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Alteration at the Sam Goosly copper-silver deposit, British Columbia Wojdak, Paul John 1974

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• ALTERATION AT THS SAM GOOSLY. • COPPER-SILVER DEPOSIT, • ' BRITISH COLUMBIA ' by PAUL JOHN WOJDAK •B.Sc., McMaster U n i v e r s i t y , 1971 A THESIS SUBMITTED IN PARTIAL.FULFILLMENT THE REQUIREMENTS FOR THE DEGREE OF MASTER OF SCIENCE i n the Department of G e o l o g i c a l Sciences We accept t h i s t h e s i s as conforming to the r e a u i r e d standard. .. :THS UNIVERSITY OF BRITISH COLUMBIA May, 197^ In p r e s e n t i n g t h i s t h e s i s i n p a r t i a l f u l f i l m e n t o f the r e q u i r e m e n t s f o r an advanced degree a t the U n i v e r s i t y o f B r i t i s h C o lumbia, I agree t h a t the L i b r a r y s h a l l make i t f r e e l y a v a i l a b l e f o r r e f e r e n c e and s t u d y . I f u r t h e r agree t h a t p e r m i s s i o n f o r e x t e n s i v e c o p y i n g o f t h i s t h e s i s f o r s c h o l a r l y purposes may be g r a n t e d by the Head o f my Department o r by h i s r e p r e s e n t a t i v e s . I t i s u n d e r s t o o d t h a t c o p y i n g o r p u b l i c a t i o n o f t h i s t h e s i s f o r f i n a n c i a l g a i n s h a l l not be a l l o w e d w i t h o u t my w r i t t e n p e r m i s s i o n . Paul J. ftbjdak Department o f Geological Sciences The U n i v e r s i t y o f B r i t i s h Columbia Vancouver 8, Canada Date May 29. 197** i ABSTRACT Copper-silver mineralization at Sam Goosly occurs as a conformable lens within pyroclastic dacites of probable late early Cretaceous age. Most mineralization is contemporaneous with development of aluminous alteration minerals. Distribution zones of scorzalite, andalusite, and an innermost corundum zone, are concentric and broadly outline the mineralized zone. Southwards, along strike, the andalusite zone becomes an andalusite-pyrophyllite zone in which mineralization post-dates aluminous alteration. Regional metamorphlsm has overprinted a propylitlc, or greenschist, assemblage on aluminous alteration. Country rocks and mineralization are intruded by two stocks* a 59+3 m.y. quartz monzonite to the west of the ore zone, and a 51+3 m.y. gabbro-monzonite stock to the east. Contact metamorphlsm associated with the gabbro-monzonite has produced a narrow, discon-tinuous zone of biotite hornfels and recrystallized metallic minerals in the ore zone. Alteration mineral assemblages and sulphide exsolution textures imply temperatures between 350°C and 625°G in the main ore zone. The assemblage andalusite-pyrophyllite-quartz indicates alteration tempera-tures of about 350°C in the andalusite-pyrophyllite zone. Chemical analysis of the altered volcanic host rocks suggests significant loss of soda and lime, and residual concentration of silica and alumina, + 1 1 These chemical changes probably result from exchange of Na and Ca for H + from a hydrothermal fluid, resulting in formation of aluminous minerals and quartz. The value of log mK+/mH+ of the fluid phase is deduced to be between 1 and 2. By analogy with other occurrences, this process probably takes place in a high-temperature solfataric, or geothermal environment. TABLE OF CONTENTS Page INTRODUCTION Purpose 1 Location and A c c e s s i b i l i t y 1 Physiqgraphy, - - Pleistocene Geology 3 History ^ Methods of Study 5 GEOLOGICAL SETTING Introduction 8 Mesozoic Strata 8 T e r t i a r y Volcanic Sequence H Intrusive Rocks 12 M i n e r a l i z a t i o n 13 GEOLOGY OF SAM GOOSLY Introduction 15 Mesozoic Rocks 22 C l a s t i c D i v i s i o n .22 P y r o c l a s t i c D i v i s i o n . . 2 3 Basal P y r o c l a s t i c s 23 Brecciated Dacite 25 Volcanic Breccia 25 E p i c l a s t i c s 2? Dust Tuff 28 Welded Ash Tuff 28 Sedimentary-Volcanic D i v i s i o n . 30 Comparison of Geologic Sections 30 Composition of Volcanic Rocks 31 T e r t i a r y Strata 3^  Intrusive Rocks 35 Quartz Monzonite 35 Gabbro-Monzonite Complex 3 5 Dykes and S i l l s 38 Structure ^0 i i i Page ORE MINERALOGY Introduction 42 M e t a l l i c Mineralogy 42 D i s t r i b u t i o n and Character of Mineralization 43 Mineral Zoning 46 Mineral Textures., 48 ALTERATION AND METAMORPHISM Introduction 52 Aluminous Al t e r a t i o n . .52 Scorzalite Zone 54 Andalusite and Andalusite-Pyrophyllite Zones 55 Corundum Zone 61 Other Minerals 65 A l t e r a t i o n Associated with Mineralization i n Unit 66 Regional Metamorphism 6? Contact Metamorphism. 70 DISCUSSION Sequence of Alte r a t i o n Events...., 73 Graphical Representation of Al t e r a t i o n Assemblages ..73 Interpretation of Aluminous Al t e r a t i o n . .80 P - T Estimates from the System Al^-SiOg-RgO 80 Hydrolysis E q u i l i b r i a 82 Correlation of Sulphide Temperatures and S i l i c a t e A l t e r a t i o n Assemblages .89 Effect of H on Aluminosilicate S t a b i l i t y . 90 Formation of Corundum 91 Formation of Other Aluminous Minerals 93 CONCLUSIONS Other Occurrences of Aluminous Al t e r a t i o n 95 A l t e r a t i o n Model 97 Geologic History 105 REFERENCES 107 APPENDIX 112 i v » LIST OF TABLES Page Table 1 Chemical Composition of Lower Cretaceous Rocks at Sam Goosly. 32 2 Comparison of Sam Goosly and Nockolds' Average Volcanic Rocks. 33 3 Chemical Analyses of Intrusions and Tertiary Lavas...36 4- Mineralogy of Aluminous A l t e r a t i o n 53 5 Cation Charge Balance 99 6 Potassium Molality i n Various Geothermal Waters 104 7 Chemical Composition of Brine i n Hole MR-1, Matsukawa 104 V LIST OF FIGURES Page F i g u r e 1 L o c a t i o n Map 2 2 R e g i o n a l G e o l o g y 9 ~<V — 3 Geology o f Sam G o o s l y . i n p o c k e t s Co-bmef 4 S e c t i o n 1 3 . 4 0 0 N . . . . 1? 5 S e c t i o n 1 2 , 4 0 0 N 18 6 S e c t i o n 1 1 . 5 0 0 N 19 7 S e c t i o n 9 . 1 0 0 N . 20 8 S e c t i o n 1 1 . 8 0 0 N ( A p p r o x i m a t e l y ) 21 9 Sequence o f A l t e r a t i o n E v e n t s 74 10 G r a p h i c a l R e p r e s e n t a t i o n o f A l u m i n o u s A l t e r a t i o n . . . 7 6 11 G r a p h i c a l R e p r e s e n t a t i o n o f R e g i o n a l Metamorphlsm..7 8 12 G r a p h i c a l R e p r e s e n t a t i o n o f H o r n f e l s Zone.... 79 13 System A l ^ - S l O g - K g O 81 14 Some E q u i l i b r i a i n t h e System KgO-A^ C y-SiOg-HgO.. . 8 4 15 Some E q u i l i b r i a i n t h e System KgO-AlgCy-SiOg-HgO.. . 8 5 16 E q u i l i b r i a i n t h e System J ^ O - A l ^ - S i O g - H g O 87 17 a + - T R e l a t i o n s h i p s f o r M u s c o v i t e , K - f e l d s p a r a n d A l g S i O ^ 88 18 T y p i c a l J a panese A l u m i n o u s D e p o s i t . 96 LIST OF PHOTOGRAPHS P h o t o g r a p h 1 B a s a l p y r o c l a s t i c u n i t (B^) . , 2 4 2 B r e c c i a t e d d a c i t e u n i t ( B ^ ) . . . . 24 3 V o l c a n i c b r e c c i a u n i t (B^) 26 4 E p i c l a s t i c u n i t (B^) 26 5 Dust t u f f u n i t (B^) 29 6 Welded a s h t u f f u n i t (Bg) 29 7 V e i n o r e i n d u s t t u f f u n i t 45 8 B r e c c i a zone i n d u s t t u f f u n i t 45 9 P y r i t e a g g r e g a t e w i t h r andomly d i s t r i b u t e d s i l i c a t e i n c l u s i o n s 4 7 10 E u h e d r a l p y r i t e w i t h zones o f inc l u s i o n s : ; . * : , . . i i . i - . 4 7 LIST OF PHOTOGRAPHS (cont.) Page Photograph 11 Pyrrhotite i n t e r s t i t i a l to granoblastic quartz", i . . . . 49 12 Hematite r e p l a c i n g magnetite along f r a c t u r e s 49 13 Chalcopyrite exsolved from a chalcopyrite host.....51 14 'Stars' of sp h a l e r i t e exsolved from chalcopyrite...51 15 S c o r z a l i t e associated with p y r i t e and muscovite....56 16 Band of andalusite, p y r i t e and quartz i n a quartz-muscovite rock 56 1? Prismatic andalusite with quartz 58 18 Andalusite intimately intergrown with p y r i t e and chalcopyrite 58 19 Andalusite r o s e t t e s , centred by r u t i l e 60 20 C h i a s t o l i t e i n dust t u f f unit 60 21 P a r a l l e l v e i n l e t s of andalusite 62 22 Andalusite with i n c l u s i o n s of corundum 62 23 Zoned blue corundum and green s p i n e l i n matrix of muscovite 64 24 Corundum and quartz 64 25 P a r a l l e l , wispy c h l o r i t e - a n d a l u s i t e v e i n l e t s cut by c h l o r i t e - p y r i t e vein 68 26 CChlorite pseudomorphs of andalusite.. ....68 ACKNOWLEDGEMENTS The author wishes to express his gratitude to Dr. P.B. Read, of the Un i v e r s i t y of B r i t i s h Columbia, who w i l l i n g l y undertook supervision of t h i s study a f t e r the death of Dr. J.A. Gower. The enthusiasm of the l a t e Dr. Gower and Mr. Andre Panteleyev, of the B.C. Department of Mines, f i r s t stimulated the author's i n t e r e s t i n the project. Sincere thanks are expressed to Dr. B.N. Church, of the B.C. Department of Mines, f o r h i s assistance i n obtaining t h i n sections, f o r h i s h o s p i t a l i t y during the author's stay i n Houston i n 1972, and f o r f i n a n c i a l support permitting a v i s i t to the property i n 1973. The author a l s o benefited from discussions with Mr. C.S. Ney and Mr. J.M. Anderson, formerly of Kennco Explorations (Western) Ltd., and with Mr. E.S. Holt, of Equity Mining C a p i t a l Ltd. 1. INTRODUCTION PURPOSE Sam Goosly is a recent copper-silver discovery in central B r i t i s h Columbia, The local geology and history of discovery have been described by Ney, Anderson and Panteleyev (1972), and the local and regional geology, by Church (l969 f 1970, 1973). Although a mineralogical study of the deposit was made by Nielsen (I969) at an early stage in the d r i l l i n g history, a comprehensive study had not been undertaken. Neilsen's work gave a good insight into the complex nature of the al terat ion, but posed rather than solved problems. This study was undertaken because of the significance of the unusual alteration assem-blages and because of an uncertainty as to the genesis of the deposit. Recent diamond d r i l l i n g allows a detailed investigation of the host rocks and alteration mineralogy. This investigation contributes to a better understanding of the deposit. LOCATION AND ACCESSIBILITY The Sam Goosly prospect i s located 35 km. (22 miles) south of Houston, B r i t i s h Columbia at latitude 54°11' north and longitude 126°l6' west (Figure l ) . It is 6.5 km. (4 miles) ENE of Goosly Lake from which the property takes i t s name. The property is 56 km. (35 miles) along the Buck Creek Road from Highway 16 near Houston. Buck Creek Road is a dry-weather gravel and logging road. 1 On most recent maps the name "Sam-Goosly-Lake" has been shortened to "Goosly Lake". 3. PHYSIOGRAPHY AND PLEISTOCENE GEOLOGY Sam Goosly is located in gently rolling country in the west-central region of the Nechako Plateau (Holland, 1964). Regionally, the relief ranges from 600 m. (2,000 feet) to 1,500 m. (5,000 feet) and the deposit is at an elevation of 1,300 m. (4,300 feet). A resistant plutonic stock immediately east of the mineralized zone forms a prominent h i l l reaching an elevation of 1,600 m. (5,300 feet). Tributary streams radiate from this high area, draining on the southwest toward Goosly Lake and into Buck Creek, and on the northeast into Foxy .Creek, Except for areas of recent lumber harvesting and an old forest fire 'burn', the region is well forested. Glacial drift is widespread and a high percentage of the bedrock is obscured. Outcrop areas are restricted to ridges and some creek beds. The mineralized zone outcropped in only one small exposure in a creek bed. Except for the h i l l of plutonic rocks to the east, rocks are poorly exposed on the property. Contradictory evidence for the direction of Pleistocene ice movement has been reported by Ney et al (1972) and by Church (I969). Regionally, Holland (1964) indicated that ice movement was eastwards and northeastwards from a centre in the vicinity of Ootsa Lake. This direction is supported locally by Church who found glacial striae indicating ice movement towards 075 degrees. However, Church also found that granite erratic boulders were transported several hundred feet southwest of a source area. This direction is in closer agreement with Ney et al who determined the direction of ice movement to be 245° , based upon glacial smoothing of some resistant dykes. Their evidence is supported by a southwesterly direction of transport of 4. glacial t i l l necessary to explain the position of the silver anomaly in the soil geochemistry. Their silver anomaly map shows a pronounced southwesterly displacement of anomalies relative to the mineralized zone. A model involving two periods of glacial advance, in essentially opposite directions, appears necessary to reconcile a l l evidence. Tipper (1971a)" has discussed the evidence for multiple glaciation in central British Columbia. He suggested that a limited re-advance of ice took place after the main (Fraser) glaciation. Thus, the best explanation of the data is that a regional northeasterly moving ice sheet was followed locally by a southwesterly moving one. The later one caused the westerly displacement of silver anomalies in t i l l , the dispersion of granite boulders and planed the surface of some dykes, but did not scour deeply enough to remove a l l evidence (the glacial striae) of the earlier, regional, ice sheet. HISTORY The history of discovery of the Sam Goosly deposit as presented here is taken in large part from Ney et al (1972). In 1961, as part of regional geochemical surveys in British Columbia, the sediments of a stream east of Goosly Lake were found to be slightly anomalous in zinc and copper. This anomaly was not followed up until subsequent analyses of the samples disclosed anomalous fluorine values. With this amount of geochemical information, plus the knowledge that inliers of Mesozoic volcanic rocks in the Tertiary volcanic sequence existed in the area, an 5. exploration program was initiated in 1967, This deposit was probably-unknown prior to i t s discovery by Kennco Explorations in 1967. Prospecting in the area uncovered two types of mineralization: chalcopyrite in quartz monzonite and pyritized volcanic rock with one occurrence of tetrahedrite. At this stage claims were staked. Due to poor bedrock exposure, a s o i l sampling program was undertaken and yielded broad copper and molybdenum anomalies and a large silver anomaly. The copper-molybdenum anomaly led to weak porphyry-type mineralization in a quartz monzonite stock. The silver anomaly, interpreted with a westerly direction of transport of glacial t i l l led to d r i l l i n g targets which outlined the mineralized zone. Between I969 and 1 9 7 1 , diamond d r i l l i n g of 62 holes was completed and a 27 ton bulk sample was taken for metallurgical studies. Faced with the dual problem of a comparatively small tonnage and a metallurgically d i f f i c u l t ore, Kennecott Copper optioned the property to Equity Mining Capital (of Vancouver) and Congdon and Carey Mineral Exploration (of Denver) in 1972. Subsequently, additional d r i l l i n g and work on the metallurgical problems have been undertaken, METHODS OF STUDY The mineralized zone, as outlined by d r i l l i n g to 1971, has the form of a steeply dipping slab or lens., elongate parallel to strike. A number of cross sections along the length of the mineralized zone were selected for detailed observation and 6. sampling. These were holes 39 > 5&» 60 a n d 61 in the south, holes 12 and 48 farther north, holes 9 and 45 in the central zone, and holes 29 and 33 in the north (Fig. 3 ) . These were supplemented by a less detailed observation and sampling of other diamond d r i l l holes. These were holes 19, 20, 21, 22 and 3° which provided a complete cross section of the stratigraphy, hole 41 which passed through the facies change that distinguishes the southern cross section from those farther north, and hole 24 which had the longest ore-grade intersection. For comparative purposes, holes 1 to 8 which were studied by Nielsen (1969) were looked over, but not sampled in d e t a i l . Checks and some limited sampling were made on other diamond d r i l l holes. The s i l i c a t e mineralogy of rock samples was investigated by means of thin section and X-ray diff rac t ion work. For X-ray d i f f r a c t i o n , the rock was powdered and a whole rock sample was pro-duced by administering the powder to a glass slide as an acetone slurry. The clay mineral fract ion was investigated by allowing the rock powder to settle in a beaker of water for 15 seconds. A concentration of the l ighter clay fraction resulted by using an eye-dropper to extract the supernatant l i q u i d . This was then administered to a glass sl ide and allowed to dry for 6 hours or longer to produce an oriented clay f ract ion. The clay mineralogy of many specimens was investigated further by placing the sample in a sealed jar with an atmosphere of ethylene glycol for a period of several days (achieving glycolation of expandable clays), and/or by heating the sample in a muffle furnace at 600-650°C for at least 7. two hours. The cut surface of many rock samples were stained for potassic minerals using a hydrofluoric acid etch and a sodium cobaltinitrite stain. In addition, a limited investigation of the opaque mineralogy was carried out by examining a small suite of polished sections. 8. GEOLOGICAL SETTING INTRODUCTION The Houston map-area was f i r s t mapped by Lang (1942), and l a t e r re-examined by Tipper (1971b), Church (1973) has recently published a preliminary geological map of the Houston - Burns Lake area and Figure 2 i s a s i m p l i f i c a t i o n of a portion of that map. Most of the Houston map-area i s underlain by a diverse suite of Mesozoic volcanic and sedimentary rocks. In the southeast quarter of the map-area, these rocks are exposed as i n l i e r s or as windows through an extensive cover of Tertiary volcanic rocks. The Sam Goosly prospect occurs within one of these i n l i e r s , MESOZOIC STRATA The Hazelton Group consists of a diverse suite of volcanic and sedimentary rocks. Due to the paucity of, f o s s i l s and the l i t h o l o g i c v a r i a b i l i t y of these rocks, Lang (1942) had l i t t l e success i n subdividing the unit. However, two basic subdivisions have been achieved by Tipper (1970). The older unit consists of bedded green, gray and purple fragmental volcanic rocks of mainly andesitic composition. Sedimentary interlayers may be up to several hundred feet t h i c k and consist of impure limestone, shales, graywackes and r a r e l y cobble and pebble conglomerate. Their age was determined to be Sinemurian to Pliensbachian (Early Jurassic). The younger unit contains a higher proportion of sedimentary rocks of varied l i t h o l o g y . Tuff, breccia,shale and graywacke are 9. S A M GOOSLY PROSPECT REGIONAL G E O L O G Y ^jfter CHURCH, 1973) UPPER CRETACEOUS TIP TOP HIU VOLCANICS i*i£J ondesile lava and pyroclastics LOWER CRETACEOUS <-o |54°00'N o_ J overlain by fragmental andesitic to basaltic volcanic rocks. These volcanic rocks are in turn overlain by and interlayered with (?) black shale, minor graywacke and rare conglomerate lenses. The age of these rocks ranges from Bajocian to Callovian (Middle Jurassic). Windows of pre - Upper Cretaceous strata are scattered over Church's map-area. These consist mainly of acid and intermediate lavas and pyroclastics, with lesser amounts of argillite, sandstone and conglomerate. Until recently, these inliers were thought to belong to the Hazelton Group. Tipper now has evidence that some of these rocks are of Cretaceous age (pers. comm., 1973). Chert pebble conglomerates and shales outcrop near Francois Lake and north of Houston, The Francois Lake locality contains the pelycepods Aucellina (Aptian to Turonian) and Trigonia (Middle Triassic to Upper Cretaceous) while an ammonite Cleoniceras (Albian) was found at the Houston locality (Tipper, pers. comm., 1973). The Goosly Lake inlier, exposed between these two localities, contains similar chert pebble conglomerate and shale. Based on similar lithology, Tipper is confident that the rocks of this inlier are also of Albian (late early Cretaceous) age. With the exception of the Brian Boru Formation in the Rocher Deboule Range (Sutherland Brown, i960), Cretaceous strata were previously unknown in this part of north-central British Columbia. Tipper suggests that such rocks may be quite extensive but not recognized because they are generally unfossiliferous. In addition to the uncertainty regarding extent and correlation of these Cretaceous strata, the status of unfossiliferous rocks assumed to belong to the Jurassic Hazelton Group is not clear. 11. TERTIARY VOLCANIC SEQUENCE Church (1970) has subdivided the late Mesozoic to Tertiary-sequence into four volcanic units, with a total maximum thickness of about 1,300 m.(4,300 feet). (1) Tip Top Volcanics These are Upper Cretaceous (75.8 + 2.7 m.y.) in age and are 460 m, (1,500 feet) thick at their type locality. The rocks are volcanic breccias of andesitic to dacitic composition. They consist of about 35% plagioclase phenocrysts, together with accessory biotite, pyroxene and hornblende suspended in a fine-grained matrix. (2) Goosly Lake Volcanics This unit consists of 460 m. (1,500 feet) of mainly trachyandesite lavas, of Eocene age (48.0 + 1.8 m.y.). They are thought to be equivalent to the Ootsa Lake Group. Large lath-shaped plagioclase phenocrysts are distinctive of this unit, although they only account for about 15% of the rock. The plagioclase phenocrysts, together with accessory diopsidic augite, magnetite, biotite and hornblende are set in a fine-grained feldspathic matrix. (3) Buck Creek Volcanics These are basaltic andesite lavas of Eocene age (47.3 + 1.6 m.y.). The thickest section observed, along Klo Creek, measures 300 m. (1,000 feet). This unit is a typical 'plateau basalt* with gently dipping flows capping many of the hills and ridges of the area. The flows consist of 80% plagioclase microlites and 10% of pyroxene with the remainder being biotite, magnetite and chlorite. This unit is probably equivalent to the Endako Formation. (4) Poplar Buttes Volcanics This 70 - 100 m. (200 - 300 feet) thick unit of columnar olivine basalt forms the capping of some buttes in the area. The flows are of Miocene age (21.0 + 1,1 m.y.) and represent the youngest rocks of the area. These are undersaturated lavas, containing normative neph'eline. In thin section they contain J% olivine phenocrysts set in a fine-grained matrix of plagioclase microlites and ferromagnesian minerals. INTRUSIVE ROCKS The oldest intrusive rocks are the Topley Intrusions which are restricted to the northeast part of the Houston map-sheet. They are part of a batholith complex consisting mainly of quartz monzonite and granite, and are 138 + 3 m.y. in age ( White, Sinclair, Harakal and Dawson, 1970), A medium-grained diorite s i l l (7^.0 + 1.0 m.y.) is exposed at the Nadina Mine, east of Owen Lake. Locally, this is known as the Mine H i l l microdiorite and is thought by Church (1970) to be a feeder to the Tip Top Hi l l Volcanics, Granitic intrusions younger than the Topley Intrusions are also exposed in the area. Church (1970) reported that these stocks are texturally porphyritic or microporphyritic with 20-50% plagioclase phenocrysts in a quartz-feldspar matrix. 1 3 . The femic minerals are biotite and hornblende. One such stock outcrops on the Sam Goosly property. Probably the most interesting intrusions in the area are a series of gabbro-monzonite stocks, Petrographically, they consist of 65-80% plagioclase (as large bladed phenocrysts), 5-20% augite, and accessory biotite, magnetite and apatite. Interstitial potassium feldspar and minor quartz complete the monzonite phase, whereas pyroxene and relict olivine crystals complete the gabbroic phase. Three stocks of this compositional range lie at approximately 13 km, (8 miles) intervals along an east northeasterly striking line. The mineralized zone at Sam Goosly lies immediately west of the most easterly of these intrusions. Distinctive, bladed feldspar porphyry dykes, similar to these stocks, are exposed at the Nadina Mine, 40 km, (25 miles) west southwest of Sam Goosly. Their presence may indicate a similar gabbro-monzonite stock hidden at depth and would extend the number of these aligned stocks to four. Church has shown these intrusions to be the source of the petrographically and chemically similar Goosly Lake Volcanics, MINERALIZATION Good coverage of the mining properties and description of mineral showings in the area are provided by Church (1969, 1970). The two most important properties in the area are Sam Goosly and the recently closed Nadina Mine operated by the Bradina Joint Venture. Sam Goosly consists of disseminations of fine-grained 14. sulphides with local lenses of more massive, coarse-grained s u l -phides. The principal sulphide and oxide minerals are pyri te , ' chalcopyrite and tetrahedrite with lesser amounts of sphalerite, magnetite, hematite and pyrrhotite. Mineralization at Nadina Mine is in veins which consist of sphalerite, pyri te , chalcopyrite, galena and tennantite (Church, I969). Veins are generally one metre (3 to 4 feet) wide, and exhibit a symmetric encrustation of ore and gangue minerals. Church (1969, 1970) has suggested that these two deposits are complementary and taken together represent the complete range of a single ore-forming process. This i s supported by the close spatial association of both deposits with a stock, or related dykes, of nearly identical monzonite. GEOLOGY OF SAM GOOSLY 15. INTRODUCTION At Sam Goosly Cu-Ag mineralization occurs as a generally conformable layer within Mesozoic volcanic and volcanoclastic rocks. Two stocks and a number of dykes intrude the Mesozoic strata, A quartz monzonite stock outcrops west of the mineralized zone and a gabbro-monzonite complex stock lies to the east. Three sections, equally spaced at thousand foot intervals along the main part of the mineralized zone, were selected for detailed study of the alteration associated with mineralization. These are Section 13,400 N (Fig. 4, d r i l l holes 29 and 33) at the northern end, Section 12,400 N (Fig. 5, d r i l l holes 9 and 45) near the centre and Section 11,500 N (Fig. 6, d r i l l holes 12 and 48) at the southern end. Mineralization extends southwestward as a narrow zone and Section 9,100 N (Fig. 7, d r i l l holes 39. 56, 60 and 6l) was selected to examine the associated, alteration. In addition, a section between the two stocks, through d r i l l holes 19, 20, 21, 22, 5 and 30 (Fig. 8, approximately 11,800 N) was also studied. This section, with the addition of holes 11 and 23 was studied by Church (1970) and by Ney et al (1972). D r i l l holes 12 and 48 have been projected less than 300 feet into this section. The geological map (Fig. 3) is a combination of surface geology mapped by Kennco geologists and d r i l l hole data projected to surface by the author. The outline of the mineralized zone was obtained from Equity Mining and is based on more detailed drilling, not shown in Fig, 3. 16. LEGEND ( f o r F i g u r e s 4 t o 8) EOCENE OR YOUNGER EOCENE E P A L E O C E N E D LOWER CRETACEOUS B, B, A Q u a r t z l a t i t e d y k e s T r a c h y a n d e s i t e d y k e s ( B l a d e d f e l d s p a r p o r p h y r y ) A n d e s i t e d y k e s ( a p h a n i t i c ) B i o t i t e p y r o x e n e m o n z o n i t e ( G a b b r o - m o n z o n i t e c o m p l e x ) B i o t i t e q u a r t z m o n z o n i t e S e d i m e n t a r y - v o l c a n i c d i v i s i o n W e l d e d a s h t u f f D u s t t u f f E p i c l a s t i c s V o l c a n i c b r e c c i a s B r e c c i a t e d d a c i t e B a s a l p y r o c l a s t i c s C o a r s e c l a s t i c d i v i s i o n •? G e o l o g i c c o n t a c t , o b s e r v e d — G e o l o g i c c o n t a c t , p r o j e c t e d ? - G e o l o g i c c o n t a c t , i n f e r r e d - i — S c o r z a l i t e z o n e - n - A n d a l u s i t e z o n e C o r u n d u m z o n e M i n e r a l i z a t i o n ( e q u i v a l e n t t o 3 o u n c e s s i l v e r p e r t o n ) M i n e r a l s a - a n d a l u s i t e b - b i o t i t e c - c o r u n d u m d - d u m o r t i e r i t e p - p y r o p h y l l i t e s - s c o r z a l i t e s p - s p i n e l T- t o u r m a l i n i z a t i o n I 13.500E 14,000E 3 14.500E FIGURE 4 .. • SECTION 13,400N GEOLOGY 'AND ALTERATION 4,000-H 3,50(H 21. SECTION 11.800N (APPROX.) F/GUKE. | \— 4 4 0 0 •4 0 0 0 • 3 6 0 0 r — 3 2 0 0 GEOLOGY A N D ALTERAT ION 1 2 . 0 0 0 E 1 3 . 0 0 0 E 1 4 . 0 0 0 E 3 6 0 0 -3 2 0 0 -1 5 . 0 0 0 E MESOZOIC ROCKS The Lower Cretaceous inlier has been subdivided into a lower coarse clastic division (unit A), a middle pyroclastic division (unit B) and an upper sedimentary-volcanic division (unit C) by Ney et al (1972). These are retained in this study but the middle pyroclastic division has been further subdivided. Clastic Division (Unit A) The lower division consists mainly of conglomerate with lesser amounts of argillite and sandstone. Ney et al (1972) have further subdivided the unit into a lower polymictic conglomerate and an upper chert pebble conglomerate. The gradational change in the conglomerate unit can be seen in d r i l l hole 52 (6,000 N, 12,620 E) but the lower subdivision does not occur within the area shown in Fig. 3. Ney et al estimate a maximum thickness of 8,000 feet for the clastic division. Local intercalations of well indurated chert pebble conglomerate persist into the pyroclastic division. These horizons are in marked contrast to the immature, poorly sorted volcanic conglomerates, dust tuffs and volcanic breccias of the pyroclastic division, and suggests an interplay of two sources. Very well-washed chert pebble conglomerates may represent a shoreline facies (Tipper, pers. comm., 1973). 23. Pyroclastic Division (Unit B) The pyroclastic division is host for Gu-Ag mineralization and is the most economically important of the three divisions. Within limits of d r i l l hole information,>it is about 2,500 feet thick, but lateral facies changes could produce significant thick-ness variations. In logging core, Kennco geologists distinguished among dust, ash and l a p i l l i tuff, and volcanic breccia based on maximum particle diameters of 0,5 mm., 5 mm. and 50 mm. respectively. A subdivision based on fragment size is unsuccessful because not a l l of these rocks were of pyroclastic origin and units defined by fragment size cannot be correlated between d r i l l holes (see Ney et a l , f i g . 5» p. 57). For these reasons a subdivision based on rocfcftypes has been used here, and these units are described below. Basal Pyroclastics (Unit B^) These are mainly tuffs and flow breccias. They commonly contain numerous blocky pseudomorphs of pyroxene phenocrysts and, less commonly, altered plagioclase phenocrysts (photograph l ) . Only altered primary minerals are present, but pyroxene and plagioclase with l i t t l e quartz suggest the original volcanic was of intermediate composition. Accidental chert fragments are numerous and undoubtedly were derived from the underlying chert pebble conglomerate,. Of six units of the pyroclastic division this one is the least clearly defined. It is not extensive as It occurs only in d r i l l holes 7$ 9» 29 and 45. In these holes i t has been intruded by the gabbro-monzonite stock, so that the base of the unit has not been observed. Photograph 2 Brecciated dacite u n i t , with Cu-Ag m i n e r a l i z a t i o n . 25. A minimum thickness of the "basal pyroclastic unit is 100 feet. The transition with the overlying brecciated dacite is sharp but that with the volcanic breccias is gradational, Brecciated Dacite (Unit B,,) This is a brecciated rock composed of light-coloured aphanitic fragments in a dark, commonly sulphide-rich matrix (photograph 2). The original nature (before brecciation) of this rock is uncertain. It has been referred to as a "brecciated dust tuff" by Ney et al and as a "shattered dacite (possibly an autobrecciated lava dome)" by Church (1970). Considerable similarity between these brecciated rocks and rocks considered by Horikoshi (1969) to be part of autobrecciated dacite lava domes supports Church's (1970) suggestion. Because of intense alteration the writer did not find sufficient evidence to decide i f these rocks are a dust tuff or a fine-grained lava. The lower contact of this unit is sharp but upwards the unit grades into volcanic breccias . This unit is exposed in d r i l l core and in the adit and decline that was constructed in 1973. The brecciated dacite is approximately 300 feet thick, and of limited areal extent. Volcanic Breccias (Unit B^) These are coarse volcanoclastic rocks (photograph 3). The aphanitic fragments range in size from 0.5 to 5 centimetres. They are predominantly acidic volcanics, although locally several texturally different types may be present. Within a hand specimen, fragments- vary from rounded Photograph 3 Volcanic breccia unit; specimens 1 and 2 may be lahars; l i g h t pink colour i n specimen 5 i s dumortierite. Photograph 4 E p i c l a s t i c unit. to very angular. Some specimens consist predominantly of fragments but others are a chaotic mixture of fragments supported in a very fine-grained "muddy" matrix. Some of these latter rocks are very similar to rocks described by Fiske (1963) as "subaqueous pyroclastic flows". However, unlike the stratigraphic sequence Fiske was studying, there are no turbidite beds at Sam Goosly. Mud-supported fragmental rocks at Sam Goosly may be mud flows or lahars. In other rocks the fragments exhibit a pronounced selvage or onion-skin texture, as though the fragment was hot at the time of deposition. Such rocks may represent a true pyroclastic accumulation. This unit is quite diverse and tends to include a l l rocks that cannot be recognized as belonging to one of the other units. The volcanic breccia unit is broadly equivalent to the undivided pyroclastic division in the southern part of the map-area. The thickness is clearly variable, but in the central part of the property is approximately 1,000 feet. Epiclastics (Unit B^) A number of lenses of volcanic conglomerate and sandstone occur within the volcanic breccia unit (photograph 4). If the volcanic breccias are partly lahars, intercalated epiclastic layers would be expected. These epiclastic rocks are usually poorly sorted and clasts up to several centimetres in diameter range from subangular to subrounded. Locally they show size sorting and, possibly, graded bedding. The clasts are usually aphanitic but here and there, plagioclase or rare ferromagnesian phenocrysts develop. Unaltered primary minerals are absent. In d r i l l hole 48, the f i r s t 200 feet are volcanic sandstone and conglomerate of a thick e p i c l a s t i c lens. Dust Tuffs (Unit B^) These are very fine-grained pyroclastic rocks (photograph 5) that interfinger with the coarser volcanic debris. Ney et a l aptly described these rocks as being "peculiarly massive for many tens of feet without change of grain size or recognizable bedding." Although primary internal structures are lacking, c h l o r i t e has formed p a r a l l e l to the bedding i n some rocks. In t h i n section, dust t u f f s that were not strongly altered, contain angular quartz and feldspar c r y s t a l fragments, and sparse l i t h i c fragments up to 0.1 mm, in s i z e , but no glass shards. Brecciation i s present, but i s not as intense as that i n the brecciated dacite unit. Much of the rock exhibits a r e t i c u l a t e fracture pattern. Welded Ash Tuff (Unit Bg) These rocks are predominantly ash and l a p i l l i t u f f s with welded fragments and glass shards (photograph 6). The fragments are angular and aphanitic. Locally porcellaneous dust t u f f s are present. These are very s i m i l a r to some porcellaneous v a r i e t i e s of the dust t u f f unit (B^) f except that the dust t u f f s of Bg are welded. The l a p i l l i t u f f s of t h i s unit may be contrasted with the underlying volcanic breccia unit (B^). In unit B,, a l t e r a t i o n and r e c r y s t a l l i z a t i o n Photograph 6 Welded ash tuff unit; specimens 2 and 3 are welded. have strongly affected the breccia matrix, and fragments may be corroded, with hazy and indistinct boundaries. In comparison, rocks of Unit Bg are unaltered. The transition between the volcanic breccia and welded ash tuff units i s sharp in d r i l l hole 33, but gradational in d r i l l hole 22. The welded ash tuff unit i s approximately 1,200 feet thick. Sedimentary - Volcanic Division (Unit C) This is the third major division of the Mesozoic strata made by Ney et a l . Rocks of this division were seen only in d r i l l hole 19 and consist of well-bedded tuff, tuffaceous a r g i l l i t e , quartzite and pebble conglomerate. Contact with the dust tuff (Bg) is gradational and the boundary is placed at the point at which good bedding develops. Comparison of Geologic Sections Geologic sections corresponding to Fig, 8 have also been drawn by Ney et a l and by Church (1970). The most useful comparison' is with Church's section. The chert pebble conglomerate at the base of Church's section probably corresponds to the basal pyro-clastic unit (B^) with abundant accidental chert fragments. In d r i l l hole 7, 250 feet north of Church's section, chert pebble conglomerate is interbedded with pyroclastic rocks. Boundaries of the brecciated dacite (B^) correspond to Church's shattered dacite. The association of economic sulphide mineralization with this rock type is also indicated by Church, Church noted "a progressive increase stratigraphically downward in the volume of tuff breccia and coarse volcanic debris". This change occurs as shown schematically between d r i l l holes 21 and 22 and corresponds to the gradational change between the volcanic breccias (B^) and welded ash tuff. (Bg). Many epiclastic lenses (B^) occur stratigraphically higher than indicated by Church and consist predominantly of volcanic detritus rather than chert. Minor chert pebble conglomerate lenses are intercalated with the volcanic breccias elsewhere (see Fig. 4 ) . The "laminar bedded tuffaceous a r g i l l i t e " in d r i l l hole 19 corresponds to the base of the sedimentary - volcanic division (c). Thus, when considered carefully, the correspondence between Church's section and Fig. 8 is good. Composition of Mesozoic Volcanic Rocks The original composition, both mineralogically and chemically, of the Mesozoic volcanic rocks is problematical. Alteration i s widespread, so that primary mineralogy i s not preserved. Most rocks have a low colour index and contain abundant quartz so that an acidic composition may be deduced. The chemical composition of a suite of 15 lava and pyroclastic rocks from Sam Goosly was estimated by Church (1969) using the method of Mathews (1951). This method involves arc fusion of the sample and measurement of the refractive index of the glass. By this method, the volcanic rocks are dacitic, with a narrow compositional range from rhyodacite to dacitic andesite, Large scale chemical changes have taken place during alteration TABLE 1 Chemical Composition 'of Lower Cretaceous Volcanic Rocks at Sam Goosly (Church, 1973> pers, comm.) s i o 2 65.72% T i 0 2 0.98 A1 20 3 18.95 F e 2 ° 3 . 1.42 FeO 3.77 MnO 0.09 MgO 1.39 CaO 1.03 Na20 0.72 K 20 2.42 p2°5 0.09 SO^ 0.48 C 0 2 0.01 H 20 + 2.80 H2°" 0.22 100.09 % 33. TABLE 2 Comparison of Sam Goosly and Nockold's (1954) Average Volcanic Rocks on a Water-Free Basis Sam Goosly Andesite Dacite Rhyodacite Rhyplite S i 0 2 67.72 54.68 63.95 66.72 74.24 T i 0 2 1.01 1.32 0.64 0.66 0.22 A 1 2 ° 3 19.53 17.32 16.76 15.50 13.56 F e 2 0 3 1.46 3.51 2.25 2.15 1.26 FeO 3.89 5.54 3.02 2.25 0.76 MnO 0.09 0.15 0.11 0.07 0.03 MgO 1.43 4.39 2.13 1.58 0.32 CaO 1.06 7.99 5.56 3.71 1.14 Na 20 0.74 3.70 4.00 4.16 3.01 K20 2.49 1.12 1.41 3.03 5.39 p2°5 0.09 0.28 0.17 0.17 0.07 so 3 0.49 _ _ _ _ 100.00 100.00 100.00 100.00 100.00 Molecular Normative Minerals Qtz 46.2 5.8 19.7 20.9 33.5 Or 15.1 6.8 8.3 17.9 31.9 Ab 6.8 31.3 34.4 35.4 25.3 An 5.0 27.4 23.4 14.6 5.0 Cor 15.6 - - - 0.9 Wo - 4,2 1.3 1.3 -En 4.1 11.0 5.3 3.9 0.8 Fs 3.5 5.3 2.8 1.3 -Mt 1.6 5.1 3.3 3.0 1.9 Ilm 1.4 2.4 1.2 1.4 0.5 Py 0.5 - - - -Ap 0.2 0.7 0.3 0.3 0.2 o f some r o c k s a n d i t s e f f e c t o f t h e r e f r a c t i v e i n d e x i s n o t c e r t a i n . A w h o l e r o c k a n a l y s i s o f a c o m p o s i t e o f t h e 15 s a m p l e s w a s d o n e a n d i s p r e s e n t e d i n T a b l e 1 ( f r o m C h u r c h , 1 9 6 9 ) . F o r c o m p a r i s o n , t h e a n a l y s i s i s r e c a l c u l a t e d t o 100 p e r c e n t a n d t a b u l a t e d w i t h N o c k o l d ' s ( 1954 ) a v e r a g e a n d e s i t e , d a c i t e , r h y o d a c i t e a n d c a l c -a l k a l i r h y o l i t e ( T a b l e 2 ) . T h e r e s p e c t i v e i g n e o u s m o l e c u l a r n o r m s a r e i n c l u d e d . T h e p u r p o s e o f t h i s c o m p a r a t i v e t a b l e w i l l b e d i s -c u s s e d i n a l a t e r c h a p t e r . T h e a n o m a l o u s c o m p o s i t i o n o f t h e v o l -c a n i c r o c k s i s r e a d i l y a p p a r e n t i n t h e n o r m a n d t h i s i s m o s t p r o b a b l y d u e t o a l t e r a t i o n . T h e c l o s e s t m a t c h i s w i t h a r o c k o f d a c i t e t o r h y o d a c i t e c o m p o s i t i o n , T E R T I A R Y STRATA A t Sam G o o s l y , g e n t l y d i p p i n g T e r t i a r y v o l c a n i c r o c k s c o n s i s t m a i n l y o f d i s t i n c t i v e b l a d e d f e l d s p a r p o r p h y r y l a v a s o f t r a c h y -a n d e s i t e c o m p o s i t i o n , n a m e d G o o s l y L a k e V o l c a n i e s b y C h u r c h ( 1 9 6 9 ) . T h e s e f l o w s s u r r o u n d M e s o z o i c s t r a t a e x c e p t t o t h e w e s t a n d n o r t h -w e s t w h e r e t r a c h y t e s o u t c r o p . T h e t r a c h y t e i s a l o c a l c o m p o s i t i o n a l v a r i a n t o f t h e t r a c h y a n d e s i t e . I n t h e f a r n o r t h w e s t c o r n e r o f t h e p r o p e r t y , G o o s l y L a k e V o l c a n i e s a r e o v e r l a i n b y p l a t e a u b a s a l t s o f t h e B u c k C r e e k V o l c a n i e s . 35. INTRUSIVE ROCKS Quartz Monzonite A compositionally homogeneous quartz monzonite stock is exposed near the western edge of the Mesozoic inlier. It is approximately 2.2 km. (1.3 miles) long by 0.9 km. (0.5 miles) wide and elongated northerly. Texturally, i t is microporphyritic with subhedral microphenocrysts of plagioclase set in a fine-grained matrix of quartz potash feldspar and biotite. Church (1969) determined the mineralogy and chemical composition of a typical specimen, and these appear in Table 3. Two biotite potassium-argon age determinations have been made on independently prepared concentrates taken from the same sample. Geochron Laboratories determined the age to be 6l.l m.y. (no error limits given by Ney et al), and N.C. Carter at U.B.C. obtained a value of 56.2 +3.0 m.y. (Church, I969). The stock intrudes Mesozoic rocks. Only weak sulphide mineralization occurs within the stock. Ney et al reported that"extensive fracturing, sericitization, and copper - molybdenum mineralization" are present at the north end of the stock. Veinlets containing tetrahedrite outcrop at another locality toward the south end. Gabbro - Monzonite Complex Because this stock is close to the mineralized zone and is compositionally complex, i t has received much attention. It is located east of the quartz monzonite at the eastern margin of the Mesozoic inlier. The stock is roughly circular in plan TABLE 3 Chemical Ana lyses of I n t r u s i o n s and T e r t i a r y Lavas a t Sam Goosly (from Church , 1969) Quartz monzonite Monzonite Goosly Lake Tra chyande s i t e S i 0 2 65.02 52 .80 55.86 T i 0 2 O.65 1.82 1.26 A 1 2 ° 3 15.76 16.95 17.52 F e 2 ° 3 2.12 3.97 4.95 FeO 1.54 3.63 • 1.41 MnO 0 .04 0 .14 0 .08 MgO 1.27 3.85 3.16 CaO 3 .21 6.03 6 .18 Na 2 0 4 .21 4 .10 4.13 K 2 0 3.59 3.30 2.05 H 2 0 + I.69 1.90 1.17 H 2 0 " 0 .21 0 .18 1.44 C 0 2 0 .08 0 .02 0.02 P 2°5 0.28 0.91 0.44 s o 3 0.01 0 .01 0 .02 BaO 0 .18 99.68 0 . 2 7 99.68 0.18 99.87 Modal Ana lyses P l a g i o c l a s e 50 58 ( A n ^ ) K - f e l d s p a r 19 25 Quartz 25 2 A u g i t e - 8 B i o t i t e 4 2 Magnet i te 2 5 A p a t i t e - 1 and measures about 2.5 km. (1.7 miles) across. Ney et al distinguished six plutonic and hypabyssal phases. Large feldspar laths in a trachytoid alignment is a distinctive textural feature common to a l l phases. The most basic phase is a gabbro containing 60 per cent labradorite and 30 per cent augite, with accessory biotite, magnetite and apatite. Quartz and potash feldspar occur locally as micrographic intergrowths along margins of plagioclase phenocrysts. With a slight decrease in anorthite content of plagioclase, and an increase in the amount of interstitial potassium feldspar, the gabbro grades through diorite to monzonite. An increase in biotite and a decrease in augite accompanies this transition. The monzonite phase is considerably larger than the basic phases and intrudes -themineralized volcanic rocks. Modal and chemical analyses of this main phase (Table 3) show the monzonite is enriched in P 2 05* T n i s i s corroborated by Ney et al who stated that the apatite content may amount to as much as 5 per cent. The gabbro - monzonite stock does not contain Cu-Ag mineralization and is only weakly altered. Pyroxenes are variably uralitized to a mixture of amphibole, chlorite and calcite, and potassium feldspars may be clouded, but plagioclase is unaltered. Of the remaining three phases of the complex distinguished by Ney et al, one is a series of bladed feldspar porphyry dykes, another is a "dyke-like" body of biotite monzonite, and the third is a large body of unknown form that merges to the north with lavas of the Goosly Lake Volcanies. There appears to be a genetic relationship between the plutonic rocks, hypabyssal rocks, and lava flows. Based on a comparison of the chemical analyses of the monzonite and Goosly Lake trachyandesite (Table 3) and mineralogical and textural s i m i l a r i t i e s , Church (1969, 1970) suggested the stock is the core of a volcano, surrounded by i t s own eruptives. Bioti te potassium-argon ages of 48.3 +3.0 m.y. for the monzonite, and 48.0 + 1,8 m.y. for the trachyandesite flows, are reported by Church (1973). Ney et a l reported a biot i te potassium-argon age of 52.5 m.y. (no error l imits given) for the monzonite. Dykes and S i l l s A large number and. variety of dykes and s i l l s cut the Mesozoic strata. They are part icularly abundant between the quartz monzonite stock and the gabbro - monzonite complex, and account for 15 per cent (Ney et al ) to 20 per cent (Church, 1970) of the rocks. A comparison of northern and southern sections (Fig, 4 and F i g . 7) indicates the number of dykes diminishes southwards. Neilson (1969) ident i f ied three types of dykes and s i l l s ; gray andesite porphyry (bladed feldspar porphyry), l ight greenish-gray altered andesite, and chalky white altered quartz l a t i t e porphyry. Neilson observed, and the writer concurs, that fresh bladed feldspar porphyry dykes grade into altered, aphanitic andesite dykes. Andesite porphyry and aphanitic andesite dykes are very abundant and individual bodies cannot be correlated between d r i l l holes. Those exposed in the adit strike at 060° to 100° 39. and dip steeply southward to v e r t i c a l . Most are 1 to 2 metres thick, although dykes up to 10 metres in apparent thickness have been seen in d r i l l core. The presence of bladed plagioclase phenocrysts strongly suggests that the dykes are consanguinous with the gabbro - monzonite complex. Fresh porphyritic varieties are texturally and mineralogically similar to the monzonite phase of the intrusive complex. Altered aphanitic dykes consist of chlori te , a lbi te and carbonate. Pale gray to chalky white quartz l a t i t e dykes form a much less abundant, but dis t inct ive , type. These contain 2 - 4 mm. plagioclase phenocrysts, 2 - J mm. quartz phenocrysts and flecks of bioti te in a fine-grained micrographic matrix of quartz and potash feldspar. Plagioclase and biot i te phenocrysts are altered to mixtures of chlori te , s e r i c i t e , a lbi te and ca lc i te , and potash feldspar of the matrix i s clouded by incipient clay al terat ion. Scattered cubes of pyrite are common. Quartz l a t i t e dykes are far fewer, but thicker, than andesite dykes. In outcrop and i n the adi t , these dykes strike about 125° and dip steeply to the southwest. Because of their thickness and rar i ty they can be correlated between d r i l l holes with some confidence. Rare, small aphanitic f e l s i t e dykes are similar in colour and may be related to the quartz l a t i t e dykes. A l l dykes cut Cu-Ag mineralization in the volcanic rocks. Even though the host rocks may consist of massive sulphides, the dykes are sparingly pyri t ized or are unmineralized, and therefore post-date Cu-Ag mineralization. Andesite porphyry dykes are intrusive into the quartz monzonite stock. A thick 40, quartz l a t i t e dyke cuts the gabbro-monzonite complex. In d r i l l core, quartz l a t i t e dykes cut andesite dykes. The intrusive history is summarized below. (1) Intrusion of the quartz monzonite stock at 59 + 3 m.y, (average K-Ar date), (2) Differentiation and intrusion of the gabbro-monzonite complex at 51 + 3 m.y, (average K-Ar date), accompanied by a variety of andesite, commonly bladed feldspar porphyry dykes, and by extrusion of the Goosly Lake Volcanics, (3) Intrusion of quartz l a t i t e dykes, STRUCTURE The structure of the Mesozoic volcanic strata is a simple homocline with tops facing west as suggested by Church (1970), Ney et a l (1972) and accepted in this study. Bedding attitudes near the mineralized zone consistently strike about 025° and dip steeply (60° - 8 0 ° ) westerly. Therefore sections defined by d r i l l holes are not necessarily normal to strike (Fig. 4 to 8). In the central part of the property, the strike apparently changes to 000° and sections are nearly perpendicular to s t r ike . Corrections of apparent dips measured from sections 11,500N, 12,400N and 13,400N indicate true dips to be 55°, 50° and 75° respectively. Top deter-minations from graded sandstone beds, both in outcrop and in d r i l l core, indicate that the section is the right way up. The contact of the gabbro-monzonite stock dips at about 50°;westerly (Fig. 6 and 8), and is subparallel to the dip of volcanic strata near the main ore zone.' In d e t a i l , i r regular i t ies in the intrusive contact cut unit so that unit B^ is penetrated by some d r i l l holes, hut in others i t has been truncated by the intrusive stock (Fig. 8), Possibly the volcanic strata dip more steeply than the intrusive contact, as unit B^ is present in shallow d r i l l holes,(such as 7 and 9 ) , but rarely in deeper holes (such as 1 2 , 3 0 and 48). Such a relationship is inferred in F i g . 6 . 42. ORE MINERALOGY INTRODUCTION Considerable effort has been expended by Kennco and is being continued by Equity on studies of the ore mineralogy. These include work by Neilsen (1969), Mariano (I9?l), Gasparrini (1971) and Ney et a l (1972). A number of samples from various types of ore grade and sub-ore grade material were examined in order to correlate differences in metallic mineralogy with s i l i c a t e alteration mineralogy. METALLIC MINERALOGY Pyrite is the most important metallic mineral throughout the Mesozoic volcanic rocks regionally and within the zone of Cu-Ag mineralization in particular. Chalcopyrite, pyrrhotite, magnetite, hematite, tetrahedrite and sphalerite are other important metallic minerals that occur within the deposit. In addition, very minor amounts of unidentified sulphosalt (?) minerals, associated with chalcopyrite and tetrahedrite occur in some specimens. One specimen contains arsenopyrite. Traces of marcasite, argentite, pyrargyrite boulangerite, pearceite, berthierite and bournonite have been reported by Mariano, or by Ney et a l , but were not identified during this study. Gasparrini identified ,fre3bergite (tetrahedrite with more than 3% silver in solid solution). Should development of the property proceed, silver, copper and gold would be recovered using an open-pit mining operation. The amount of sphalerite i s not sufficient to economically recover zinc. DISTRIBUTION AND CHARACTER OF MINERALIZATION The character of mineralization exhibits a close relationship with specific host rocks of the local stratigraphic succession. The zone of Cu-Ag mineralization is broadly conformable with the volcanic strata. Metallic mineralogy associated with each unit i s described below. Chert pebble conglomerates of the coarse clastic division (A) intercalated with pyroclastic division rocks (B) contain pyrite cubes ( l mm.) disseminated throughout the matrix. The basal pyro-clastic unit (B^) contains up to 3 per cent finely disseminated pyrite and magnetite. Brecciated dacite (B^) is the most specific host rock for Cu-Ag mineralization and i s invariably associated with economic grades. Overall sulphide content i s also highest in this unit, ranging from less than 5 per cent to over 50 per cent locally. Sulphides occur as disseminations, veinlets or irregular masses within the breccia matrix. Typical specimens of disseminated sulphide ore contain an average of 10 per cent sulphide minerals, consisting of about 9 per cent pyrite, 1 per cent chalcopyrite and less than 1 per cent sphalerite, pyrrhotite and tetrahedrite. Pyrite grains range from 0 , 0 2 mm, to 1 mm,, chalcopyrite from 0 , 0 1 to 0 . 1 mm.; sphalerite i s about 0 , 0 3 mm. a n ( i tetrahedrite is about 0 . 0 1 mm. Grain size becomes more variable in zones of mas-sive sulphide but generally increases to several millimetres. The proportion of minerals i s extremely variable; pyrite 30-80 per cent, magnetite 10-60 per cent, chalcopyrite 5-20 per cent, sphalerite 0-20 per cent and pyrrhotite 0-60 per cent. Brecciated dacite does not extend to the northern part of the ore zone (D.D.H. 24 and 29 ) . Here, sulphides are in the matrix of volcanic breccia ( B 3 ) . Volcanic breccias (B^) and epiclastics (B^) overlying Cu-Ag mineralization contain disseminated pyrite and local zones of massive sulphide, consisting of about 70 per cent pyrite, 0-30 per cent magnetite and 0-30 per cent specular hematite. The average grain size i s 1 to 2 mm, Massive zones may contain millimetre-size vugs lined with specular hematite, or more rarely pyrite, Stratigraphically upwards, disseminated and massive forms diminish and in the welded ash tuff rare 2 mm, pyrite veins account for much less than one per cent of the rock. The character of mineralization changes as the ore zone is followed southward along strike into dust tuff (B^), In the north economic grades are maintained over more than 200 feet (true thickness), but southward the ore zone narrows to less than 50 feet in By The main ore control is intensity of fracturing and brecciation. Total sulphide content of the ore rarely exceeds 20 per cent. The decrease in total sulphide content from the main ore zone to the north, i s principally due to a large decrease in pyrite. Outside the ore-zone c h l o r i t e - f i l l e d fractures range from hairline width to 1 cm. These fractures usually have pyrite, or rarely chalcopyrite, at their core. Locally, a network of fractures may progress into a chlorite-cemented breccia, Brecciation be-comes very important in the ore zone where breccia fragments are Photograph 7 0.005 0^01 mm. Vein ore in dust tuff unit. Surface coating of tetrahedrite (gray) and chalcopyrite (gold) on pyrite (pale yellow). 0.5 L _ mm. Photograph 8 Breccia zone in dust tuff unit,cemented by chalcopyrite 46. cemented by sulphides and vein quartz. Sulphides do not occur as very fine-grained disseminations in the matrix, as in brecciated dacite, but form vein structures and f i l l open spaces between breccia fragments. Symmetric banding and textures such as those shown in photograph 7 indicate the paragenetic sequence i s pyrite, tetra-hedrite, chalcopyrite. Commonly the dust tuff has been very weakly brecciated, or "crackled" and the cement of such a breccia may consist solely of chalcopyrite (photograph 8), or i n other areas, of sphalerite. In rocks that are more strongly brecciated, the cement consists of vein quartz, pyrite, chalcopyrite, sphalerite, tetrahedrite and tourmaline. Sulphide grain size varies from 0,5 to 5 m m « MINERAL ZONING Church (1969) sampled the brecciated dacite at the creek exposure of the ore zone (12,200N, l4 ,600E) and i t assayed: gold, 0,05 ounces per tonj silver, 4.7 ounces per ton; copper, 1.04 per cent; zinc, 0.23 per cent; lead, 0,015 per cent; antimony, 0,10 per cent. This is approximately twice the average grade of the main ore zone. The silv e r to copper ratio for this sample i s 0,016 which i s similar to ratios from d r i l l core inter-sections of the brecciated dacite in D.D.H. 7, 9f and 45. Silver to copper ratios were also calculated from d r i l l core assays of the other d r i l l holes studied. These show an erratic distribution in the main ore zone but range from 0.016 up to 0.05. The narrow, southern extension of the ore zone has a lower silve r content, and silve r to copper ratios are typically 0,01. On the basis of the 25 polished sections studied, tetrahedrite, the main silver-bearing 0.05 O.l^mm. Photograph 9 Pyrite aggregate with randomly d i s t r i b u t e d s i l i c a t e inclusions. 48. mineral, tends to occur in zones of disseminated sulphides, not with massive sulphide, MINERAL TEXTURES In the main ore zone, pyrite commonly occurs as highly i r r e -gular crystal aggregates, with randomly distributed gangue material (photograph 9). In other samples, pyrite crystals may be euhedral and contain zones of inclusions parallel to crystal boundaries (photograph 10). Similar, euhedral single crystals of pyrite become visible macroscopically adjacent to the thick quartz l a t i t e dyke and the gabbro-monzonite complex. In D.D.H. 48 these pyrite crystals increase in size from 2 mm, at 175 feet from the contact to 10 mm. adjacent to the contact. Because these are single, euhedral crystals with inclusions, and not anhedral crystal aggregates, they : are probably pyrite porphyroblasts rather than clastic fragments, Pyrite porphyroblasts in sulphide mineral deposits probably result from metamorphism (Vokes, 1969). Stanton (1972) proposed a sulphide -oxide - s i l i c a t e idiomorphic sequence based on studies of metamorphosed sulphide deposits, Pyrite is high in the sequence, comparable with garnet and, like garnet, tends to form porphyroblasts. Chalcopyrite, tetrahedrite and pyrrhotite are low in the sequence and are comparable with chlorite. These minerals tend not to recrystallize as idiomorphic porphyroblasts. Photograph 11 shows pyrrhotite i n t e r s t i t i a l to granoblastic quartz. In the hanging wall of the main ore zone, specular hematite extensively replaces magnetite (photograph 12), Hematite is later than magnetite and becomes more prevalent than magnetite s t r a t i -49. 0 0 .1 0.2 mm. Photograph 11 P y r r h o t i t e i n t e r s t i t i a l to granoblastic quartz (adjacent to quartz l a t i t e dyke). graphically upwards. Appearance of hematite corresponds approxi-mately with the lower boundary of the corundum alteration zone (p. 6l) Sphalerite in the main ore zone contains blebs of chalcopyrite (photograph 13). These are due to unmixing of chalcopyrite originally-contained within host sphalerite (Stanton, 1972). Stanton noted that unmixing of sphalerite from a chalcopyrite host is much less common. In two specimens, chalcopyrite contains 'stars* of exsolved sphalerite (photograph Ik), 51. 0 0 . 1 0 , 2 m m . I I I Photograph 14 'Stars' of sphalerite exsolved from chalcopyrite. 5 2 . ALTERATION AND METAMORPHISM INTRODUCTION Four types of a l t e r a t i o n and metamorphism are recognized i n the Lower Cretaceous rocks at Sam Goosly, (1) Aluminous a l t e r a t i o n i s characterized by a suite of aluminous minerals including s c o r z a l i t e , andalusite, pyrophyllite and corundum. A l t e r a t i o n zones are conformable with some stratigraphic boundaries but crosscut others. These a l t e r a t i o n zones also show a systematic s p a t i a l relationship to the mineralized zone. ( 2 ) Quartz-muscovite a l t e r a t i o n i s associated with brecciation and mineralization i n the dust t u f f ( B ^ ) . (3) Regional metamorphism has affected a l l volcanic rocks, producing a p r o p y l i t i c , or greenschist, assemblage of muscovite, c h l o r i t e , a l b i t e , k a o l i n i t e , quartz and carbonate. Proportions of these minerals are determined by the nature of the host rock, (4) Contact metamorphism by the gabbro-monzonite resulted i n a narrow, discontinuous zone of b i o t i t e hornfels and a more extensive zone of r e c r y s t a l l i z e d pyrite porphyroblasts. Potash feldspar has developed adjacent to the quartz monzonite stock. ALUMINOUS ALTERATION The alumina-rich minerals andalusite, corundum, pyrophyllite, dumortierite, s p i n e l , s c o r z a l i t e and a u g e l l i t e are developed i n units B 0 , B ^ , B k , and B g . , They form three a l t e r a t i o n zones: s c o r z a l i t e , 53. TABLE 4 Mineralogy of Aluminous A l t e r a t i o n Mineral and Chemical Composition Andalusite, A l o S i 0 c 2 5 A u g e l l i t e , Al 2(PO^)(OH) 3 Corundum, A 1 2 0 3 Dumortierite, AlgSi 3B0 1 9(OH) Pyrophyllite, A l 2 S i i + 0 1 0 ( 0 H ) 2 S c o r z a l i t e , (Fe,Mg)Al 2(P0^) 2(0H) 2 Spinel, (Fe,Mg)Al20i)_ Identifying Features -occurs as euhedral crystals or aggregates, showing good cleavage, -usually colourless, more rarely pleochroic from colourless to pink, - c h i a s t o l i t e occurs very ra r e l y . - occurs as anhedral aggregates with poor cleavage. -low f i r s t order interference t i n t s . - colourless, which distinguishes i t from s c o r z a l i t e . - distinguished from quartz by moderate positive r e l i e f and a x i a l angle of +45°. - very high r e l i e f , low f i r s t order interference and prominent parting are d i s t i n c t i v e ; u n i a x i a l negative. - usually colourless, but may be zoned with a blue pleochroic core. - prismatic to tabular crystals are pleochroic from colourless to lavender. - minute crystals are a c i c u l a r , non-pleochroic, and similar to s i l l i m a n i t e except dumortierite i s length-fast. - occurs i n f i n e micaceous aggregates, very similar to muscovite can be posi-t i v e l y i d e n t i f i e d only by X-ray d i f f r a c t i o n . - blue i n hand specimen and pleochroic bright to dark blue i n t h i n section. - grains are anhedral with no cleavage. - mid-second order interference t i n t s that are commonly masked by the body colour. - spectrographs analysis by Church (1970) gives 12 per cent FeO and 2.5 per cent MgO. -occurs as isotr o p i c octahedra with extreme positive r e l i e f ; i s o t r o p i c . - colour ranges from dark green to l i g h t green. 54. andalusite and corundum. In the dust tuff unit (B^), the andalusite zone becomes an andalusite-pyrophyllite zone. Chemical compositions and identifying features of aluminous minerals are summarized in Table 4. Throughout the aluminous alteration zones, quartz and muscovite predominate and only loca l ly are andalusite or pyrophyllite a significant volume of the rock. Muscovite polytypes were investigated following the method of Carrol l (1970). Application of C a r r o l l ' s 1 c r i t e r i a suggests that lMd, IM and 2M polytypes are present. Nielsen (1969) ident i f ied predominantly lMd muscovite and some 2M muscovite within the zone of aluminous al terat ion. Where muscovite polytypes could be distinguished, i t is indicated throughout the following descriptions, Scorzalite Zone The scorzalite zone is 3,000 feet long by 1,200 feet wide and broadly outlines Cu-Ag mineralization. The zone is not centered on the ore zone but is offset towards the west, or hanging wall , side. Due to i t s blue colour, scorzalite was noted in d r i l l core logging, i f not correctly ident i f ied . D r i l l logs of a l l 62 Kennco holes were used to define the scorzalite zone. Because d r i l l logs could be used, the scorzalite zone extends from the area studied in deta i l into the area marked " insuff ic ient data" (Fig. 3). 1 Of six possible muscovite polytypes, the naturally occuring ones are lMd, IM, 2M and 3T where 1, 2 and 3 refer to the number of octahedral layers in the unit c e l l , M and T designate monoclinic or trigonal symmetry, and ' d ' denotes a disordered crystal structure. 55. Pyrite, muscovite and quartz usually contact scorzalite (photograph 15) and locally andalusite or chlorite may he present. Commonly, scorzalite is intimately associated with pyrite and other sulphides. This close association suggests a genetic relationship between scorzalite and sulphide minerals. However, scorzalite and pyrite are not closely associated on the western, stratigraphically highest, side of the scorzalite zone as in d r i l l hole 22 where scorzalite occurs with IM muscovite, corundum, spinel, andalusite, r u t i l e and very minor pyrite. Augellite was found with scorzalite in two samples, D.D.H. 6-300 feet and D.D.H. 22-450 feet. Augellite, in comparison to scorzalite, lacks iron and magnesium. This difference is consistent with the decrease in pyrite associated with scorzalite. Apatite occurs sporadically in the scorzalite zone but i t i s not directly associated with scorzalite. The underlying basal pyroclastic unit (B^), and dykes cutting the volcanic rocks, contain accessory apatite, but no scorzalite, Andalusite and Andalusite-Pyrophyllite Zones Andalusite was f i r s t identified at Sam Goosly by Nielsen (1969). It develops sporadically and is identifiable only in thin section. Thus the boundary of the zone cannot be located as precisely as that of scorzalite. The andalusite zone is over 4,500 feet long by a maximum surface width of 1,200 feet, and is elongate parallel to the strike of the pyroclastic strata. The zone encloses most of the Cu-Ag mineralization but is offset to the west so that i t is not concentric with mineralization. Across the facies boundary 56. 0 1 mm. I 1 Photograph 1 6 Band of a n d a l u s i t e , p y r i t e and quartz ( c l e a r ) , i n a quartz-muscovite rock. 57. into the dust tuff unit (B^), pyrophyllite develops and the zone becomes an andalusite-pyrophyllite zone. The andalusite zone develops most prominently in brecciated dacite (Bg) and immediately overlying volcanic breccias (B^), In Section 12,400N (Fig. 5)» every thin section of brecciated dacite contains andalusite but none of the underlying basal pyroclastics (B^) contains i t . The boundary of the andalusite zone corresponds very closely to the stratigraphic boundary between B^ and B^. Alteration of the brecciated dacite, consisting of a submicroscopic mixture of quartz and lMd muscovite, begins along fractures and progresses into fragments. In very weakly brecciated rocks, some fractures only 0,5 mm, wide are cored by andalusite. With increasing intensity of alteration, fractures increase in width to several millimetres and form a dense network. In this network, andalusite is disseminated in the breccia matrix, and i t has coarsened to 0,3 mm,, quartz to an average of 0,2 mm. and 2M muscovite to 0,02 mm. Rocks consist either of dominant muscovite with minor quartz and rare andalusite, or dominant quartz plus andalusite with minor muscovite (photographs 16 and 17). The most andalusite-rich domains consist of about 75 per cent quartz, 15 per cent andalusite, 5 per cent 2M muscovite, and 5 per cent sulphides. These modal relationships suggest muscovite has been converted to andalusite plus quartz, with a loss of potassium. Andalusite and sulphides are spatially related in the matrix of the dacite breccia. A polished section (D.D.H. 9-120 feet) contains clusters of pyrite, chalcopyrite and tetrahedrite with 1 mm. 0 r Photograph 17 Prismatic andalusite with quartz (clear). 5 9 . andalusite and quartz around the margin. In other rocks, sulphides are i n t e r s t i t i a l to, or included within, andalusite (photograph 1 8 ) , These textures suggest that p y r i t e , chalcopyrite, t e t r a h e d r i t e , quartz and andalusite formed contemporaneously. This conclusion accords with the observations of Ney et a l (1972) who noted s i l i c i f i c a t i o n was c l o s e l y r e l a t e d to mineralization, Andalusite becomes sporadic i n volcanic breccias (B^) and e p i c l a s t i c s (B^). I t occurs i n the matrix of volcanic breccias but i n e p i c l a s t i c rocks. Where the matrix may be very s i l i c e o u s , andalusite forms within muscovite-bearing c l a s t s , A conglomerate from an e p i c l a s t i c lens i n d r i l l hole 22 contains 2 cm, d a c i t i c c l a s t s In a very fine-grained s i l i c e o u s matrix. A 1-2 mm, t h i c k outer rim of the c l a s t s has concentrations of andalusite (now pseudomorphed by c h l o r i t e ) and p y r i t e . S t r a t i g r a p h i c a l l y higher, andalusite i s not c l o s e l y associated with sulphides and corundum becomes more abundant than andalusite. Andalusite occurs as c l u s t e r s of rosettes (up to 0 . 5 mm. i n diameter) producing a s o l i d mass or pod of andalusite several millimetres i n s i z e (photograph 1 9 ) . The rosettes are centred by a few grains ( 0 , 0 2 mm.) of r u t i l e , with andalusite r a d i a t i n g outward. This texture suggests that r u t i l e has acted as a point f o r nucleation of andalusite. Highly aluminous zones occur l o c a l l y that consist of 80 per cent f i n e - g r a i n e d 2M muscovite, 10 per cent andalusite, 2 per cent disseminated r u t i l e , a va r i a b l e amount of tourmaline, but no quartz. One such rock from D.D.H. 2 2 - 2 7 6 f e e t i s banded, with a l t e r n a t i n g 1 cm. wide tourmaline-rich and a n d a l u s i t e - r i c h bands, which may have formed at the same time. 0 1 mm. | 1 Photograph 1 9 Andalusite rosettes, centred by r u t i l e , 61. In dust tuff unit (B,-) andalusite, pyrophyllite and chlorite form the typical assemblage of the andalusite - pyrophyllite zone. Andalusite is not spat ial ly associated with sulphides or brecciation, but develops in two zones flanking Cu-Ag mineralization (Pig. 7). Andalusite usually occurs as 0.1 to 0.4 mm. disseminated grains, or as aggregates up to 5 mm. in s ize . The chiastolite variety occurs l o c a l l y (photograph 2 0 ) , Andalusite l i e s in a very fine-grained matrix, identif ied by X-ray d i f f rac t ion as muscovite (either IM or 2M polytypes), pyrophyllite, chlorite and quartz. Pyrophyllite is not present in a l l rocks and i n others, pyrophyllite occurs without andalusite. Although secondary quartz i s associated with andalusite, quartz never becomes a major constituent of the rock as i t does in the brecciated dacite. In the lower andalusite -pyrophyllite zone, narrow (0,02 mm.) veinlets of andalusite are common. These are para l le l to and intimately associated with th in , wispy chlorite veinlets (photograph 2 1 ) . Corundum Zone Scattered occurrences of corundum l i e within a zone that i s 1,300 feet long by 500 feet wide. The zone is completely enclosed by the andalusite and scorzalite zones. It l i e s stratigraphically above Cu-Ag mineralization and shows the same westerly displacement as described for the preceding alteration zones. The corundum zone may have extended as far north as 13,400N,>as possible corun-dum pseudomorphs occur in d r i l l hole 29. Although corundum is sparse, several different associations have been recognized. 0 y 1 mm. H Photograph 21 P a r a l l e l veinlets of andalusite; t h i n section from hand specimen 1, photograph 25. 63. (1) In a sample from D.D.H. 12-683 feet , corundum forms inclusions in andalusite (photograph 22). Margins of large (0.3 mm.) prismatic andalusite grains are altered, to muscovite but centres are crowded with minute corundum grains. (2) Corundum and muscovite may occur as 0.5 to 3 mm, nodules. Corundum is separated from the surrounding quartz-bearing matrix by a sheath of fine-grained muscovite. Spinel may be associated with corundum (photograph 23). (3) At D.D.H. 22-452 feet , a highly aluminous rock consists of 65 per cent IM muscovite, 15 per cent scorzali te , 10 per cent augel l i te , 3 per cent spinel , 2 per cent r u t i l e and 5 VeT cent randomly distributed corundum, but no quartz. Rare andalusite grains are ragged and embayed by surrounding corundum and muscovite. These three types of corundum occurrences indicate a close spat ia l , and possibly genetic relationship, between andalusite and corundum (see p. *3I). (4) Corundum, with pyrite and tourmaline, , : f i l ls fractures less than 1 mm. wide. At D.D.H.'.'30-314 feet , for example, a 0.4mm. wide quartz-pyrite veinlet abruptly becomes a corundum-pyrite veinlet . Although quartz and corundum are not in contact, they are part of the same vein system. (5) At D.D.H. 22-706 feet , quartz and corundum form a 5 mm. thick layer cutting a rock of quartz, muscovite and dumortierite. Muscovite pseudomorphs of andalusite are also present. The layer has a narrow muscovite-rich border and contains minor dumortierite and rare andalusite in addition to quartz and corundum (photograph 24). Andalusite grains are ragged and replaced by corundum. 64. Photograph 24 Corundum (high r e l i e f ) and quartz ( c l e a r ) . Andalusite replaced by corundum at centre of photo. 65. Other Minerals Spinel i s associated with corundum and, less commonly, with scorzalite or andalusite. In one specimen scorzalite mantles spinel indicating that, at least l o c a l l y , spinel was present before the formation of scorzali te . Dumortierite in the brecciated dacite (Bg) occurs as rare disseminated grains, or as a cluster of grains bordering pyri te . Dumortierite i s closely associated with andalusite and in some rocks replaces andalusite. In D.D.H. 22, about 200 feet above Cu-Ag mineralization, fibrous dumortierite i s developed throughout the matrix of a volcanic breccia, giving the matrix a pale lavender colour over a distance of 30 feet . Tourmaline, another boron mineral, has a very widespread distr ibution as an accessory mineral, occurring in Lower Cretaceous and Tertiary volcanic rocks at Sam Goosly. However, textural evidence, such as the banded andalusite - tourmaline rock (p. 59 ) suggests at least some tourmaline is related to the formation of aluminous minerals. Locally within the andalusite zone, volcanic breccias consist almost entirely of schorlite tourmaline. One such zone is shown on Section 11,500 N (Fig. 6), where intense tourmalinization extends over 10 to 15 feet in both d r i l l holes 12 and 48. The trend of this tourmalinized zone is similar to that of other alteration zones, suggesting a genetic relationship. Schorli te , the i ron-r ich tourmaline dominates in the mineralized zone, and dravite, the magnesium-rich variety, occurs.only l o c a l l y . In D.D.H. 12-600 to 800 feet , large (0.5 mm.) scattered dravite p o i k i ' l i t i c a l l y encloses quartz grains, i s rimmed by schorlite,and 66. i s in contact with andalusite. ALTERATION ASSOCIATED WITH MINERALIZATION IN UNIT In the dust tuff unit (B^), Cu-Ag mineralization occurs as open-space f i l l i n g in a breccia zone. Strongly fractured dust tuffs are altered to a pale tan or buff rock consisting of IM and 2M muscovite and quartz for at least 1,4000 feet between D.D.H. 41 and D.D.H. 3 9 , 5 6 , 60 and 61. These rocks are 250 feet thick and are flanked, above and below, by gray andalusite - pyrophyllite rocks. Brecciation decreases in intensity away from the quartz -sulphide breccia of the ore zone into pyrite - chlorite fractures. These fractures crosscut chlorite - andalusite veinlets (p. 6 l ) and indicate at least two generations of chlorite (photograph 25 ) . Where andalusite - pyrophyllite rocks are cut by chlorite - pyrite fractures, pale tan or buff alteration envelopes, from a few millimetres to 20 cm. wide, consist mainly of muscovite and quartz. Commonly, kaolinite also develops in the envelope but pyrophyllite i s rare and andalusite i s absent. This distr ibution of minerals implies that kaolinite replaces andalusite and pyrophyllite in the alteration envelope. The small scale alteration envelopes about single fractures are analagous to the quartz - sulphide breccia zone and i t s large scale alteration envelope of muscovite and quartz. Therefore, the two andalusite - pyrophyllite zones in the south (Fig. 7) may have been one large andalusite -pyrophyllite zone which has been dissected by quartz - muscovite alteration associated with mineralization. Thus, sulphide deposition in the dust tuff unit i s later than andalusite al terat ion, and 67. contrasts with the ore zone farther north where a single andalusite zone i s contemporaneous with sulphide deposition. REGIONAL METAMORPHISM Outside the aluminous alteration zones, rocks of the pyroclastic division consist of muscovite, quartz, chlorite, albite and calcite with mineral proportions depending on host rock composition. A corresponding assemblage i s developed sporadically within the zone of aluminous alteration. The following is a systematic description of the units. In the basal pyroclastic unit (B^) chlorite, pyrite, and quartz commonly replace pyroxene phenocrysts. Less abundant feldspar phenocrysts are dusty brown and pseudomorphed by An^ ^  plagioclase. A fine-grained groundmass consists of quartz, muscovite, albite and calcite. An estimated average mode is 20 per cent chlorite, 25 per cent albite, 20 per cent quartz, 27 per cent muscovite, 5 per cent calcite and 3 per cent pyrite. In the brecciated dacite (B^) andalusite is replaced by kaolinite, muscovite and chlorite. Most commonly, andalusite grains are replaced by kaolinite with an outer rim of muscovite. Andalusite closely associated with sulphides i s replaced by chlorite, such that a completely replaced grain may have a chlorite core with a kaolinite or muscovite margin. Scorzalite intergrown with andalusite is not as susceptible to alteration and only rarely alters to chlorite. A more prominent feature i s chlorite halos, or alteration rims about sulphide grains. Chlorite and carbonate (siderite?) microveinlets occur locally. 68. Photograph 25 m e n 1 mm. 0 Photograph 2 6 C h l o r i t e (green) pseudomorphs of andalusite. 69. Ghlorite-albite-carbonate alteration i s well developed in volcanic breccias (B )^ and epiclastics (B^). Muscovite and quartz with variable amounts of chlorite comprise the matrix of volcanic breccias. Locally, chlorite may account for 60 per cent of the matrix as in the 'muddy' matrix of possible lahar units. Chlorite mantles on sulphides are more prominent than in unit Bg. Here and there radiating bursts of tourmaline (schorlite) are intergrown with chlorite. Andalusite is variably replaced by kaolinite, muscovite and chlorite (photograph 26), and corundum alters readily to a brown micaceous aggregate. In addition to the ubiquitous muscovite-quartz assemblage, breccia fragments may also contain albite and calcite. Albite pseudomorphs rare plagioclase microlites, or more commonly, forms a patchwork of cloudy, untwinned 0,05 mm, grains. Chlorite alteration i s not as prominent in epiclastic horizons where carbonate alteration develops more strongly. Composition of the carbonate depends on i t s local environment of formation, Ankerite, or rarely siderite, i s closely associated with pyrite whereas calcite develops within clasts, away from pyrite. In some rocks, pyrite mantled by ankerite i s ragged but adjacent pyrite, without a carbonate mantle, i s euhedral. The inference i s that pyrite has supplied iron for ankerite. Muscovite in epiclastic horizons i s predominantly 2M polytype. A typical dust tuff from unit B^, outside the andalusite pyrophyllite zone consists of 25 per cent crystal and l i t h i c fragments in a fine-grained mesh of chlorite, muscovite and quartz. Crystal fragments are mainly quartz and clear, untwinned albite. Lithic 70. fragments are extremely fine-grained and consist predominantly of muscovite and quartz. Patches and stringers of calcite occur sporadically. Microveinlets and a few patches of epidote were found in one sample. In many rocks within the andalusite-pyrophyllite zone, andalusite is replaced by oval 'spots' (0,1 to 0.3 mm.) of kaolinite. In some rocks evidence is contradictory as andalusite veinlets cut through kaolinite 'spots'. Rocks of the welded ash tuff unit (Bg) have been altered to a quartz-muscovite-albite-calcite assemblage. Ash-size fragments are converted to a very fine-grained mixture of 2M muscovite and quartz, and l i e in a siliceous matrix. Feldspar crystal fragments, 0.5 to 2 mm. in size, are replaced by twinned low-temperature albite (An Q_g). Calcite occurs as patches, generally within l i t h i c or crystal fragments rather than the matrix. An average specimen contains 50 per cent quartz, 35 per cent 2M muscovite, 10 per cent albite and 5 per cent calcite. Tourmaline i s extremely rare and occurs as radial aggregates. CONTACT METAMORPHISM D.D.H, 19 shows contact effects of the quartz monzonite stock. The contact was not cut in this hole, but projection of surface geology indicates the d r i l l collar should be within 100 feet of the intrusion. Potash feldspar alteration i s very strong within the f i r s t 10 feet of core, and is associated with chlorite and muscovite. Over the next 150 feet sporadic pyrite veins, 2 or 3 mm, wide, have strongly bleached envelopes (2 cm. wide) consisting 71. of relatively coarse-grained (up to 1 mm, in size) flakes of muscovite and quartz. Outside vein envelopes the rock contains chlorite, muscovite, alhite and quartz, a typical assemblage of the regional metamorphism. Vein envelopes and the small zone of potash feldspar may be related to the quartz monzonite. This type of alteration is typical of 'porphyry' environments and may be related to the weak copper-molybdenum mineralization within the quartz monzonite. D.D.H. 9, 12, 2 4 , 4 5 and 4 8 show contact effects of the gabbro-monzonite complex. In marginal phases of the intrusion, plagioclase phenocrysts (An^) up to one cm. long are broken and ragged. Rare 2 mm. pyroxene phenocrysts are altered to chlorite and biotite. Plagioclase and pyroxene phenocrysts l i e in a fine-grained (0,1 mm.) matrix of plagioclase, secondary biotite, chlorite, quartz, magnetite and apatite. Scapolite and calcite occur locally. In d r i l l holes 9 and 4 5 , an assimilation zone up to 10 feet thick consists of unit B^ pyroclastic rocks with disseminated ragged plagioclase laths similar to the intrusion. Within this zone, micrographic intergrowths of quartz plagioclase and potash feldspar indicate partial fusion. The main effect of the intrusion on the si l i c a t e mineralogy i s formation of a narrow discontinuous zone of biotite hornfels. The biotite zone i s about 20 feet wide in d r i l l hole 9 and about 30 feet in d r i l l hole 12. Biotite i s disseminated in a matrix of granular quartz, muscovite, potash feldspar, chlorite and magnetite. Where biotite i s absent, the principal effect on si l i c a t e mineralogy has been recrystallization to a granoblastic texture. Pyrite porphyroblasts become prominent in d r i l l holes 12 and 48 w i t h i n 175 f e e t of the c o n t a c t , and i n d r i l l ho le 33 w i t h i n 80 f e e t . In d r i l l ho le 4 8 , p y r r h o t i t e becomes a major s u l p h i d e c o n s t i t u e n t w i t h i n 200 f e e t of the contac t (see p. 4 8 ) , 73. DISCUSSION SEQUENCE OF ALTERATION EVENTS Alteration, regional metamorphism and contact metamorphism developed in a complex sequence summarized in Fig. 9. Aluminous alteration i s probably the earliest alteration event. Textures such as the replacement of andalusite by fine-grained kaolinite, muscovite and chlorite (p. 6?) indicate aluminous alteration predates regional metamorphism. Aluminous alteration also predates quartz - muscovite alteration associated with mineralization in unit (p. 66). Trachyandesite dykes crosscut quartz - muscovite alteration and hence, this alteration pre-dates contact metamorphism. The age relationship between quartz - muscovite alteration and regional metamorphism is uncertain and this is indicated in Fig. 9. If Cu-Ag mineralization was a single event, then quartz - muscovite alteration associated with mineralization in unit B^ pre-dates regional metamorphism. Adjacent to the gabbro - monzonite intrusion, a biotite hornfels, caused by contact metamorphism post-dates aluminous alteration. Contact metamorphism is probably later than regional metamorphism. Biotite in the hornfels zone is not chloritized, and plagioclase and augite in the intrusive are unaltered. GRAPHICAL REPRESENTATION OF ALTERATION ASSEMBLAGES Aluminous Alteration The three-component system Al 0„-SiO»-H_0 portrays equilibria Event Aluminous alteration and Cu-Ag mineralization in the main ore zone Vein-like mineralization in B- and associated quartz-muscovite alteration Regional metamorphism Intrusion of quartz monzonite and associated contact metamorphism Intrusion of gabbro-monzonite, associated dykes and contact metamorphism 75 among the aluminous alteration minerals andalusite, corundum and pyrophyllite and quartz. Additional phases can be accounted for by the presence of additional components, such as KgO for muscovite, BgO^ for dumortierite, ^2^5 ^ o r s c o r z a l i t e , S for pyri te , TiCv, for r u t i l e , MgO and FeO for spinel and tourmaline. At Sam Goosly, assemblages of three s o l i d phases in the system AlgO^-SiOg-HgO are uncommon. The most strongly altered rock, the brecciated dacite, i s characterized by the assemblage andalusite - quartz (Fig. 10-a). Kaolinite replaces andalusite and is clearly in disequilibrium. Corundum generally occurs sporadically in a quartz-free microenvironment as the assemblage corundum - andalusite or as corundum alone (Fig. 10-b) The only rock observed to contain a three-phase assemblage, corundum -andalusite - quartz is considered an unstable assemblage. In the andalusite - pyrophyllite zone the assemblage andalusite - pyrophyllite-quartz is common and may result from the system being closed, so that HgO is not a mobile component, or because the rock i s buffered on the breakdown curve of pyrophyllite , A l 2 S i ^ 0 1 ( ) ( O H ) 2 A l 2Si0 5 + 3 S i 0 2 + H 2 0 (l ) pyrophyllite andalusite quartz water In a hydrothermal system, water i s a mobile component, and the la t ter alternative is favored. Rocks in the andalusite - pyrophyllite zone are interpreted as transit ional between a pyrophyllite -quartz assemblage and an andalusite - quartz assemblage (Fig. 10-c). Regional Metamorphism Regional metamorphism results in muscovite - quartz - chlorite a lbi te + calcite + kaolinite + epidote. Within the aluminous alteration Figure .10 Graphical Representation of Aluminous A l t e r a t i o n 77. zone, the typical assemblage is quartz - muscovite - chlorite -kaolinite - which is shown on an AlgO^-SiOg-HgO diagram and on an i A KF projection in Fig. 11-a. The formation of kaolinite i s expressed hy, Al 2 S i 0 5 + Si0 2 + 2H20 ±==== AlgSigO^OH)^ (2) andalusite quartz water kaolinite which indicates conditions of regional metamorphism were below the st a b i l i t y of pyrophyllite. Rocks outside the aluminous alteration zone do not contain kaolinite. The typical assemblage is muscovite -quartz - chlorite - albite - calcite but no projection represents this assemblage suitably. The very rare occurrence of epidote in this assemblage can be shown in an ACF projection (Fig. 11-b). Contact Metamorphism Biotite within the contact hornfels zone adjacent to the monzonite intrusion forms with chlorite and muscovite. A possible reaction i s , 3KAl 3Si 30 1 ( )(OH) 2 + 5(Mg,Fe) 5Al 2Si 3O 1 0(OH)g muscovite chlorite 3K(Mg,Fe) 3AlSi 30 1 ( )(OH) 2 + MMg fFe )y^SI 20 1 0(OH )g + 7 SiCv, + 4^0 (3) biotite Al-rich chlorite quartz water Winkler (1967, p.99) suggested this reaction accounts for the f i r s t appearance of biotite in regional metamorphism. However, in the absence of andalusite and cordierite within the contact hornfels zone, a similar reaction may account for the formation of biotite at Sam Goosly. The muscovite - K-feldspar - quartz and biotite -FIGURE 1 1 Graphical Representation of Regional Metamorphism x Chlorite 79. FIGURE 12 Graphical Representation of Assemblages in the Hornfels Zone Muscovite K-feldspar + Quartz Chlorite Biotite F muscovite-chlorite-quartz may be represented g r a p h i c a l l y by the A KF p r o j e c t i o n ( F i g . 12). According to Winkler (1969) both these assemblages occur i n the a l b i t e - e p i d o t e hornfels f a c i e s . However the assemblage muscovite-biotite-K-feldspar-quartz i s stable u n t i l the K - f e l d s p a r - c o r d i e r i t e hornfels f a c i e s . INTERPRETATION OF ALUMINOUS ALTERATION Pressure-Temperature Estimates from the System AlgO^-SiO^-H^O Considerable experimental work has been performed i n the system Al^O^-SiOg-HgO. Some of the c r i t i c a l reactions have been examined up to nine times with a range of P-T estimates. A portion of the AlgO^-SiOg-HgO system i s shown i n Figure 13 with a number of r e a c t i o n curves. The d i s c o n t i n u i t y i n the diaspore-corundum curve a r i s e s from i t s i n t e r s e c t i o n with the water-steam curve. The i n t e r s e c t i o n of the breakdown curves f o r p y r o p h y l l i t e and p y r o p h y l l i t e plus diaspore, with the kyanite-andalusite boundary produces two degenerate invariant points, IP^ and IPg* ^ e only experimental determination of the breakdown of k a o l i n i t e to diaspore plus p y r o p h y l l i t e (Aramaki and Roy, I963) appears to be at too high temperature (390°C at 4 kb) and has not been used. The l o c a t i o n of t h i s curve i s based only on the c a l c u l a t e d p o s i t i o n of the "AlgSiO^ absent" invariant point of Wall and Essene (1972). The p o s i t i o n of the "quartz absent" inva r i a n t point i s also a r b i t r a r y . Other reactions are added to complete the consideration of the two non-degenerate invariant points. The p o s i t i o n of other inv a r i a n t points i n the system i s unknown. 81. - 6.0 4.0 - 3.0 FIGURE 13 System AlgO -SiOg-Hg© [Ky absent ~] Reactions I Haas (1972), Fyfe and Hollander (1964). II Richardson, Bell and Gilbert (1969). j ^ H a a s and Holdaway (1973). Matsushima et a l (1967). VII Velde and Kornprobst (1969) 1.0 / py- pyrophyllite a- andalusite ky- kyanite q- quartz k- kaolinite d- diaspore c- corundum w- water 450°G I 82. Mineral assemblages in the system Al^O -SiOg-HgO at Sam Goosly give l i t t l e information on pressure conditions during alteration. The only constraint is the presence of andalusite rather than kyanite. Within the pyrophyllite s t a b i l i t y f i e l d this limits pressures to less than 3 kilobars. Within the brecciated dacite and volcanic breccias, the presence of andalusite, quartz plus assumed water and the absence of pyrophyllite gives a minimum temperature of about 350°C depending on pressure. The occurrence of corundum plus assumed water rather than diaspore, provides an independent minimum temperature estimate of 360°-400°C, The only constraint on maximum alteration temperatures is the andalusite-sillimanite boundary, which at pressures of 1-2 kilobars is at 750°-800°C (not shown in Fig. 13). Lower temperature conditions can be deduced for the pyrophyllite-bearing dust tuffs. At pressures within the andalusite s t a b i l i t y f i e l d , a quartz-pyrophyllite assemblage indicates temperatures between about 300°G and 380°C. Rocks that contain andalusite, pyrophyllite and quartz probably are buffered on the pyrophyllite breakdown curve (p.75). Since the diaspore-corundum equilibrium l i e s at a higher temperature than the pyrophyllite breakdown curve, i t can be predicted that corundum w i l l be associated with andalusite but not with pyrophyllite. This agrees with alteration assemblages at Sam Goosly; pyrophyllite and corundum are not associated. Diaspore should occur within the andalusite-pyrophyllite zone, but none has been identified. Hydrolysis Equilibria Evidence from thin sections (p.57) indicates that andalusite and quartz form at the expense of muscovite by the hydrolysis reaction, 2KAl 3Si 30 1 0(0H) 2 + 2H + , 3Al 2Si0 5 + 3Si0 2 + 3^0 + 2K + (4) muscovite andalusite quartz water This reaction suggests that andalusite w i l l form in areas open to the passage of an acidic f l u i d . This would account for the formation of andalusite within the matrix of volcanic breccias and the brecciated dacite, and not within the breccia fragments. Veins and stringers of andalusite would represent former solution channelways. The dust tuff must have been especially permeable as andalusite commonly occurs scattered throughout the rock, as well as in veinlets. Pyrophyllite may form by a hydrolysis reaction analagous to (4). 2KAl 3Si 30 1 0(OH) 2 + 6Si0 2 + 2H + 3Al 2Si^0 1 ( )(0H) 2 + 2K + ;; (5) muscovite quartz pyrophyllite A significant difference between the two reactions is that quartz is produced during the formation of andalusite, but i s consumed in the formation of pyrophyllite. Intense s i l i c i f i c a t i o n occurs with andalusite in the brecciated !dacite- but only minor amounts of quartz are present in pyrophyllite-bearing rocks. Hemley (1959) and Hemley and Jones (1964) have experimentally determined the conditions for hydrolysis of K-feldspar and muscovite (Fig. 14) according to the following reactions: 3KAlSi30g + 2H + ' , KAl 3Si 30 1 ( )(OH) 2 +. oSiOg + 2K + (6) K-feldspar muscovite quartz 2 KAl 3Si 30 1 0(OH) 2 + 2H + + 3^0 ^kl^x^^m)^ + 2K+ (?) muscovite water kaolinite 84. FIGURE lk Some Equilibria in the System K 20-Al 20 3-Si0 2-H 20 (from Hemley and Jones, 1964) I Quartz present - 5000 \ \ Pressure '= lkb. K-feldspar -\ Muscovite \ _ 400° Pyrophyllite \ -Kaolinite \ \ _ 300° 1 2 ^ ' 1 3 -log mT.+/mu+ 85. FIGURE 15 Some Equilibria in the System X 2O-Al 20 3-SiO 2-H 20 (from Shade, 1968) 1 1 - 700° | I 1 I 1 Quartz present 1 . 1 Pressure = 1 k b . Andalusite -600° 1 \. X-feldspar — 1 1 1 --500° Muscovite \ --400° — 0 1 1 2 1 1 3 i log *K+/n>H+ 86. Shade (l Q68) has expanded their investigations to higher temperatures, examining hydrolysis equilibria between K-feldspar, muscovite and AlgSiO^ (Fig. 1 4 ) . The reactions involved are ( 4 ) , (6) and, 2KAlSi30g + 2H+ " 7 AlgSiO^ + 5Si0 2 + HgO + 2K+ (8) K-feldspar andalusite quartz water These two sets of experimental data show good internal consistency and together give a more complete representation of hydrolysis equilibria in the system KgO-AlgO^-SiOg-HgO (Fig. 16). The aluminosilicate f i e l d has been divided into kaolinite, pyrophyllite and andalusite consistent with Figure IJ. In the andalusite-pyrophyllite zone the assemblage muscovite, andalusite and pyrophyllite implies that the system is buffered at a particular solution composition and temperature, i f equilibrium is maintained between the f l u i d and mineral phases (Fig. 16), The potassium molality of the f l u i d for a moderately acidic pH of 4 (neutral pH at 350°C is 5 . 4 ) is 0,005. However, in an open, hydrothermal system i t may be dangerous to assume equilibrium i s attained. Eugster (1970) has calculated the hydrolysis equilibria among muscovite, K-feldspar and aluminosilicate assemblages from experimental and thermochemical data. Following the suggestion of Helgeson (1967, p. 375-378), Eugster rejected Hemley's experimental data (Fig. 13) for reaction (6) in favour of "best estimates" based on thermochemical data. At high temperatures this "best estimate" deviated from Hemley's data by several orders of magnitude. Eugster combined the thermochemical data with Evans' (1965) experimental data on the thermal st a b i l i t y limit of muscovite plus quartz, to derive expressions for the equilibrium constant in terms of H + 87. 1 I i : 1 FIGURE 16 Equilibria in the System K^O-Al^-SiOg-HgO -700° \ (data from Hemley and Jones, 1964 -\ Shade, 1968 L Velde and fCornprobst, 1969 -\ Haas and Holdaway, 1973). --6oo> \ >v Quartz present -\ Pressure - 1Kb. --500° - \ \ K-feldspar \ Muscovite \ Andalusite \ \ • — -400° . -Dust tuff \ assemblage \w Pyrophyllite \ ^ -300® Kaolinite 0 1 2 3 1 1 1 1 log raK+/mH+ 88. FIGURE 17 - T Relationships for Muscovite, K-felspar and AlgSiO^ (after Eugster, 1970) 1 1 r — r -3 -2 - 1 . 0 89. and K + a c t i v i t i e s , for reactions (4)_ and (8). The results are presented, together with st a b i l i t y f i e l d s of kaolinite, pyrophyllite and andalusite (Fig. 17). The discrepancy between Eugster and Hemley + and Jones may be determined by finding the K molality at the muscovite-andalusite-pyrophyllite equilibria, as before. The acti v i t y coefficient of K + may be estimated from Helgeson (1969) and the resulting K + molality i s 0.06, This compares with a value of 0,005 deduced from Hemley and Jones' (1964) data (Fig. 16). Consideration of hydrolysis equilibria in the system KgO-Al^O^-SiOg-HgO provides a maximum temperature estimate of alteration. Because andalusite forms from muscovite and not from K-feldspar, the maximum temperature is that of the isobaric invariant point at which K-feldspar, muscovite and andalusite coexist. This maximum, at 1 kb, i s 600°C from Eugster's data (1970) or 625°C from Shade's data (1968). Correlation of Sulphide Temperatures and Sili c a t e Alteration Assemblages Exsolution of chalcopyrite and sphalerite has been investigated experimentally, Buerger (1934) found that chalcopyrite exsolved from sphalerite at 350°-400°C. The temperature of unmixing of sphalerite from chalcopyrite was determined by Borchert (193^) to be 550°C. This high temperature agrees with the empirical observations of Ramdohr (I969) who noted that "sphalerite stars [exsolved from chalcopyrite] are very much restricted to high temperature deposits". The occurrence of both of these exsolution textures in the main ore zone at Sam Goosly indicates very high temperatures and agrees with the temperature range inferred from s i l i c a t e alteration mineralogy (between 360°C 90. and 625°C). Based on Buerger's experimental result, the absence of sphalerite-chalcopyrite exsolution textures in the southern ore zone suggests temperatures less than 350°-400°C. The maximum temperature of andalusite-pyrophyllite alteration in nearby dust tuffs i s deduced to be about 380°C. Sulphide deposition i s later than aluminous alteration in the southern ore zone {.p. 66). Since temperatures estimated from sulphides and from s i l i c a t e assemblages are consistent, the time lapse between events may be short. Effect of on Aluminosilicate Stability Althaus (4966) has suggested that the temperature of the pyrophyllite-andalusite equilibrium i s depressed as much as 80°C in acidic solutions. His experiments were performed with HF, HG1, HoS0,, and H„B0„. Aluminosilicates containing fluorine (topaz) and chlorine (zunyite) developed as intermediates between the breakdown of pyrophyllite and the formation of andalusite. This may be relevant since zunyite and topaz occur as part of the aluminous mineral assemblage in some other deposits (see Appendix). Althaus* experiments with boric acid f a i l e d to produce the boron analogue, dumortierite. Althaus attributed the depression of the pyrophyllite breakdown to a lowering of the activity of water. Kerrick (1968) has calculated that the temperature depression for this reason to be very slight. For example the activity of water in a 4-N HgSO^ solution i s 0.918 at 60°C. Since the ionization of acids decreases with increasing temperature, the activity of water in a 4N H^SO^ solution w i l l be closer to unity at higher temperatures. Using 0.918 the effect on AG can be found from, 9 1 . & G = RT l n a to be -130 calories. The temperature depression can then be found from, 6 'cG = - A S & T + to be only 7°C. Kerrick suggested that the main effect of H in Althaus* experiments was that i t acted as a catalyst in the breakdown of pyrophyllite. This explanation appears plausible, as Althaus' temperatures for the pyrophyllite-andalusite equilibrium without acid are too high, but with acid they agree closely with Kerrick (I968), Hemley (196?) and Haas and Holdaway (1973). Formation of Corundum Three reactions may be considered in the formation of corundum, K A l 3 S i 3 O 1 0 ( O H ) 2 ^ r ^ KAISi Og + A l ^ + HgO (9) muscovite K-feldspar corundum water 2 AlgSiO^ + k S i 0 2 + 2K + + HgO ±=? 2KAlSi 30g + A l ^ + 2H + (id) andalusite quartz water K-feldspar corundum 6 Al 2SiO^ + 2K + + 3H20 t==? 2KAl 3Si 3O 1 0(OH) 2 + 3 ^ 1 ^ + 2H + ( l l ) andalusite water muscovite corundum Reactions (9) and(lO) require the association of corundum with K-feldspar, which is not observed. The last reaction i s consistent with the observed mineralogy and has been proposed by Rose (1957) to account for the formation of corundum and muscovite at the core of an andalusite grain. This texture described by Rose i s comparable, but not identical, to the inclusions of corundum within andalusite described earlier (p.63). If andalusite at Sam Goosly has formed by hydrolysis of muscovite, as in reaction (4) and that, at a later stage, the composition of the f l u i d phase changes toward a higher mK +/ nH + (perhaps by a decrease in acidity), then muscovite w i l l form at the expense of andalusite. If quartz is available, the 92. reaction w i l l be the reverse of reaction (4), 3Al 2Si0 5 + 3Si0 2 + 3H20 + 2K + ^  - 2KAl 3Si 30 1 ( )(0H) 2 + 2H + andalusite quartz water muscovite In a locally quartz-deficient environment, reaction ( l l ) operates: 6Al 2Si0 5 + 2K + + 3H20 *—7 2KAl 3Si 30 1 ( )(OH) 2 + ^lgO^ + 2 H + andalusite water muscovite corundum The interior of an andalusite grain would be a quartz-deficient micro-environment. Pods of corundum, sheathed by muscovite, occur in a number of samples and could represent the end product of this reaction. Veinlets of corundum may also form in this manner, by the alteration of andalusite veinlets. This alternative i s preferable to suggesting that corundum has been deposited from solution. Korzhinski (1964), Carmichael (1969) and others have emphasized the immobility of alumina. Anderson and Burnham (1967) have found 3+ that the solubility of A l v only becomes significant in basic solutions at high pressure and temperature. Alumina solubility i s depressed at the low pH conditions envisaged for alteration at Sam Goosly. Although quartz and corundum occur together (p.63) they can not stably coexist. Evans (1965) has calculated the free energy for reaction 12 to be -I36O calories at 2 kb and 680SC. AlgO^ + S i 0 2 AlgSiO^ (12) corundum quartz andalusite Hemley (1967) has suggested that the small free energy differences between quartz-corundum and Al^iO^, may "partially account for the common occurrence of small amounts of corundum in quartz-bearing andalusite-pyrophyllite associations". It is more li k e l y that d i f f i c u l t y of nucleation and a high activation energy are responsible for metastable quartz-corundum associations. Experiments on aluminosilicate 93. s t a b i l i t y , such as those of Aramaki and Roy (1963), commonly resulted i n metastable quartz and corundum instead of Al^SiO^ for these reasons. Hydrothermal a l t e r a t i o n processes may also produce non-equilibrium assemblages. Formation of Other Aluminous Minerals Unusual phosphate minerals, such as s c o r z a l i t e , l a z u l i t e and a u g e l l i t e , are t y p i c a l of aluminous a l t e r a t i o n assemblages (Geijer, 1963, Espenshade and Potter, i960). Although chemical analyses of c o n t e n t of altered rocks are rare, available ones (Espen-shade and Potter, i960) range from 0.06 per cent to 0.33 per cent. These values are very s i m i l a r to the average c o n ^ e n ^ °f u n ~ altered volcanic rocks, such as 0.17 per cent i n dacite (Table 2). Thus phosphorus does not occur i n abnormal amounts, but what i s unusual i s i t s occurrence as aluminum-bearing phosphates rather than the calcium phosphate, apatite. Geijer (1963) suggested that the absence of apatite i s due to the marked depletion i n calcium, t y p i c a l of aluminous a l t e r a t i o n . The chemical analysis of altered rocks from Sam Goosly (Table l ) shows an average c o n _ t e n t (0.09 per cent) but an unusually low GaO content of 1.03 per cent. At Sam Goosly apatite occurs outside the s c o r z a l i t e zone, but not within i t (p. 55). The irregular d i s t r i b u t i o n of s c o r z a l i t e , and i t s occurrence i n veinlets implies at least l o c a l transfer of phos-phorus. Possibly calcium and phosphate are taken into solution from apatite, but the phosphate i s subsequently precipitated where iron and aluminum are available. Reaction (13) would account f o r the association of s c o r z a l i t e with pyrite and quartz, though there 94. 3 ( M g , F e ) 5 A l 2 S i 3 0 1 0 ( O H ) 8 + 2 C a 5 ( P O ^ ) 3 ( O H ) + 56H+ + 12S"" c h l o r i t e a p a t i t e 3 ( F e , M g ) A l 2 ( P 0 ^ ) 2 ( 0 H ) 2 + 6FeS 2 + 9Si0 2 + 1 0 C a 2 + + 6Mg 2 + + 38H20 ( 13 ) s c o r z a l i t e p y r i t e q u a r t z i s n o t s p e c i f i c e v i d e n c e t h a t t h e y have f o r m e d f r o m c h l o r i t e . A r e a c t i o n s u p p o r t e d by good t e x t u r a l e v i d e n c e i s t h e f o r m a t i o n o f d u m o r t i e r i t e f r o m a n d a l u s i t e . These two m i n e r a l s a r e c h e m i c a l l y s i m i l a r and d u m o r t i e r i t e f o r m s by t h e a d d i t i o n o f b o r o n , 4 A l o S i 0 c + H oB0„ " — 7 Al QSi,BC\. n(OH) + S i C L + H o0 (14) 2 5 3 3 o 3 J-9 2 2 a n d a l u s i t e d u m o r t i e r i t e q u a r t z w a t e r L a c k i n g thermodynamic d a t a f o r d u m o r t i e r i t e , l i t t l e can be done w i t h t h i s r e a c t i o n . Magnesium-bearing a l u m i n o s i l i c a t e s , s u c h a s c o r d i e r i t e , c h l o r i t o i d o r s p i n e l a r e n o t r e p o r t e d i n o t h e r o c c u r r e n c e s ( s e e A p p e n d i x ) . The a s s o c i a t i o n o f s p i n e l w i t h corundum, a n d a l u s i t e a n d s c o r z a l i t e a t Sam G o o s l y i s anomalous. U n f o r t u n a t e l y , t h e r e i s n o " c l e a r t e x t u r a l e v i d e n c e t o i n d i c a t e t h e s p i n e l - f o r m i n g r e a c t i o n . C h l o r i t e i s r a r e l y p r e s e n t i n s p i n e l - b e a r i n g r o c k s , a n d t e x t u r e s s u g g e s t c h l o r i t e i s a l a t e m i n e r a l a n d p r o b a b l y has f o r m e d f r o m s p i n e l . Thus, s p i n e l has f o r m e d f r o m some p r e - e x i s t i n g m a f i c a l u m i n o s i l i c a t e , s u c h a s a p r i m a r y m a f i c m i n e r a l ( b i o t i t e ? ) , o r a n a l u m i n o u s a l t e r a t i o n m i n e r a l , s u c h a s c o r d i e r i t e , ( M g , F e ) 2 A l ^ S i ^ 0 ^ g , o r c h l o r i t o i d , ( F e , M g ) A l 2 S i 0 5 ( O H ) 2 . 95. CONCLUSIONS OTHER OCCURRENCES OF ALUMINOUS ALTERATION Some of the aluminous minerals can occur i n a v a r i e t y of ge o l o g i c environments. According t o a l i t e r a t u r e survey (see Appendix) a l l of the aluminous mineral assemblages occur i n a r e s t r i c t e d environment. This environment i s t y p i c a l of some Japanese deposits i n v o l c a n i c rocks ( F i g . 18). T y p i c a l l y the aluminous a l t e r a t i o n zone occurs w i t h i n s i l i c e o u s v o l c a n i c rocks ( r h y o l i t e t o d a c i t e ) as an i r r e g u l a r to l e n t i c u l a r body, conformable w i t h the v o l c a n i c s t r a t a . Commonly the rocks are t u f f s , which may be b r e c c i a t e d . The most a l t e r e d rocks are very r i c h i n quartz and a l u m i n o s i l i c a t e s . They are enveloped by quartz-muscovite rocks which grade outward i n t o u n a l t e r e d rock. In some de p o s i t s there i s a p e r i p h e r a l c h l o r i t e -r i c h zone. C h a r a c t e r i s t i c minerals of the aluminous assemblage i n c l u d e a n d a l u s i t e , corundum, diaspore, p y r o p h y l l i t e , muscovite, d u m o r t i e r i t e , k a o l i n i t e , q u a rtz, l a z u l i t e - s c o r z a l i t e , r u t i l e and p y r i t e . Many unusual minerals such as svanbergite, topaz and zuny i t e are common. In some d e p o s i t s , a l t e r a t i o n i s c l o s e l y a s s o c i a t e d w i t h h i g h - l e v e l i n t r u s i o n s , contemporaneous w i t h the v o l c a n i e s . The grade of metamorphism of a s s o c i a t e d rocks ranges from z e o l i t e f a c i e s t o amphibolite f a c i e s . The host rock i n high-grade metamorphic t e r r a i n s i s a quartz-muscovite s c h i s t , u s u a l l y deduced t o have been a s i l i c e o u s v o l c a n i c u n i t . Kyanite, r a t h e r than a n d a l u s i t e , commonly occurs i n such d e p o s i t s . Deposits t h a t are mined f o r t h e i r alumino-s i l i c a t e content do not n e c e s s a r i l y have any economic sulphide m i n e r a l i z a t i o n , B o l i d e n , Sweden, i s the only deposit known to have FIGURE 18 Typi c a l Japanese Aluminous Deposit (from Iwao, 1 9 7 0 ) Corundum-andalusite-p y r o p h y l l i t e rock Andalusite-diaspore-p y r o p h y l l i t e clay S e r i c i t e - k a o l i n -p y r o p h y l l i t e clay V S i l i c i f i e d rock containing andalusite A l t e r e d t u f f containing s e r i c i t e and p y r o p h y l l i t e C h l o r i t i z e d t u f f As above, with l e s s of the clay f r a c t i o n s A n t i c l i n e Dip and s t r i k e been mined for metals (Au, Ag, Cu, As) and for aluminosilicates. If sulphide mineralization is present, pyrite i s the dominant mineral. Chalcopyrite, silver-bearing sulpharsenides and gold are the most common economic minerals, while sphalerite and especially galena are less important. The genetic model proposed normally involves a high temperature, low pressure environment. Hot, acid solutions leach most cations except S i , A l , T i and K. These remain to produce assemblages of quartz, plus aluminosilicates, r u t i l e , and muscovite except in the most strongly altered rocks. Iron may remain fixed as pyrite, or may be leached as are magnesium, calcium and sodium. Magnesium (and iron?) may be concentrated in a peripheral zone as chlorite. The hot fluids responsible for these effects are attributed to nearby intrusions or to high-level volcanic processes (solfataric). Aluminous alteration at Sam Goosly is similar to that described in other areas. Associated sulphide mineralization i s comparable, though not identical. A major difference is that antimony, in tetrahedrite, i s prominent at Sam Goosly rather than arsenic. ALTERATION MODEL The altered volcanic rocks at Sam Goosly are very impoverished in Na^ O and CaO and enriched in alumina and s i l i c a (Table 1 and 2, p. 32-33), compared to Nockold's (195*0 average dacite or rhyodacite. IC,0 content is not significantly different from that of a typical dacite. The relationships among elements is best displayed by the norm, which contains 15 per cent corundum, shows a marked depletion in albite and anorthite and a large increase in quartz relative 98. to average dacite or rhyodacite. In the rock, alumina is partly incorporated in muscovite. Recalculating the norm with muscovite in place of K-feldspar s t i l l indicates 10 per cent excess alumina. This excess forms the suite of aluminous alteration minerals in the mode. The f i r s t step in the alteration sequence i s the conversion of an acidic volcanic rock to a quartz-muscovite rock, by a leaching of sodium and calcium. The general reaction i s , Plagioclase + K-feldspar + H Muscovite + Quartz + Na + Ca +(K ) (15) This reaction remains qualitative unless the ratio of orthoclase: albite: anorthite i s known. Because fresh rocks, with primary feldspars, are absent at Sam Goosly, this ratio can not be determined. The ratio may be determined for Nockold's average volcanic rocks and two examples are given below: Dacite: Or:Ab:An 1 :4 :3 (16) 3KAlSi 30 Q + 12 NaAlSI^Og + 9CaAl 2Si 20g + 22H + + 8 K + l l K A l 3 S i 3 0 1 0 ( 0 H ) 2 + 30Si0 2 + 12Na + + 9Ca 2 + Rhyolite: 0r:Ab:An 6:5:1 lSKAlSi^Og + 15NaAlSi30g + 3CaAl 2Si 20g + 2 6 H + *—7 13KAl 3Si 30 1 Q(0H) 2 + 66Si0 2 + 15Na + + 5 K + +3Ca 2 + The important feature to note from these reactions is that K + must be added in the alteration of a dacite, or more basic rock, but i s removed In the alteration of a rhyolite. For a range of compositions between dacite and rhyolite, a l l the feldspars may be converted to muscovite without appreciable change in the KgO content of the rock. In a l l rocks Na20 and CaO must be removed. If alteration has proceeded in this manner, then there must be a charge balance, 99. with respect to cations l o s t and gained, i n order to preserve electroneutrality. Compared with Nockold's average dacite, the volcanic rocks at Sam Goosly show a loss of 4.44 per cent CaO, 3.22 per cent Na^O and a gain of 1,16 per cent K^ O, 2.24 per cent HgO. Recalculating to ion i c percentages, and multiplying by the valences of the ions, 2+ + r e s u l t s i n 99.2 units of positive charge removed as Ca and Na , for every 100 units added as K + and H + (Table 5). CaO Na2C K 20 H 20 TABLE 5 Cation Charge Balance Sam Goosly Average Dacite Change 1.09% 5.53% -4.44% 0.76% 3.98% -3.22% 2.56% 1.40% +1.16% 2.80% 0.56% +2.24% Charge Balance 99.2 units removed 100 units added Sam Goosly CaO 1.09% 0.76% 2.56% 2. Na20 K 20 Average Rhyodacite Change Charge Balance H20 3. bcr/o 4.13% 3.01% 0.68% -3.37% 89.7 units removed -0.45%, +2.12% 100 units added Similar calculations for rhyodacite indicate 89.7 units of positive 2+ + + charge removed as Ca , Na and K f o r every 100 units added as H +. The calculations are highly dependent upon the HgO content of fresh and unaltered rock and such close agreement i s fortuitous. The calculations demonstrate that application of a hydrolysis reaction of the general form of reaction (15) to altered volcanics at Sam Goosly 100. is consistent with charge balance requirements. The second step in the alteration sequence is the appearance of pyrophyllite and andalusite by hydrolysis of muscovite, as indicated by reactions (4) and (5). Calculation on the Goosly analysis show that a complete leaching of cations would yield a residual rock with 32 volume":per cent andalusite and 68 volume per cent quartz, compared to the estimated mode of 75 per cent quartz, 15 per cent andalusite, 5 per cent muscovite and 5 Ver cent sulphides of the most strongly andalusite-altered rocks. Gresens (1971) has proposed a similar sequence of reactions to explain the formation of quartz-kyanite schists, bordered by muscovite schist within a metarhyolite. The close association of pyrite with andalusite suggests that iron was not leached with other cations, but was fixed as a sulphide. The total iron content of the altered rocks is close to that of an average dacite or rhyodacite and only differs by an increase in the ferrous:ferric ratio. The analysis shows that sulphur has been added during alteration and iron is generally combined with sulphur as pyrite. Assuming that iron was present in the original volcanic rocks as a s i l i c a t e then hydrolysis by sulphuric acid could produce pyrite and aluminosilicates, perhaps accounting for the close spatial association of andalusite and pyrite in the brecciated dacite. Significantly, andalusite and pyrophyllite in the dust tuff are commonly associated with chlorite, and not with iron sulphides. The aluminosilicates in the dust tuff must be the result of hydrolysis of muscovite. In the brecciated dacite, andalusite would be produced from both muscovite and chlorite (?) with subsequent release of iron to form sulphides. In summary, alteration involved acidic solutions which profoundly affected the original rock composition. Some elements, such as Na and Ca have been extensively leached and the residual rock i s enriched in quartz and aluminous minerals. Mineral assemblages indicate temperatures between a minimum of 300°C in the dust tuff to a maximum possible temperature of 6Z5°C in the brecciated dacite. This alteration could occur in the following environments; (1) Geothermal, caused by meteoric and possibly juvenile water circulating through the hot pyroclastic strata. ( 2 ) Chemical weathering, followed by metamorphism. Soon after deposition of the volcanic strata, s u r f i c i a l chemical weathering could leach soluble cations, leaving a residual of clay minerals (kaolinite and muscovite) and quartz. Subsequent metamorphism would be isochemical, but produced a higher temperature assemblage. (3) Hydrothermal fluids from the gabbro-monzonite complex or the quartz monzonite may have been responsible for alteration and mineralization. The pronounced stratigraphic control of both alteration and mineralization favours either of the f i r s t two alternatives. Because of this and for the following reasons the third alternative is considered very unlikely: (1) The shape of the alteration zones is not spatially related to either intrusion. For example they do not rim one or other of the intrusions. The north end of the alteration and mineralization l i e s more than 1 km. from the granite, whereas the southern end is more than 1 km. from the gabbro-monzonite. ( 2 ) Contact metamorphism related to the stocks differs from the 1024 aluminous alteration in the ore zone. Biotite hornfels is associated with the gabbro-monzonite and K-feldspar is associated with the quartz monzonite. (3) Dykes related to the gabbro-monzonite cut mineralization and aluminous alteration. Only deuteric alteration occurs within the dykes. (4) Comparison with other occurrences of aluminous alteration shows no correlation between alteration and intrusions but a good correlation between alteration and acidic volcanic rocks. A model of chemical weathering followed by metamorphism i s considered unlikely for the following reasons: (1) The geometry of the alteration zones is not similar to a weathered horizon. Alteration zones are concentric, cross stratigraphic boundaries and are not evidently related to a disconformity. Horizons produced by weathering would be asymmetric. (2) Textural evidence indicates that regional metamorphism is later than aluminous alteration (p .69) . (3) If concentration of s i l i c a and alumina results from chemical weathering, then such deposits should be associated with a variety of rock types, and not only with acidic volcanic rocks. Aluminous alteration may develop in a geothermal environment, that i s , a hydrothermal process genetically related to the volcanic rocks. Acidic tuffs or high-level lava domes, brecciated by steam explosion would be hot, permeable, possess a high surface area, and be open to meteoric water. Circulation of' large volumes of f l u i d through the rock would result in compositional changes in the rock as i t attempted to equilibrate with the f l u i d . This model would 103. account for the gross parallelism of the alteration zones with the volcanic strata. It i s tempting to interpret the brecciated dacite as an autobrecciated lava dome, consistent with this model. Present-day geothermal systems are associated with areas of recent volcanism. The solutions involved are acidic potassium and sodium chloride brines, with large amounts of other dissolved species. Sulphide mineralization (chalcopyrite, sphalerite, galena) may be present in minor amounts, as at Broadlands, New Zealand (Browne and E l l i s , 1970), to large amounts, as in the Red Sea geothermal area (Degens and Ross, 1969). The K + molality in a number of geothermal areas i s compared to that deduced for Sam Goosly in Table 6. Both estimates of the solution K + molality during alteration at Sam Goosly are within the range found in geothermal brines, but the agreement i s closer using the estimate based on Hemley5'and Jones (196k). In the Matsukawa geothermal area, Japan, Sumi (1969) described a pyrophyllite zone, with pyrophyllite, quartz, andalusite, diaspore and zunyite. The pyrophyllite zone i s irregular and i s currently overlapped by three other zones- montmorillonite, kaolinite and alunite. Maximum temperature currently recorded in the f i e l d i s 254°C, The brines are acidic (with pH as low as 2.5) and are characterized by a high content of sulphate and low content of chloride ions. This i s consistent with the formation of acidic minerals such as alunite, pyrite and kaolinite. Composition of the solution from d r i l l hole MR-1 of the Matsukawa f i e l d i s given in Table 7. The formation of aluminous minerals and Cu mineralization at Sam Goosly l i k e l y occured in a near-surface geothermal environment. The geothermal solutions were characterized by a low pH, a high 104. TABLE 6 (information from E l l i s , 19691 and Sumi, 19692) Potassium Molality in Various Geothermal Waters LOCATION K + MOLALITY Hole 44, Waixakei, N.Z.1 0.006 Hole 2, Broadlands, N.Z. 0.005 Hole 7, Otake, Japan 0.003 Hole 63, Hveragerdi, Iceland 0.0007 Hole I.I.D., No.l,Salton Sea, 1 California 0.6 Hole G.S.'2V Steamboat Springs, 1 Nevada O.oo2 2 Hole MR-1 Matsukawa, Japan 0.004 Sam Goosly (based on Eugster, 1970) 0.06 (based on Hemley and Jones, 1964) 0.005 TABLE 7 (from Sumi, 1969) Chemical Composition of Brine in Hole MR-1, Matsukawa Temperature = 254°C PH 4.9 HC03" 36.6 S V " 1779.9 H2S t r . C l " 12.4 F e 2 + 507.7 £l3 + 28.6 „, 2+ 8.7 Mg^  2+ 22.9 Ca Na + 263.5 K + 1^3.5 sio2 599.5 HB02 248.2 105. sulphate ion content, and temperatures greater than 300°G but less than 600° to 6%5°C. GEOLOGIC HISTORY Volcanic activity in late early Cretaceous resulted in the accumulation of some 2500 feet of mainly dacitic pyroclastic debris. This may have taken place at or near a strand-line, represented by the chert pebble conglomerates. A limited amount of reworking of the volcanic rocks produced interbeds of volcanic sandstone, conglomerate, and possibly, lahar. Meteoric water circulating through the hot volcanic pile, mixed with metalliferous primary water, and was heated above the boiling point. The resulting steam explosion fractured unit Bg, providing solution channelways through i t . Since unit Bg is the most pervasively altered and mineralized, i t may have been the major heat source, possibly a lava dome. Units Bg, Bj, and B^ were highly permeable, whereas the underlying unit, B^, and overlying unit, Bg, were relatively impermeable. Very hot acidic solutions circulated through the permeable horizons and reacted with the surrounding rock. These reactions resulted in the exchange of H + ions from the solution with cations, mainly + 2+ + 2 + Na , Ca and some K and Mg , from the rock. Iron from the rock combined with sulphur and metals in the solution to form pyrite and other metallic minerals. As the rock was depleted in cations, quartz, aluminosilicates, scorzalite and other aluminous minerals formed. Lower temperatures, and possibly a change in composition of the solution, could account for the lack of ore closely associated with aluminous alteration in unit B^. Ore solutions deposited 1 0 6 . sulphide minerals in open spaces with limited chemical interaction with the host rocks. 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APPENDIX Summary of Occurrences of Aluminous Alteration Location (Reference) Host Rock Age ^Associated Intrusion Metamor-phism Shape Zoning & Mineralogy Economic Minerals Genesis Japan ( l ) , (2), (3),(4) i i : < dacite, andesite, pyro-clastics late Cre-taceous to Eocene high level granite domes (2) no specific data, but low grade lenticular bedded, mushroom-shaped 1. corundum-diaspore 2. pyrophyllite-kaolinite 3. sericite Other minerals: andalusite, quartz, alunite, dumortierite, zunyite, hematite, r u t i l e (3). A l -silicates Leaching of cations leaves the rocks enriched in Al 0 and SiOg. Takes ^ place in near-surface, acid hot springs environ-ment, related to volcanism ( l ) , (3). ireen Tuff pormation (variety )f sub-narine volcanies) Miocene none as above and pipe-shaped Pyrophyllite with diaspore, kaolinite, sericite. copper, pyrite lacite, tndesite tuffs and lavas Pliocene to Recent none geothermal areas Pyrophyllite, quartz with andalusite, diaspore, zunyite, montmorillonite, kaolinite, alunite W none Location (Reference) Host RocW Age Associated Intrusion Metamor-phism Shape Zoning & Mineralogy Economic Minerals Genesis Puerto Rico (5) andesite, basalt Late Cre-Itaceous to early Tertiary granodiorite none ilongate 1. Alunite-quartz patches 2. Pyrophyllite within a 3. Clay-sericite belt 50k111 Other minerals: x 5&m. kaolinite, halloysit'e andalusite, topaz, zunyite, svanbergite, pyrite, barite. none Magmatic emanations from granodiorite removed CaO, MgO, FeO and added SiO , S and possibly K 2 0 . Boliden, Sweden (6) quartz porphyry, keratophyre| dacite Pre-bambrian none low gradefLenticularu. Sericite-andalusite put cross-l cut Istrati-graphy -quartz, with corundum, diaspore 2 . sericite-quartz 3 . chlorite-sericite quartz. Other minerals: r u t i l e , apatite, tourmaline massive pyrite-arsenopyrite with Au-Ag-j Gu-As Ore and alteration produced by hydrothermal process. No change in volume, [Al-silicates Al 0 , LO, Ti6J S i 0 o , ' 2 ' " " " 2 ' H 2 0 added to zone 1 . FeO, MgO removed from zone 1,;added to zone 3. Overall loss of Na 0 and CaO. Location (Reference Host Rockj Age [Associated Intrusion Metamor-phism Shape Zoning & Mineralogy Economic Minerals Genesis Cordillera ( 7 ) , ( 8 ) , ( 9 ) , ( 1 0 ) tuff, frhyolite, trachyte Triassic granite Green-schist bonform-ahle lenses |l .Andalusite-dumortierite with muscovite, quartz 2. Muscovite-quartz A l -silicates quartz-monzonite very low grade irregular ( 8 ) ( 9 ) . Quartz-, muscovite, pyrophyllite, diaspore, corundum, lazulite, r u t i l e , alunite etc. Formed by pneumatolytic and hydrothermal processes, related to granite intrusion. l a t i t e , quartz l a t i t d Tertiary quartz monzonite very low grade lenticular| 1. Quartz-sericite-conformable andalusite with (10) | kaolinite, diaspore, r u t i l e , carbonate. 2. Sericite-quartz Breccia zone with Pb, Ag High T, low P leaching of Na 0, CaO, MgO. Residual concentration of K20, S i 0 2 , A1 20 3 FeO removed unless fixed as pyrite. Russia (11),(12) dacite, ignim-b r i t e ( l l s p i l i t e , kerato-phyre(l2) Mesozoic and enozoic none range fronjl unmeta-morphosed to epidot a c t i n o l i t ^ facies enticular|, 1.Secondary ' quartz conformable ites' with corunduml with volcanic stra-tigraphy andalusite, diaspore dumortierite,zunyite pyrophyllite,topaz, rutilej'apatite, tourmaline, Sericite-quartz, with pyrophyllite kaolinite. [3. Sericite-Chlorite with quartz. ^.Chlorite, with quartz, carbonate, spidote, sericite. Zone 1 ha: [sulphur-arsenic-Volcanic environ-ment. Leaching by volcanic gases pyrite(ll)jproduces residual jZone 2 has pyrite. IZone 3 has concentration of alumina and s i l i c a in zone 1, and halogens. KgO, leached from zone jCu-Pb-Zn(l2) fixation of and Au-Cu-Sn (11). 1, is concentrated in zone 2. MgO and FeO are redeposited in zones 3 and 4. CaO is concentrated in zone 4. Na20 i s completely (removed. Location (Reference' Host Roci i Age Associated Intrusion Metamor-phism Shape Zoning & Mineralogy Economic Minerals Genesis Bulgaria (13) dacite Jpper Cre-taceous no information no infor-mation within a belt 10km x 1.5km. 1. "monoquartzites" 2. pyrite-sericite, with diaspore 3. quartz-sericite 4. chlorite-epidote albite Dumortierite i s also present, zone not given. no information Hydrothermal alteration Sweden (14) rhyolite, dacite Pre-cambrian none very low grade no informatio Mainly quartz-n sericite. Also Chlorite, andalusite, kyanite. Pyritic Cu-Zn ore occurs with chlorite and kyanite Chemical changes produced by volatile magmatic emanations operating at low pressures but high temperatures. AlgO^ and SiOg represent material present in the original rock. quartzite Pre-cambrian none high grade (host rock i s gneiss) lenses or irregular Quartz, kyanite, muscovite,lazulite, hematite, r u t i l e , pyrite, augellite. Pyrophyllite and svanbergite as late veins. India (15) quartz-muscovite schists (derived from acid tuffs) Archean none moderate to high grade bedded Kyanite, topaz, andalusite, dumortierite, tourmaline, muscovite, damourite (after corundum). A l -silicates Thermal activity during volcanism produced fluids which leached the tuffs and added boron and halogens. Location (Reference) Host Rock Age Associated Intrusion Metamor-phism Shape Zoning & Mineralogy Economic Minerals Genesis Appalaichan (16),(17) rhyolite, dacite Pre-cambrian or Paleo-zoic(?) none amphib-olite facies bedded, s t r a t i -graphic units Pyrophyllite-andalusite-quartz, Other minerals: muscovite, diaspore, lazulite, r u t i l e , topaz, kyanite. Al-sili c a t e Chemical weather-ing of volcanic flows and tuffs followed by metamorphism (16),(17). irregular lenticular Kyanite-quartz. Also muscovite, pyrophyllite, lazulite, topaz, pyrite, r u t i l e . Solfataric activity removed nearly a l l constituents except SIO ?, T i 0 2 , A1 20 3. (16) (1) Iwao (1968) (2) Shimada and Nagayama (1969) (3) Iwao (1970) (4) Sumi (1969) (5) Hildebrand (1961) (6) Nilsson (1968) (7) Kerr and Jenny (1935) (8) Kerr (1932) (9) Gross and Parwell (1968) (10) Butler (1913) (11) Romanova and Petrachenko (1970) (12) Smirnov (1970) (13) Radonova (1967) (14) Geijer (I963) (15) Dunn (1937) (16) Espenshade and Potter (i960) (17) Zen (1961) 


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