated in both tremolite and layering is conformable with sotrth-facingpillow reliot pyroxene. Chromiferous peridotite and structures in adjacent volcanic rocks. chromitite form 18 persistent layers within the SERPENTINZJED METAMORPIIC OLIVINE, BIRD RIVER SILL 849 serpentinized peridotite near its upper coDtact with the overlying anorthositic gabbro. Regional metamorphism increases in grade eastward; rocks at the Dumbarton mine are in the lower amphibolite facies. Mineral assem- blagesin the ultramafic portion of the sill, south of.,the mine, are recorded by Juhas (1973) as follows: (1) antigorite,* chlorite -+- tremolite t carbonate; (2) antigorite * chlorite * talc -+ -+- tremolite carbonate; (3) olivine tremolite -+ * :t talc carbonate -r chlorite :L antigorite; (4) tremolite t carbonate r- chlorite; (5) diop- side * olivine * tremolite -r chlorite. The assemblagesoccupy the full width of the ultramafic unit, with assemblage5 in the centre grading laterally outward in both direc- tions, successivelythrough zones4, 3,2 and l. Their formation is attributed to contact-thermal metamorphism of the sill by the Maskwa quartz- diorite pluton. The thermal-metamorphic iffects are superimposed on regional metamorphism and are apparently restricted to a limited area. Textural criteria indicate that all the assem- blages were derived from an initial serpentinite. Petrology of the ultramalic rocks at Maskwa Vl/est Little evidenceof magmatic layering is present in the ultramafic unit of the sill at Maskrya West. Rocks exposed in the Maska open pit and intersected by exploration diamond-drill holes consist of dark green to black serpentinite in a dense, light grey matrix of talc, carbonate and chlorite (Fig. 2). Serpentine content ranges from zero to a maximum of approximately 6OVo,in irregularly shaped patches up to 3 cm Frc. 3. Photomicrograph of magnesite pseudo- acro6s. Massive talc-carbonate zones within the morphs after equant primary olivine. Very fine- sill seem to be associated with zones of intense erained magnetite occupiesfractures and outlines shearing, related to prominent northwest fault- the margins of the original olivine grains. Sample ing in the area and to less obvious strike faulting 65-302.Scale bar 0.1 mm. within the sill. The contacts of the ultramafic unit with underlying volcanic rocks and over- existenceof an olivine-rich ultramafic cumulate lying anorthositic gabbro are highly carbonated, zone in the lower part of the sill. Sulfides tectonized surfaces. present in a zone close to the sill base occupy The phases cornprising the matrix to the the interstices between the pseudomorphedoliv- serpentine patches in the ultramafic rocks in- ine grains, in a poorly defined net-texture. There clude magnesite,dolomite, calcite, talc, chlorite, is no remaining textural evidence indicating the magnetite, hematite and chrome spinel (14.7%o former presence of primary pyroxene in these CrrOr). Magnesite forms pseudomorphs after rocks. Estimates of initial pyroxene content will equant and close-packedcumulate olivine grains, be discussedin a later section on the chemistry with fine-grained magnetite outlining the mar- of the rocks. gins of, and the fractures
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