THE GEOLOGY, LITHOGEOCHEMISTRY AND PETROGENESIS OF INTRUSIONS ASSOCIATED WITH GOLD MINERALIZATION IN THE PORCUPINE GOLD CAMP, TIMMINS, CANADA
by PETER J. MACDONALD
Thesis presented as a partial requirement in the Master of Science (M.Sc.) in Geology
School of Graduate Studies Laurentian University Sudbury, Ontario
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Abstract Most gold deposits within the Porcupine Gold Camp of the Abitibi greenstone belt are spatially associated with porphyry intrusions. These intrusions, however, are present beyond the immediate gold-hosting environment, extending over 80 kilometers along the Porcupine-Destor deformation zone (PDDZ). While petrographically similar, the intermediate to felsic intrusions along the PDDZ represent at least four distinct geochemically defined magmatic suites that span the deformation history of the Porcupine gold camp. The Timmins porphyry intrusive suite (TIS) intrusions are related to magma generated Dl-related crustal thickening related to uplift and extension as a result of flat subduction-related underplating of mafic crust, and resultant delamination and partial melting ca. 2690 Ma during Dl deformation at depths <40 kilometers. These TIS magmas were emplaced near surface and represent subvolcanic intrusions to coeval eruptive equivalents such as the Krist Formation pyroclastic volcanic rocks. Two additional suites of lower crustal sourced magmas, the Carr Township porphyry intrusive suite (CIS) and the granodiorite intrusive suite (GIS) were generated from mafic source rocks 10-15 m.y. later. The CIS was generated by lower crustal melting at shallower depths than the TIS, whereas the GIS was generated at greater depths than the TIS indicating that, in the immediate vicinity of Timmins, D2-related magmatism and thrust stacking significantly thickened the crust to in excess of 40 kilometers. The Holmer intrusive suite (HIS) is a late- to post-tectonic suite formed via the partial melting and fractionation of magma sourced from slab-melt altered mantle at depths >40 kilometers. Gold mineralization has long been recognized to be spatially associated with intrusions proximal to the PDDZ. Although there is no genetic link between spatially related porphyries and mineralization, gold mineralization is associated with sulphidized, sericite ± carbonate altered TIS intrusions emplaced during Dl and to a lesser extent with the late- to post-tectonic HIS and GIS intrusions. The spatial association of gold with the TIS intrusions is related to the intrusions and gold utilizing the same emplacement conduits, presumably reactivated regional faults, as well as the formation of dilation zones surrounding the intrusions during deformation. Similar to gold mineralization, copper mineralization is spatially associated to the Porcupine intrusive suites but does not have a genetic association. iv
Acknowledgements
This thesis would not have been possible without the interaction and support of many people, organizations and companies. I would like to begin by thanking my thesis supervisor Dr. Stephen Piercey, whose endless amount of patience, support and guidance have been a motivating inspiration to me. I also would like to thank my thesis committee members, Drs. Lafrance, Thurston and Ayer, along with my external examiner, Dr. Beakhouse, whose thoughtful edits have improved this thesis. Acknowledgement is given to the Discover Abitibi Initiative for financial support and the Ontario Geological Survey for publishing preliminary results. Staff from the Ontario Geological Survey are thanked for geological discussions and sharing knowledge of the Timmins region, including Brian Atkinson of the Resident Geologist office and Lindsay Hall and crew. The many companies, and people therein, are acknowledged for access to properties, drill core and logistics, including: The Porcupine Joint Venture (Alastair Still, Keith Green, Peter Harvey, Erik Barr, Bill MacRae, Steve Harding and Michael Nerup), Falconbridge Limited (Damien Duff and Cliff David), Kinross Au Corporation (Ryburn Norman), Lakeshore Au Corporation (Henry Marsden and Jacques Samson) and Tom Exploration Inc. (Chris Dupont). Roger Bateman and Dave Rhys are acknowledged for insight into the structural geology of the area, and Etienne Dinel is thanked for sample collection of porphyry intrusions within the Hoyle Pond deposit. Finally, I would like to thank my family and friends. Geoff for mentoring me into geology, Ed for showing me the results of determination, Dad for the knowledge that anything is possible; and Mom for motivating and enabling me to do so much. Lastly, and most importantly, I want to thank Christine for her love and support, I am not sure where I would be without it. V
Table of Contents
Abstract iii Acknowledgements iv Table of Contents v List of Figures viii List of Tables x Foreword xi
Chapter 1: An Introduction to the Porphyry Intrusions of the Porcupine Gold Camp, Western Abitibi Subprovince, Ontario 1
1.1 Introduction 1 1.2 Geological Overview of the Porcupine Gold Camp 2 1.3 Previous Work 6 1.4 Objectives 9 1.5 Methodology 9 1.5.1 Geological Mapping and Sampling 9 1.5.2 Lithogeochemistry 10 1.6 Thesis Presentation 11 1.7 References 12
Chapter 2: The Lithogeochemistry and Petrogenesis of Intrusions Associated with Gold Mineralization in the Porcupine Gold Camp, Timmins, Canada 22
2.1 Abstract 22 2.2 Introduction 23 2.3 Regional Geological Setting 25 2.4 Geological Attributes 26 2.4.1 Geological Attributes of Porcupine Intrusive Suites 26 2.4.2 Geological Attributes of the Felsic Volcanic Suite 30 2.5 Lithogeochemistry 30 2.5.1 Previous Geochemical Studies 30 2.5.2 Sampling and Analytical Procedures 31 2.5.3 Alteration Geochemistry of the Porcupine Intrusive and Felsic Volcanic Suites ... 33 2.5.4 Lithogeochemistry of the Porcupine Intrusive and Felsic Volcanic Suites 34 2.5.4.1 Lithogeochemistry of the Timmins Porphyry Intrusive Suite (TIS) 34 2.5.4.2 Lithogeochemistry of the Carr Township Porphyry Intrusive Suite (CIS) 36 2.5.4.3 Lithogeochemistry of the Holmer Intrusive Suite (HIS) 37 2.5.4.4 Lithogeochemistry of the Granodiorite Intrusive Suite (GIS) 38 2.5.4.5 Lithogeochemistry of the Felsic Volcanic Suite (FVS) 39 2.6 Discussion 41 2.6.1 Petrogenesis of the Porcupine Intrusive Suites 41 VI
2.6.2 Petrogenesis of the Felsic Volcanic Suite (FVS) 44 2.6.3 Relationship of Voleanism to the Emplacement of the Porcupine Intrusive Suites 45 2.6.4 Geological Differences between Gold Mineralized and Barren Intrusions 45 2.6.5 The Relationship of the Porcupine Intrusive Suites to Gold Mineralization 47 2.6.6 The Relationship of the Porcupine Intrusive Suites to Copper Mineralization 50 2.7 Conclusions 51 2.8 References 53
Chapter 3: Summary and Direction of Future Research 94
3.1 Key Conclusions 94 3.2 Potential Direction for Future Research 96 3.3 References 98
Appendix A: Porphyry Intrusions of the Porcupine Gold Camp, Western Abitibi Subprovince, Ontario 100
A.l Abstract 100 A.2 Introduction 101 A.3 Previous Work 102 A.4 Regional Geology 103 A.5 Geology: Quartz Feldspar Porphyries 106 A.5.1 Timmins Porphyry Intrusive Suite - Main Camp 106 A.5.1.1 Field Relationships 107 A.5.1.2 Petrography 109 A.5.1.3 Alteration, Veining, and Mineralization 110 A.5.1.4 Deformation 113 A.5.1.5 Geochronology 114 A.5.2 Timmins Porphyry Intrusive Suite - Other 114 A.5.2.1 Field Relationships 115 A.5.2.2 Petrography 117 A.5.2.3 Alteration, Veining, and Mineralization 118 A.5.2.4 Deformation 119 A.5.2.5 Geochronology 120 A.5.3 Carr Township Intrusive Suite 120 A.5.3.1 Field Relationships 120 A.5.3.2 Petrology 121 A.5.3.3 Alteration, Veining, and Mineralization 121 A.5.3.4 Deformation 122 A.5.3.5 Geochronology 123 A.5.4 Southern Trend 123 A.5.4.1 Field Relationships 123 vii
A.5.4.2 Petrology 124 A.5.4.3 Alteration, Veining, and Mineralization 124 A.5.4.4 Deformation 125 A.5.4.5 Geochronology 126 A.5.5 Eastern Trend 126 A.5.5.1 Field Relationships 126 A.5.5.2 Petrology 127 A.5.5.3 Alteration, Veining, and Mineralization 128 A.5.5.4 Deformation 129 A.5.5.5 Geochronology 130 A.6 Geology: Krist Formation 130 A.6.1 Field Relationships and Petrology 131 A.6.2 Alteration, Veining, Mineralization, and Deformation 131 A.6.3 Geochronology 132 A.7 Comparison of Porphyry Trends 132 A.8 Comparison of the Krist Formation and Porphyry Intrusions 133 A.9 Summary 135 A. 10 References , 137
Appendix B: An Assessment of the Immobility of Elements in Petrogenetic Interpretations of the Porcupine Intrusive Suites 171
B.l Introduction 171 B.2 Geochemical Tests of Element Immobility 171 B.3 Discussion of Element Immobility 173 B.4 Summary of Element Immobility 174 B.5 References 174 viii
List of Figures Figure 1.1 Simplified geological map of the Archean Superior Province 19 Figure 1.2 Simplified regional geological map of the Porcupine gold camp, Abitibi Subprovince 20 Figure 1.3 Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt 21
Figure 2.1 Regional geological map displaying the location of differing Assemblages within the Abitibi greenstone belt in the vicinity of the Porcupine gold camp, Timmins, Canada 60 Figure 2.2 Surface geological map of the Porcupine gold camp showing the location of historically significant producing gold mines and the felsic volcanic suite in relation to some of the Porcupine intrusive suites 61 Figure 2.3 Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt 62 Figure 2.4 Photographs and photomicrographs showing features of the Porcupine intrusive suites and the felsic volcanic suite 63 Figure 2.5 Mobile element plots for the Porcupine intrusive suites and the felsic volcanic suite 65 Figure 2.6 Immobile element discrimination plots for the Porcupine intrusive suites and the felsic volcanic suite 67 Figure 2.7 Classification plots of adakite-like rocks for the Porcupine intrusive suites and the felsic volcanic suite 68 Figure 2.8 Primitive mantle- and chondrite-normalized plots for the Porcupine intrusive suites and the felsic volcanic suite 69 Figure 2.9 Discrimination plots for the Porcupine intrusive suites and the felsic volcanic suite 71 Figure 2.10 Chronology of volcanism, sedimentation, intrusive magmatism, deformation, metamorphism and mineralization within the Porcupine gold camp ... 72
Figure Al Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt 142 Figure A2 Simplified regional geological map displaying the location of differing Assemblages within the Abitibi greenstone belt in the vicinity of the Porcupine gold camp, Timmins, Canada 143 Figure A3 Simplified surface geological map showing the names and locations of some of the intrusions of the Timmins porphyry intrusive suite -main camp 144 Figure A4 Simplified surface geological map showing the names and locations of some of the intrusions of the Timmins porphyry intrusive suite - main camp 145 Figure A5 Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - main camp 146 Figure A6 Surface geological map of the Crown porphyry breccia, Shania Twain Centre 150 ix
Figure A7 Map showing location of the Hollinger-Mclntyre gold mineralization and sericite-calcium carbonate alteration relative to part of the Timmins porphyry intrusive suite - main camp 151 Figure A8 Simplified surface geological map showing the names and locations of some of the intrusions of the Timmins porphyry intrusive suite - other 152 Figure A9 Simplified surface geological map showing the names and locations of some of the intrusions of the Timmins porphyry intrusive suite -other 153 Figure A10 Simplified surface geological map showing the names and locations of some of the intrusions of the Timmins porphyry intrusive suite - other 154 Figure Al 1 Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - other 155 Figure A12 Simplified surface geological map showing the names and locations of intrusions of the Carr Township porphyry intrusive suite 157 Figure A13 Photographs and photomicrographs showing features of the Carr Township porphyry intrusive suite 158 Figure A14 Simplified surface geological map showing the names and locations of intrusions of the Holmer intrusive suite 159 Figure A15 Photographs and photomicrographs showing features of the Holmer intrusive suite 160 Figure A16 Simplified surface geological map showing the names and locations of some of the intrusions of the granodiorite intrusive suite 161 Figure A17 Simplified surface geological map showing the names and locations of some of the intrusions of the granodiorite intrusive suite 162 Figure A18 Photographs and photomicrographs showing features of the granodiorite intrusive suite 163 Figure A19 Simplified surface geological map of the felsic volcanic suite 164 Figure A20 Photographs and photomicrographs showing features of the felsic volcanic suite 165
Figure Bl Immobile element versus immobile element immobility test plots 175 Figure B2 Immobility test plots of the Al2C«3/Na20 alteration index versus major, trace and rare earth element abundances and ratios 176 Figure B3 Immobility test plots of the absolute mass change of Na20 versus trace and rare earth element abundances, ratios and mass change 178 X
List of Table
Table 2.1 Table of porphyry intrusions and felsic volcanic rocks included in this study 73 Table 2.2 Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites 74 Table 2.3 Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite 78
Table Al Table of porphyry intrusions and felsic volcanics included in this study 166 Table A2 Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites 167
Table Bl Table of Zr enrichment factors, LOI-free major element abundances and relevant absolute mass change values 181 xi
Foreword
This thesis contains the results of research with economic and academic implications completed at Laurentian University in conjunction with government and industry support.
It contains three chapters and one appendix, including two papers produced in collaboration with my thesis supervisor (Dr. Stephen Piercey). The format of the thesis is as follows.
Chapter 1 is an introduction to the research, explaining why research needed to be performed on the association of porphyry intrusions to gold mineralization within the
Porcupine gold camp.
Chapter 2 tackles the main issues of this thesis, presenting and interpreting the data collected and discusses the implications of the data. It is written to be published in either
Economic Geology or the Canadian Journal of Earth Science, co-authored by Dr. Stephen
Piercey, who edited the original manuscript and aided in the development of ideas and interpretations.
Chapter 3 reviews the main conclusions of this thesis and presents potential avenues of future research.
Appendix A is a revised version of a paper previously published as part of an Ontario
Geological Survey (OGS) Open File Report. This paper's revisions include the deletion of geochemical data and interpretations from the original manuscript, as well as reformatting of porphyry intrusive suite subdivisions to coincide with the paper presented in Chapter 2. The original OGS Open File report was co-authored by Drs. Stephen
Piercey and Mike Hamilton who each edited the original manuscript, and of which the xii latter obtained new U-Pb geochronological data included within the publication. The
OGS Open File Report is:
MacDonald, P.J., Piercey, S.J. and Hamilton, M.A. 2005. An Integrated Study of
Intrusive Rocks Spatially Associated with Gold and Base Metal Mineralization in the
Abitibi Greenstone Belt, Timmins area and Clifford Township: Discover Abitibi
Initiative: Ontario Geological Survey, Open File Report 6160, 189p.
Appendix B presents the assessment of element immobility by comparisons of element abundances and element ratios commonly known to remain immobile during alteration versus: 1) other element abundances commonly known to remain immobile during alteration; 2) alteration, using an alteration monitor; and 3) Na20 mass change variations and associated immobile element mass changes (Barrett and MacLean 1994). 1
Chapter 1: An Introduction to the Porphyry Intrusions of the Porcupine Gold Camp, Western Abitibt Subprovince, Ontario.
1.1 Introduction
The Porcupine gold camp is one of the richest and most prolific gold mining camps in the world (Marmont and Corfu 1989; Robert and Poulsen 1997; Kerrich et al. 2000;
Bateman et al. 2008). Having produced over 60 million ounces of gold since discovery in 1909, the Porcupine gold camp mineralization is classified as structurally controlled quartz vein lode gold systems hosted within tholeiitic mafic volcanic rocks, siliciclastic sedimentary rocks and quartz-feldspar porphyritic intrusions (Ferguson 1968; Hodgson
1983; Burrows and Spooner 1986,1989; Wood et al. 1986; Proudlove et al. 1989;
Piroshco and Kettles 1991; Robert and Poulsen 1997; Burrows et al. 1993; Brisbin 1997,
2000; Brisbin and Pressaco 1999; Kerrich et al. 2000; Gray and Hutchinson 2001;
Bateman et al. 2008).
Although the bulk of the gold is not hosted by the quartz-feldspar porphyritic intrusions of the Porcupine gold camp, the mineralization is strongly spatially associated with the intrusions, which are present in the mine workings of almost every historic or active mine in the camp (Burrows 1925; Ferguson 1968; Luhta 1974; Davies 1977;
Davies and Luhta 1978a; Pyke 1982; Burrows and Spooner 1986, 1989; Mason and
Melnik 1986; Wood et al. 1986; Colvine et al. 1988; Colvine 1989; Piroshco and Kettles
1991; Moritz and Crocket 1991; Melnik-Proud 1992; Burrows et al. 1993; Gray 1994;
Brisbin 1997, 2000; Brisbin and Pressaco 1999; Gray and Hutchinson 2001; Robert 2001;
Dinel and Fowler 2004). The reasons for this spatial association are strongly debated, with varying ideas ranging from a cogenetic, hydromagmatic relationship (e.g., magmatic hydrothermal fluid relationship), to a structural involvement (e.g., nucleator of gold 2 controlling structures), to purely a coincidental association (Davies 1977; Davies and
Luhta 1978a, 1978b; Griffis 1978; Pyke 1982; Corvine 1983; Marmont 1983; Cherry
1983; Burrows and Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986;
Colvine et al. 1988; Piroshco and Kettles 1991; Melnik-Proud 1992; Burrows et al. 1993;
Gray 1994; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Gray and Hutchinson 2001;
Robert 2001). This thesis attempts to address the role of porphyries in the genesis of gold deposits in the Porcupine Camp, and provides new information, interpretations, and insights on the relationships between gold mineralization and the porphyry intrusions.
The following chapter will provide an introduction to the geology of the Porcupine gold camp, a review of previous research undertaken on the porphyry intrusions of the
Porcupine gold camp, the objectives of this thesis, the methods used in data collection and an overview of the format of this thesis.
1.2 Geological Overview of the Porcupine Gold Camp
The Porcupine gold camp is located within the Abitibi subprovince, a subdivision of the Archean Superior Province (Fig. 1.1). The Superior Province is the world's largest
Archean craton, stretching from Manitoba in the west, through northern Ontario and
Quebec in the east (Fig. 1.1: Card et al. 1989; Colvine 1989; Thurston 1991). It is composed of numerous east-northeast trending geological subprovinces, including volcanic-plutonic (granite-greenstone), metasedimentary belts, and/or high-grade gneisses that represent ancient volcanic arcs, flysch basins and micro-continent fragments
(e.g., Card et al. 1989). The subprovinces have been accreted to one another and typically have sharp (i.e., faults) or gradational contacts (zones of deformation and/or metamorphism: Fig. 1.1: Card and Ciesielski 1986; Colvine et al. 1988; Card 1990; Thurston and Chivers 1990; Hoffman 1990; Williams 1990; Thurston 1991; Percival et al. 1994; Pan and Fleet 1999; Daigneault et al. 2002). U-Pb zircon dates for the Superior
Province range from -3.0 Ga in the northwest corner (North Caribou terrane and
Northern Superior Superterrane), generally younging to the southeast to 2.6 Ga (Pontiac
Subprovince: Card et al. 1989; Corfu and Wood 1986; Corfu and Ayres 1991; Machado et al. 1991; Card and Poutsen 1998; Percival 2007).
The Abitibi subprovince is the largest volcano-plutonic (granite-greenstone) subprovince of the Superior Province (Fig. 1.1: Corfu et al. 1989; Hodgson and Hamilton
1989; Card 1990; Jackson and Fyon 1991; Brisbin and Pressaco 1999; Brisbin 2000;
Polat and Kerrich 2001; Ayer et al., 2003, 2005). It is located near the southeastern edge of the Superior Province within northern Ontario and Quebec, and is the second youngest of the Superior Province's subprovinces, with U-Pb geochronological ages ranging from
-2791-2670 Ma (Fig. 1.1: Ayer et al. 2003, 2005; Corfu et al. 1989; Bandyayera et al.
2004; Thurston et al. 2008). The Abitibi subprovince is composed of numerous volcanic
(greenstone) and sedimentary packages distinguished by distinctive geological and geochronological attributes (Fig. 1.2: Pyke 1982; Jackson and Fyon 1991; Corfu 1993;
Polat and Kerrich 2001; Ayer et al. 2002a, 2002b, 2003; Thurston et al. 2008). Large deformation zones cut across the subprovince from west to east and have been used to separate it into smaller districts (Fig. 1.2: Pyke 1982; Hodgson and Hamilton 1989;
Robert 2001; Ayer et al 2002b). One of these large deformation zones is the Porcupine-
Destor Deformation Zone (PDDZ), which strikes east, runs the entire length of the
Abitibi Subprovince and hosts the Porcupine gold camp (Fig. 1.2: Pyke 1982; Hodgson 4 and Hamilton 1989; Jackson and Fyon 1991; Easton 2000; Ayer et al. 2002b; Daigneault et al. 2002).
The oldest rocks in the Porcupine gold camp are the volcanic rocks of the Deloro
Assemblage (2734-2724 Ma), which are exposed within the Shaw Dome area south of the
PDDZ (Figs. 1.2-1.3: Pyke 1980, 1982; Jackson and Fyon 1991; Piroshco and Kettles
1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002b; Thurston et al.
2008). The Deloro Assemblage is composed of calc-alkaline mafic through felsic flows and pyroclastic rocks intercalated with banded iron formations near the top of the assemblage (Pyke 1980, 1982; Jackson and Fyon 1991; Piroshco and Kettles 1991;
Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002b; Thurston et al. 2008).
The Deloro assemblage is overlain by the volcanic Tisdale Assemblage (2710-2703 Ma), which hosts the majority of gold deposits in the Porcupine camp (Figs. 1.2-1.3: Pyke
1980, 1982; Burrows and Spooner 1989; Jackson and Fyon 1991; Moritz and Crocket
1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al 2002b). The volcanic flows of the Tisdale Assemblage range in composition from komatiite-tholeiite at the base through to the middle units of the assemblage (Hersey
Lake, Central and Vipond Formations) through calc-alkaline in the upper unit (Gold
Centre Formation: Fig. 1.3: Pyke 1980, 1982; Jackson and Fyon 1991; Brisbin 1997,
2000). Intercalated with the volcanic flows are very minor amounts of carbonaceous argillite and wacke (Pyke 1982; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Bateman et al. 2008).
The Tisdale Assemblage volcanic rocks are intruded by numerous porphyritic felsic bodies ca. 2687-2691 Ma (Corfu et al. 1989; Gray and Hutchinson 2001; Ayer et al. 5
2003, 2004). These quartz-feldspar porphyritic intrusions are the focus of this thesis and wiil be discussed further in the following chapter.
The Porcupine Assemblage lies unconformably above the Tisdale Assemblage within regional-scale basins such as the Porcupine and Kayorum Synclines (Figs. 1.2-1.3:
Ferguson 1968; Pyke 1982; Mason et al. 1988; Piroshco and Kettles 1991; Brisbin 1997,
2000; Brisbin and Pressaco 1999). The base of the Porcupine assemblage is the Krist
Formation (ca. 2687 Ma), which is coeval with the porphyry intrusions (Fig. 1.3:
McAuley 1983; Ayer et al. 2002b). The Krist Formation is locally underlain by a thin carbonaceous argillite and is overlain by a thick succession of interbedded wacke and argillite (Figs. 1.2-1.3: Ferguson 1968; Pyke 1982; Mason et al. 1988; Jackson and Fyon
1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 1999, 2002b).
Fluvial to shallow-marine sedimentary rocks of the Timiskaming Assemblage lie unconformably above the Porcupine Assemblage and were deposited into isolated topographic lows from 2676 to 2670 Ma (Fig. 1.3: Ayer et al. 2002b, 2003, 2005). This unit includes polymictic conglomerate and arenite as well as lesser wacke and argillite
(Pyke 1982; Jackson and Fyon 1991; Piroshco and Kettles 1991: Brisbin 1997, 2000;
Brisbin and Pressaco 1999; Ayer et al. 2002b).
Further intrusive magmatism occurred at 2672.8±1.1 Ma with the emplacement of late albitite dikes (Marmont and Corfu 1989; Corfu et al. 1989; Ayer et al. 2005). These albitite dikes represent the last magmatic event prior to gold mineralization, and although volumetrically minor, as they are present only at a few places within the Porcupine gold camp, they do show a strong spatial association with gold mineralization similar to that of 6 the porphyry intrusions (Melnik-Proud 1992; Brisbin 1997, 2000; Brisbin and Pressaco
1999).
Most gold mineralization events of the Porcupine gold camp post-date albitite dike emplacement at 2672.8±1.1 Ma (Marmont and Corfu 1989; Ayer et al. 2005) because gold-bearing veins cross-cut the albitite dikes (Melnik-Proud 1992; Brisbin 1997 &
2000). Re-Os geochronology on molybdenite from the Dome mine mineralization has been dated at 2670 ±10 Ma (Ayer et al. 2003) and molybdenite from the Mclntyre mine copper zone has been dated at 2672 ±7 Ma (Bateman et al. 2004), further supporting a young age for gold mineralization. Although the albitite dikes are cross-cut by the copper-gold veins, the Mclntyre mine copper zone date of 2672 Ma is similar to the emplacement age of albitite diking at the mine (2673 Ma: Marmont and Corfu 1989;
Corfu et al. 1989), which suggests that copper-gold mineralization of the Porcupine gold camp may be genetically related to hydrothermal activity generated by albitite dike emplacement, as previously suggested by Melnik-Proud (1992) and Brisbin (1997, 2000).
1.3 Previous Work
The spatial association of gold mineralization and felsic porphyry bodies has long been recognized in the Porcupine gold camp (e.g. Burrows 1925). Since discovery much of the research done on the camp has been, at least, partially focused on the porphyry bodies (e.g. Ferguson et al. 1968; Davies and Luhta 1978a; Pyke 1982; Burrows and
Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986; Corfu et al. 1989;
Burrows et al. 1993; Brisbin 2000; Gray and Hutchinson 2001; Ayer et al. 2002a, 2002b,
2003,2005; Bateman et al. 2004,2005,2008; Dinel et al. 2008). Although a wealth of research has been completed, very little descriptive documentation of the porphyry bodies 7 has been brought into the public domain excluding a few unpublished theses, including:
Luhta (1974); McAuley (1983); Melnik-Proud (1992); Gray (1994); and Brisbin (1997.)
Much of the previous research done on the camp has led to the hypothesis that the porphyry bodies were intrusive (Hurst 1936; Holmes 1944; Griffis 1962). This idea was questioned by Luhta (1974) and Davies (1977) who suggested that the porphyries represented felsic volcanic rocks. Luhta (1974) and Davies and Luhta (1978a) later suggested that these felsic porphyritic volcanic rocks were not originally porphyritic but rather that the porphyritic texture was a result of metasomatism by mineralizing fluids unrelated to the felsic porphyritic bodies; subsequently, this model became the subject of debate and due to a lack of evidence has been dismissed (e.g., Griffis 1978; Davies &
Luhta 1978b). In Pyke's (1982) regional overview of the Timmins area, he suggested that the porphyries were subvolcanic intrusions or alternatively, felsic domes.
A second debate of significance was introduced by Mason and Melnik (1986) who suggested that the gold and copper mineralization within the Hollinger-Mclntyre deposits was a result of an Archean porphyry-type hydrothermal system, similar to Phanerozoic porphyry-copper deposits. Conversely, Wood et al. (1986) and Burrows and Spooner
(1986) suggested that the gold and copper mineralization occurred late during deformation, whereas the porphyries predated or were emplaced early during regional deformation, suggesting a time gap between porphyry magmatism and gold mineralization. This view was corroborated by the U-Pb geochronological studies of
Corfu et al. (1989) and Marmont and Corfu (1989), which indicated a temporal separation of at least 15 Ma between porphyry emplacement and gold mineralization.
Further workers suggested that porphyry magmatism was not the cause of gold g mineralization, but rather a later albitite diking event was the driving force of the hydrothermal mineralizing system (Melnik-Proud 1992; Brisbin 1997, 2000). This hypothesis was challenged by Burrows et al. (1993) who argued that mineralization was deposited in structurally favourable zones/traps unrelated to intrusion-related hydrothermal activity.
Gray (1994) combined the earlier two models for mineralization, intrusion-related hydrothermal system versus deformation-related system, into a single model. Gray
(1994) suggested that early Cu-Au mineralization was the result of intrusion-related hydrothermal activity and was followed by a later structural-related gold mineralization event responsible for the bulk of the mineralization within the Timmins camp. Gray and
Hutchinson (2001) further suggested that there were two separate porphyry intrusion types: quartz-feldspar porphyries and feldspar porphyries. This hypothesis has since been abandoned due to an internal Placer-Dome geochemical study as well observations collected by this study that demonstrated that the two separate porphyry intrusion types described by Gray and Hutchinson (2001) are geochemically identical and thus, genetically related, with petrographic differences related to magma fractionation and segregation, rather then petrogenetic differences (Wells 2001).
Recent Re-Os molybdenite geochronology has further dismissed the possibility of a genetic relationship between porphyry magmatism and gold-copper mineralization. A U-
Pb zircon age of 2672 ±7 Ma from Au-bearing quartz veins at the Mclntyre mine
(Bateman et al. 2004) illustrates that the gold mineralization is >15 Ma younger than the porphyry intrusions. 9
1.4 Objectives
Even though the porphyry intrusive bodies have been the partial focus of various past studies (Luhta 1974; Davies and Luhta 1978a; Gorman et al. 1981; Karvinen 1982; Pyke
1982; Burrows and Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986;
Melnik-Proud 1992; Burrows et al. 1993; Gray 1994; Brisbin 1997, 2000; Gray and
Hutchinson 2001; Robert 2001; Dinel and Fowler 2004), as discussed above, much debate still exists on the various aspects of intrusion pedogenesis and relationship to gold mineralization. It is the aim of this thesis to:
1) compare and contrast field relationships, petrology, geochemistry and
geochronology of the different porphyry intrusions throughout the entire
Porcupine gold camp; on the north and south sides of the PDDZ from 20 km west
of Timmins to near Matheson, over 60 km east of Timmins (Fig. 1.2);
2) test correlations of the porphyry intrusions with the extrusive Krist Formation and
other felsic volcanic units, in the vicinity of Timmins, and around the periphery of
the Shaw Dome;
3) identify differences between mineralized and barren porphyry intrusions;
4) investigate the petrogenesis of the porphyry intrusions, discussing implications
bearing on the geological evolution and mineralization of the Porcupine gold
camp.
1.5 Methodology
1.5.1 Geological Mapping and Sampling
Field mapping, drill core examination and sampling was conducted by the author over the summer months of 2003 and 2004, with summary presentations of the field results 10 published by the Ontario Geological Survey (MacDonald and Piercey 2003; MacDonald et al. 2004; MacDonald et al. 2005). Field mapping and drill core logging was done at
1:1000 to 1:5000 scales to identify relationships between the various porphyry intrusions and the rocks they intruded, as well as alteration assemblages and mineralization spatially associated to the porphyry intrusions.
Over 150 representative samples of porphyry intrusions and felsic volcanics were collected from outcrop, drill core and mine workings. The samples are representative of the different primary textures, alteration facies and mineralization styles observed in each of the porphyry intrusions examined. A spectrum of porphyry intrusions were sampled ranging from intrusions with a strong spatial association to mineralization to intrusions with no known mineralization. All intrusions were sampled in at least duplicate, often in different locations, to test textural and geochemical homogeneity.
1.5.2 Lithogeochemistry
Of the 150 representative samples, 119 samples were analyzed for major and trace element geochemistry. These analyses were used to: 1) decipher primary and alteration- related petrography; 2) separate intrusions into genetic suites and to distinguish their potential petrogenesis; and 3) identify differences between mineralized intrusions vs. barren intrusions. This latter aspect is the primary and most significant contribution of this thesis.
Lithogeochemistry utilized within this thesis includes major, trace and rare earth element abundances determined by X-ray fluorescence (XRF) at the Ontario Geoscience
Laboratory (Sudbury, Ontario) and at ActLab (Ancaster, Ontario), by inductively coupled plasma emission spectroscopy (ICP-ES) at the Ontario Geoscience Laboratory (Sudbury, 11
Ontario) and by inductively coupled plasma mass spectroscopy (ICP-MS) at the Ontario
Geoscience Laboratory (Sudbury, Ontario). Details on the methodology, precision and accuracy of these techniques and analyses are presented in Chapter 3.
1.6 Thesis Presentation
Contained within this thesis following this introductory chapter is a chapter containing a research manuscript intended for submission to an international scientific journal followed by a summation chapter. Appendix A includes an updated version of a previous manuscript previously published by the Ontario Geological Survey (OGS) as an
OGS Open File (see MacDonald et al. 2005) and Appendix B includes the assessment of the immobility of elements. The contents of the following chapters are outlined below.
Chapter 2 presents the results of a regional geological and geochemical study of the porphyry intrusions of the Porcupine gold camp. By combining the detailed geological attributes of the intrusions with alteration and lithological geochemistry, Chapter 2 documents similarities and key differences between intrusions associated with gold mineralization and barren intrusions within the Porcupine gold camp. Chapter 2 further discusses the petrogenesis of the intrusions and the reasons for the association between gold mineralization and the porphyry intrusions within the Porcupine gold camp.
A summary of the key observations, discussion and conclusions of the thesis is presented in Chapter 3. This chapter also outlines unresolved questions and possible research avenues for future work.
Appendix A presents a detailed description of the porphyry intrusions within the
Porcupine gold camp. Utilizing geographical and geological observations the many porphyry intrusions examined are grouped into five intrusive suites with each suites 12 location, field relationships, petrography, alteration, veining, mineralization, deformation and geochronology described. A similar description of felsic volcanic rocks is also presented. A comparison between the different intrusive suites, along with a comparison of the porphyry intrusive suites to the Krist Formation and other felsic volcanics is then discussed.
Appendix B presents the assessment of element immobility utilized in chapter 2 for petrogenetic interpretations. The assessment of element immobility is illustrated by comparisons of element abundances and element ratios commonly known to remain immobile during alteration versus: 1) other element abundances commonly known to remain immobile during alteration (Barrett and MacLean 1994); 2) alteration, using the
Ab03/Na20 alteration index as an alteration monitor (Spitz and Darling 1978; Piercey et al. 2002); and 3) Na20 mass change variations and associated immobile element mass changes (Barrett and MacLean 1994).
1.7 References
Ayer, J.A., Berger, B.R. and Trowell, N.F. 1999a. Geological Compilation of the Timmins area, Abitibi greenstone belt: Ontario Geological Survey, Map P.3398, scale 1:100 000. Ayer, J.A., Berger, B.R. and Trowell, N.F. 1999b. Geological Compilation of the Lake Abitibi area, Abitibi greenstone belt: Ontario Geological Survey, Map P.3398, scale 1:100 000. Ayer, J., Amelin, Y., Corfu, F., Kamo, S., Ketchum, J.F., Kwok, K. and Trowell, H.F. 2002a. Evolution of the Abitibi greenstone belt based on U-Pb geochronology: autochthonous volcanic construction followed by plutonism, regional deformation and sedimentation: Precambrian Research, v.l 15, p.63-95. Ayer, J., Ketchum, J., and Trowell, N. 2002b. New geochronological and Nd isotopic results from the Abitibi Greenstone belt, with emphasis on timing and tectonic implications of late Archean sedimentation and volcanism; in Summary of Field Work and Other Activities 2002: Ontario Geological Survey, Open File Report 6100, p.5-lto5-16. 13
Ayer, J., Barr, E., Bleeker, W., Creaser, R., Hall, G., Ketchum, J., Powers, D., Salier, B., Still, A. and Trowell, N. 2003. Discover Abitibi. New Geochronological Results from the Timmins Area: Implications for the Timing of Late-Tectonic Stratigraphy, Magmatism and Gold Mineralization; in Summary of Field Work and Other Activities 2003: Ontario Geological Survey, Open File Report 6120, p.33-1 to 33-11. Ayer, J.A., Thurston, P.C., Bateman, R., Dube, B., Gibson, H.L., Hamilton, M.A., Hathway, B., Hocker, S.M., Houle, M.G., Hudak, G., Ispolatov, V.O., Lafrance, B., Lesher, CM., MacDonald, P.J., Peloquin, A.S., Piercey, S.J., Reed, L.E. and Thompson, P.H. 2005. Overview of results from the Greenstone Architecture Project: Discover Abitibi Initiative: Ontario Geological Survey, Open File Report 6154, 146p. Bandyayera, D., Rheaume, P., Doyon, J., and Sharma, K. N. M. 2004. Geologie de la region du lac Hebert: Ministere des Ressources naturelles et de la Faune du Quebec rapport RG 2003-07, 57p. Barrett, T.J. and MacLean, W.H. 1994. Chemostratigraphic and Hydrothermal Alteration in Exploration for VHMS Deposits in Greenstones and Younger Volcanic Rocks; in Alteration and Alteration Processes associated with Ore-forming Systems, edited by Lentz, D.R.: Geological Association of Canada, Short Course Notes, v.l 1, p.433-467. Bateman, R., Ayer, J.A., Barr, E., Dube, B. and Hamilton, M.A. 2004. Discover Abitibi. Gold Subproject 1. Protracted Structural Evolution of the Timmins-Porcupine Gold Camp and the Porcupine-Destor Deformation Zone; in Summary of Field Work and Other Activities 2004: Ontario Geological Survey, Open File Report 6145, p.41- 1 to 41-10. Bateman, R., Ayer, J.A., Dube, B. and Hamilton, M.A. 2005. The Timmins-Porcupine gold camp, northern Ontario: the anatomy of an Archaean greenstone belt and its gold mineralization: Discover Abitibi Initiative: Ontario Geological Survey, Open File Report 6158, 90p. Bateman, R., Ayer, J.A. and Dube, B. 2008. The Timmins-Porcupine Gold Camp, Ontario: Anatomy of an Archean Greenstone Belt and Ontogeny of Gold Mineralization: Economic Geology, v.103, p.1285-1308. Brisbin, D.I. 1997. Geological setting of gold deposits in the Porcupine mining district, Timmins, Ontario. Unpublished Ph.D. thesis, Queens University, Kingston, Ontario, 523p. Brisbin, D.I. 2000. World Class Intrusion-Related Archean Vein Gold Deposits of the Porcupine Gold Camp, Timmins Ontario; in Geology and Ore Deposits 2000: The Great Basin and Beyond; edited by Cluer, J.K., Price, J.G., Struhsacker, E.M., Hardyman, R.F. and Morris, C.L.: Geological Society of Nevada Symposium Proceedings, May 15-18, 2000, p. 19-35. Brisbin, D.I. and Pressaco, R. 1999. World-class Archean vein gold deposits of the porcupine camp, Timmins, Ontario: Geological Association of Canada, Joint Annual Meeting, Field Trip A3 Guidebook, 98p. Burrows, A.G. 1925. The Porcupine gold area. Ontario Bureau of Mines, v.33, pt.2, 112p. 14
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Davies, J.F. 1977. Structural interpretation of the Timmins mining area: Canadian Journal of Earth Science, v.14, p.1046-1053. Davies, J.F. and Luhta, L.E. 1978a. An Archean "Porphyry-type" Disseminated Copper Deposit, Timmins, Ontario: Economic Geology, v.73, p.383-396. Davies, J.F. and Luhta, L.E. 1978b. An Archean "Porphyry-type" Disseminated Copper Deposit, Timmins, Ontario - A reply: Economic Geology, v.74, p.687. Dinel, E. and Fowler, A.D. 2004. Discover Abitibi. Preliminary Results of the Geology and Geochemistry of the Volcanic Rocks Hosting the Hoyle Pond Mine, Timmins, Ontario; in Summary of Field Work and Other Activities 2004: Ontario Geological Survey, Open File Report 6145, p.46-1 to 46-4. Dinel, E., Fowler, A.D., Ayer, J., Still, A., Tylee, K. and Barr, E. 2008. Lithogeochemical and Stratigraphic Controls on Gold Mineralization within the Metavolcanic Rocks of the Hoyle Pond Mine, Timmins, Ontario. Economic Geology, v. 103, p. 1341-1363. Easton, R.M. 2000. Metamorphism of the Canadian Shield, Ontario, Canada: I. The Superior Province: The Canadian Mineralogist, v.38, p.287-317. Ferguson, S.A. et al. 1968. Geology and ore deposits of Tisdale Township, District of Cochrane: Ontario Department of Mines, Geological Report 58, 117p. Gorman, B.E., Kerrich, R. and Fyfe, W.S. 1981. Geochemistry and Field Relations of Lode Gold Deposits in Felsic Igneous Intrusions- Porphyries of the Timmins District: Ontario Geological Survey, Miscellaneous Paper 98, p.108-124. Gray, M.D. 1994. Multiple Gold Mineralizing Events in the Porcupine Mining District, Timmins Area, Ontario, Canada. Unpublished Ph.D. thesis, Colorado School of Mines, Gold Colorado, 220p. Gray, M.D. and Hutchinson, R. W. 2001. New Evidence for Multiple Periods of Gold Emplacement in the Porcupine Mining District, Timmins Area, Ontario, Canada: Economic Geology, v.96, p.453-475. Griffis, A.T. 1962. A geological study of the Mclntyre mine: Canadian Institute of Mining and Metallurgy, Bulletin, v.55, no.598, p.76-83. Griffis, A.T. 1978. An Archean "porphyry-type" disseminated copper deposit, Timmins, Ontario - A discussion: Economic Geology, v.74, p.695-696. Hodgson, C.J. 1983. The structure and Geological Development of the Porcupine Camp - a Re-evaluation; in The geology of Gold in Ontario; edited by Colvine, A.C.: Ontario Geological Survey, Miscellaneous Paper 110, p.48-55. Hodgson, C.J. and Hamilton, J.V. 1989. Gold Mineralization in the Abitibi Greenstone Belt: End-Stage Result of Archean Collisional Tectonics: Economic Geology, Monograph 6, p.86-100. Hoffman, P.F. 1990. On accretion of granite-greenstone terranes; in Greenstone Gold and Crustal Evolution; edited by Robert, F., Sheahan, P.A. and Green, S.B: Geological Association of Canada, Nuna Conference volume, p.32-45. Holmes, T.C. 1944. Some porphyry-sediment contacts at the Dome mine, Ontario: Economic Geology, v.39, p. 133-141. Hurst, M.E. 1936. Recent studies in the Porcupine area: Canadian Institute of Mining and Metallurgy, Transactions, v.45, p.379-386. 16
Jackson, S.L. and Fyon, J.A. 1991. The western Abitibi Subprovince in Ontario; in Geology of Ontario; edited by Thurston, P.C., Williams, H.R., Sutcliffe, H.R. and Stott, G.M.: Ontario Geological Survey, Special Volume 4, pt.l, p.405-484. Karvinen, W.O. 1982. Geology and evolution of gold deposits, Timmins area, Ontario: Canadian Institute of Mining and Metallurgy, Special Volume 24, p. 101-124. Kerrich, R., Goldfarb, R., Groves, D. and Garwin, S. 2000. The Geodynamics of World-Class Gold Deposits: Characteristics, Space-Time Distribution and Origins: Reviews in Economic Geology, v. 13, p.501-551. Luhta, L.E. 1974. A Petrographic and Mineralogic Study of the Mclntyre Disseminated Copper Deposit. Unpublished M.Sc. thesis, Laurentian University, Sudbury, Ontario, 97p. MacDonald, P.J. and Piercey, S.J. 2003. Discover Abitibi. Gold Subproject 3. Preliminary Regional Geological assessment of porphyry intrusions spatially associated with gold deposits in the Western Abitibi Subprovince, Timmins, Ontario; in Summary of Field Work and Other Activities 2003: Ontario Geological Survey, Open File Report 6120, p.36-1 to 36-7. MacDonald, P.J., Piercey, S.J. and Hamilton, M.A. 2004. Discover Abitibi. Gold Subproject 3. Regional Geological assessment of porphyry intrusions spatially associated with Gold Deposits along the Porcupine-Destor Deformation Zone, Western Abitibi Subprovince, Timmins, Ontario; in Summary of Field Work and Other Activities 2004: Ontario Geological Survey, Open File Report 6145, p.43-1 to 43-7. MacDonald, P.J., Piercey, S.J. and Hamilton, M.A. 2005. An Integrated Study of Intrusive Rocks Spatially Associated with Gold and Base Metal Mineralization in the Abitibi Greenstone Belt, Timmins area and Clifford Township: Discover Abitibi Initiative: Ontario Geological Survey, Open File Report 6160, 189p. Machado, N., Rive, M., Gariepy, C. and Simard, A. 1991. U-Pb geochronology of granitoids from the Pontiac Subprovince, preliminary results: Geological Association of Canada, Program Abstracts, v. 16, p.A78. Marmont, S. 1983. The Role of Felsic Intrusions in Gold Mineralization; in The Geology of Gold in Ontario; edited by Colvine, A.C.: Ontario Geological Survey, Miscellaneous Paper 110, p.38-47. Marmont, S. and Corfu, F. 1989. Timing of Gold Introduction in the Late Archean Tectonic Framework of the Canadian Shield: Evidence from U-Pb Zircon Geochronology of the Abitibi Subprovince: Economic Geology, Monograph 6, p.101-111. Mason, R., Brisbin, D.I., and Aitken, S. 1988. The Geological Setting of Gold Deposits in the Porcupine Mining Camp; in Geoscience Research Grant Program. Summary of Research, 1987-1988: Ontario Geological Survey, Miscellaneous Paper 140, p.133- 145. Mason, R. and Melnik, N. 1986. The Anatomy of an Archean Gold System-The Mclntyre-Hollinger Complex at Timmins, Ontario, Canada; in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A. J. Macdonald. Toronto, p.40-55. 17
McAuley, J.B. 1983. A Petrographic and Geochemical Study of the Preston, Preston West, and Paymaster porphyries, Timmins, Ontario. Unpublished M.Sc. thesis, Laurentian University, Sudbury, Ontario, 118p. Melnik-Proud, N. 1992. The geology and ore controls in and around the Mclntyre Mine at Timmins, Ontario, Canada. Unpublished Ph.D. thesis, Queen's University, Kingston, Ontario, 353p. Moritz, R.P. and Crocket, J.H. 1991. Hydrothermal Wall-Rock Alteration and Formation of the Gold-Bearing Quartz-Fuchsite veins at the Dome Mine, Timmins area, Ontario, Canada: Economic Geology, v.86, p.620-643. Pan, Y. and Fleet, M.E. 1999. Kyanite in the Western Superior Province of Ontario: Implications for Archean Accretionary Tectonics: The Canadian Mineralogist, v.37, p.359-373. Percival, J.A. 2007. Geology and metallogeny of the Superior Province, Canada; in Mineral Deposits of Canada: A Synthesis of Major Deposit-Types, District Metallogeny, the Evolution of Geological Provinces, and Exploration Methods; edited by Goodfellow, W.D.: Geological Association of Canada, Mineral Deposits Division, Special Publication Number 5, p.903-928. Percival, J.A., Stern, R.A., Skulski, T., Card, K.D., Mortensen, J.K. and Begin, N.J. 1994. Minto Block, Superior Province: missing link in deciphering assembly of the craton at 2.7 Ga.: Geology, v.22, p.839-842. Piercey, S.J., Mortensen, J.K., Murphy, D.C., Paradis, S. and Creaser, R.A. 2002. Geochemistry and tectonic significance of alkalic mafic magmatism in the Yukon- Tanana terrane, Finlayson Lake region, Yukon.: Canadian Journal of Earth Sciences, v.39,p.l729-1744. Piroshco, D.W. and Kettles, K. 1991. Structural geology of Tisdale and Whitney Townships, Abitibi Greenstone Belt, District of Cochrane, Northeastern Ontario: Ontario Geological Survey, Open File Report 5768, 115p. Proudlove, D.C., Hutchinson, R.W. and Rogers, D.S. 1989. Multiphase Mineralization in Concordant and Discordant Gold Veins, Dome Mine, South Porcupine, Ontario, Canada: Economic Geology, Monograph 6, p. 112-123. Polat, A. and Kerrich, R. 2001. Geodynamic processes, continental growth and mantle evolution recorded in late Archean greenstone belts of the southern Superior Province, Canada: Precambrian Research, v.l 12, p.5-25. Pyke, D.R. 1980. Relationship of Gold Mineralization to Stratigraphy and Structure in Timmins and Surrounding Area; in Genesis of Archean, Volcanic Hosted Gold Deposits; edited by Pye, E.G. and Roberts, R.G.: Ontario Geological Survey, Miscellaneous Paper 97, p. 1-15. Pyke, D.R. 1982. Geology of the Timmins Area, District of Cochrane: Ontario Geological Survey, Geological Report 219, 141 p. Robert, F. 2001. Syenite-associated disseminated gold deposits in the Abitibi greenstone belt, Canada: Mineralium Deposita, v.36, p.503-516. Robert, F. and Poulsen, K.H. 1997. World-class Archean gold deposits in Canada: an overview: Australian Journal of Earth Science, v.44, p.329-351. Spitz, G. and Darling, R. 1978. Major and minor element lithogeochemical anomalies surrounding the Louvem copper deposit, Val d'Or, Quebec: Canadian Journal of Earth Science, v. 15, p. 1161-1169. 18
Thurston, P.C. 1991. Archean Geology of Ontario: introduction; in Geology of Ontario; edited by Thurston, P.C, Williams, H.R., Sutcliffe, H.R. and Stott, G.M.: Ontario Geological Survey, Special Volume 4, pt.l, p.73-80. Thurston, P.C. and Chivers, K.M. 1990. Secular variations in greenstone sequence development emphasizing the Superior Province, Canada: Precambrian Research, v.46,p.21-58. Thurston, P.C, Ayer, J.A., Goutier, J., and Hamilton, M.A. 2008. Depositional gaps in Abitibi greenstone belt stratigraphy: A key to exploration for syngenetic mineralization: Economic Geology, v. 103, p. 1097-1134. Wells, R.C. 2001. Petrographic, lithogeochemical and interpretative report on a porphyry sample suite, Dome mine area. Internal, unpublished report for Placer Dome Ltd., 32p. Williams, H.R. 1990. Subprovince accretion tectonics in the south-central Superior Province: Canadian Journal of Earth Science, v.27, p.570-581. Wood, P.C, Burrows, D.R., Thomas, A.V. and Spooner, E.T.C 1986. The Hollinger- Mclntyre Au-Quartz Vein System, Timmins, Ontario, Canada; Geologic Characteristics, Fluid Properties and Light Stable Isotope Geochemistry; in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A. J. Macdonald. Toronto, p.56-80. 19
Canada
USA 0 200 400 1 i i • I i • • I Kilometers Ashuanipi
Bienville MANITOBA La Grande,- ^Northern Superior Superterrane Pikwitonei / <-->SuttSuttori< V Opinaca teS>i Island Lake - . Oxford-Stull QUEBEC ONTARIO Opatica North Caribou
Uchi nglisnRiyej jg^5
', Minnesota River Valley Boundary Water J ^ ""-, Political Boundary Figure 1.1. Simplified geological map of the Archean Superior Province, displaying the east- northeast trending Subprovinces (modified from Thurston et al. 2008). 20
I .' -I Porcupine Assemblage Kinojevis Assemblage I I Tisdale Assemblage 8tZ I Y I Kidd-Munro Assemblage I E^<3 Stoughton-Roquemaure a ^"^ Assemblage V/\ Deloro Assemblage » " Major Fault ^f Town Kilometers 10 20
Figure 1.2. Simplified regional geological map of the Porcupine gold camp, Abitibi Subprovince (modified from Ayer et al. 1999a, 1999b). 21
Timiskaming Assemblage: Dominantly composed of interbedded medium- to coarse-grained siliciclastic metasedimentary rocks.
Unconformity Porcupine Assemblage: Beatty Formation Dominantly composed of turdibidic fine- to medium-grained siliciclastic metasedimentary rocks. Krist Formation Dominantly composed of intermediate to felsic .•».* a-'gi\a-* conglomeritic volcaniclastic, lapilli tuff and lappillistone rocks. "~™~"~ Unconformity
Tisdale Assemblage: Gold Centre Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows.
Vipond Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows. Central Formation Dominantly composed of Mg-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows. Hersey Lake Formation Dominantly composed of komatiitic to basaltic- komatiite metavolcanic flows. • Porcupine-Destor Deformation Zone
Deloro Assemblage: Dominantly composed of mafic, calc-alkaline metavolcanic flows interbedded with felsic volcaniclastic and banded iron formations at the top.
Figure 1.3. Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt. Assemblages included are the Deloro, Tisdale, Porcupine and Timiskaming (modified from Pyke 1982; Ayer et al. 2002b). Maximum thicknesses of Assemblages is presented excluding the Deloro Assemblage. 22
Chapter 2: The Geology, Lithogeochemistry and Petrogenesis of Intrusions Associated with Gold Mineralization in the Porcupine Gold Camp, Timmins, Canada
2.1 Abstract
Most gold deposits within the Porcupine gold camp of the Abitibi greenstone belt are spatially associated with porphyry intrusions. These intrusions, however, are present beyond the immediate gold-hosting environment, extending over 80 kilometers along the
Porcupine-Destor deformation zone (PDDZ). Although petrographically similar, the intermediate to felsic intrusions along the PDDZ represent at least four distinct, geochemically defined magmatic suites that span the deformation history of the
Porcupine gold camp. The Timmins porphyry intrusive suite (TIS) intrusions are related to magma-generated Dl-related crustal thickening associated with uplift and extension as a result of flat subduction-related underplating of mafic crust, and resultant delamination and partial melting ca. 2690 Ma during Dl deformation at depths <40 kilometers. These
TIS magmas were emplaced near surface and represent subvolcanic intrusions to coeval eruptive equivalents such as the Krist Formation pyroclastic volcanic rocks. Two additional suites of lower crustal sourced magmas, the Carr Township porphyry intrusive suite (CIS) and the granodiorite intrusive suite (GIS) were generated from mafic source rocks 10-15 m.y. later. The CIS was generated by lower crustal melting at shallower depths than the TIS, whereas the GIS was generated at greater depths than the TIS indicating that, in the immediate vicinity of Timmins, D2-related magmatism and thrust stacking significantly thickened the crust to in excess of 40 kilometers. The Holmer intrusive suite (HIS) is a late- to post-tectonic suite formed via the partial melting and fractionation of magma sourced from slab-melt altered mantle at depths >40 kilometers. 23
Gold mineralization has long been recognized to be spatially associated with intrusions proximal to the PDDZ. Although there is no genetic link between spatially related porphyries and mineralization, gold mineralization is associated with sulphidized, sericite ± carbonate altered TIS intrusions emplaced during Dl, and to a lesser extent with the late- to post-tectonic HIS and GIS intrusions. The spatial association of gold with the TIS intrusions is related to the intrusions and gold utilizing the same emplacement conduits, presumably reactivated regional faults, as well as the formation of dilation zones surrounding the intrusions during deformation. Similar to gold mineralization, copper mineralization is spatially associated to the Porcupine intrusive suites but does not have a genetic association.
2.2 Introduction
The Porcupine gold camp represents one of the world's most prolific gold mining camps with over 60 million oz. of gold having been produced since its discovery in 1909
(Card et al. 1989; Robert and Poulsen 1997; Brisbin 2000). Within the Porcupine gold camp, gold mineralization shows a strong spatial association with intermediate to felsic meta-intrusive rocks loosely termed 'porphyries' (herein termed the Porcupine intrusive suites; Fig. 2.1). Although most of the gold produced from the Porcupine camp has been within one kilometer of these intrusions (Fig. 2.2) the exact reasons for the porphyry relationship to gold mineralization remains unknown (Gray and Hutchinson 2001).
The spatial association between gold mineralization and porphyry bodies has been recognized since the early days of mining (e.g. Burrows 1925). With the creation of the porphyry ore deposit model by Lowell and Guilbert (1970), hydro-magmatic models for the Porcupine gold camp were proposed based on the association of gold mineralization with the porphyry bodies (Davies and Luhta 1978; Mason and Melnik 1986a, 1986b). 24
But these ideas were immediately debated, based on observations that gold mineralization within the Porcupine gold camp was late syn- to post-tectonic, whereas the porphyry bodies were pre- to early syn-tectonic representing a time-gap between porphyry emplacement and gold mineralization (Wood et al. 1986; Burrows and Spooner
1986). To complement this observation, Wood et al. (1986), Burrows and Spooner
(1986) and Burrows et al. (1993) suggested that the gold-porphyry relationship was structural with gold-bearing structures having developed along the margins of the porphyries during regional deformation. Further documentation of a time gap between porphyry emplacement and gold mineralization based on U-Pb zircon geochronology also suggested that the porphyries pre-dated mineralization significantly (Corfu et al.
1989; Marmont and Corfu 1989). Recently, however, Gray and Hutchinson (2001) proposed that the Porcupine gold camp had undergone two separate gold mineralization events, including an early porphyry related copper-gold event (e.g., magmatic- hydrothermal) followed by a younger, structural event (i.e., orogenic) responsible for the bulk of the gold mineralization. Thus, there still remains an uncertain spatial and genetic relationship between the Porcupine intrusive suite and gold in the Porcupine camp.
As an attempt to contribute to the debate, research reported herein was undertaken to document the field relationships, petrology and geochemical attributes of the Porcupine intrusive suites within the Porcupine gold camp, along the Porcupine-Destor Deformation
Zone (PDDZ). Preliminary documentation has been presented by MacDonald and Piercey
(2003), MacDonald et al. (2004), and MacDonald et al. (2005). Field relationships, petrography and geochronological data are described below, followed by presentation of lithogeochemical (major, trace, rare-earth element) data for the Porcupine intrusive suites. This geochemical data will be utilized to constrain the petrogenetic history of the 25 intrusive suites, their lithogeochemical features in comparison to coeval felsic volcanism, lithogeochemical differences between gold-associated and gold-barren intrusive rocks and the association of a given intrusive suite with gold and copper mineralization.
2.3 Regional Geological Setting
The oldest rocks in the Porcupine gold camp are the calc-alkaline volcanic rocks of the Deloro Assemblage (-2730 Ma), which are exposed south of the PDDZ (Figs. 2.1 &
2.3; Pyke 1982; Brisbin 1997, 2000; Ayer et al. 2002a, 2002b; Bateman et al. 2005).
Most gold deposits of the Porcupine camp, however, are north of the PDDZ in volcanic flows of the younger Tisdale Assemblage (2710-2703 Ma; Figs. 2.1 & 2.3; Pyke 1982;
Brisbin 1997, 2001; Ayer et al. 2002a, 2002b; Bateman et al. 2005). The volcanic flows of the Tisdale Assemblage range in composition from komatiitic at the base of the assemblage (Hersey Lake Formation) through Fe-tholeiitic (Central, Vipond and Gold
Centre formations) in the middle to upper units of the assemblage (Fig. 2.3; Pyke 1982;
Brisbin 1997, 2000; Ayer et al. 2002a, 2002b; Bateman et al. 2005).
Prior to gold mineralization, the Tisdale Assemblage volcanic rocks were intruded by numerous -2687-2691 Ma (Corfu et al. 1989; Ayer et al. 2003), intermediate to felsic porphyritic intrusions (the Porcupine intrusive suite; Fig. 2.1 & 2.3; MacDonald et al.
2005). Coeval with the porphyry intrusions are the felsic metavolcanic rocks of the Krist
Formation (-2687 Ma), which form the base of the Porcupine Assemblage and unconformably overlie the Tisdale Assemblage within the Porcupine camp (Figs. 2.1 &
2.3; Pyke 1982; Brisbin 1997, 2000; Ayer et al. 2002a, 2002b; Bateman et al. 2005).
Post-dating the intermediate to felsic magmatism of the porphyry intrusions and Krist
Formation metavolcanics, but predating gold mineralization, are clastic sedimentary rocks of the middle and upper sections of the Porcupine Assemblage, which were 26 deposited -2687 Ma (Figs. 2.1& 2.3; Ayer et al. 2002a, 2002b; Bateman et al. 2005).
These sedimentary units overlie the Krist Formation in basins such as the Porcupine and
Kayorum Synclines (Fig. 2.2; Pyke 1982; Brisbin 1997, 2000; Ayer et al. 2002a, 2002b).
Coarse-grained, clastic strata of the Timiskaming Assemblage post-dates the Porcupine
Assemblage and was deposited from 2676 to 2670 Ma (Pyke 1982; Brisbin 1997, 2000;
Ayer et al. 2003, 2005; Bateman et al. 2005).
Further intrusive magmatism occurred at 2672.8 ±1.1 Ma with the localized emplacement of albitite dikes (Corfu et al. 1989; Ayer et al. 2005). The majority of gold mineralization in the Porcupine camp post-dates the albitite dikes (Melnik-Proud 1992;
Burrows et al. 1993; Brisbin 1997, 2000; Bateman et al. 2005) because gold-bearing veins cross-cut the albitite dikes (Melnik-Proud 1992; Brisbin 1997, 2000). Recent Re-
Os molybdenite geochronology further supports this assertion as molybdenite from the
Dome mine gold zone has yielded an age of 2670 ±10 Ma (Ayer et al. 2003) and molybdenite from the Mclntyre mine copper zone has yielded an age of 2672 ±7 Ma
(Bateman et al. 2004). Although the albitite dikes are cross-cut by the copper-gold veins, the Mclntyre mine copper zone Re-Os date of 2672 ±7 Ma is within the error range of the age of albitite dikes (2673 Ma; Corfu et al. 1989), which suggests that earlier copper-gold mineralization may be genetically related to hydrothermal activity generated by albitite dike emplacement, as previously suggested by Melnik-Proud (1992) and
Brisbin (1997, 2000).
2.4 Geological Attributes
2.4.1 Geological Attributes of Porcupine Intrusive Suites
The intrusions of the Porcupine camp all display near identical characteristics, but are grouped into four suites based on location, geology and lithogeochemistry (MacDonald et 27 al. 2005). The suites include the: Timmins porphyry intrusive suite (TIS), Carr Township porphyry intrusive suite (CIS), Holmer intrusive suite (HIS) and granodiorite intrusive suite (GIS). The TIS is further subdivided into TIS-main camp and TIS-other by the location of the individual intrusions. TIS-main camp represents intrusions within the immediate vicinity of the Timmins town site. TIS-other includes more distal porphyry intrusions, located south of the PDDZ, west of the Mattagami River Fault and east of the
Burrows-Benedict Fault (Fig. 2.1). The individual intrusions that make up each of the suites are presented on Figure 2.1 and Table 2.1, and their geographical and geological relationships, petrography, metamorphism, alteration, deformation, veining, emplacement age and association to mineralization are summarized in Table 2.2 (also see Appendix A and MacDonald et al. 2005).
All of the suites constitute groups of three or more intrusions generally trending east- west with individual intrusions ranging from meter- to kilometer-scale that have sill-, dike-, and plug-like forms (Figs. 2.1 and 2.2). The intrusions have generally intruded subparallel to the volcanic stratigraphy at four discrete stratigraphic levels: 1) the upper units of the Deloro Assemblage; 2) at the contact of the Deloro/Tisdale Assemblages; 3) within the lower to middle units of the Tisdale Assemblage; and 4) at the contact of the
Tisdale/Porcupine Assemblages (Fig. 2.3). The intrusive suites are located near or at assemblage/formation/flow contacts (Fig. 2.3) and generally have sharp contacts, being the result of the intrusive emplacement or of later structural repositioning (Figs. 2.4A and
2.4B). An exception to these characteristics is the Mt. Logano porphyry of the TIS-other and the entire CIS, which are both large composite intrusive bodies instead of a cluster of distinct intrusions. 28
The intrusions are dominantly porphyritic and typically contain subeuhedral and lesser anhedral plagioclase feldspar (albite) and quartz (typically strained) phenocrysts, with lesser orthoclase, apatite, tourmaline, pyrite, pyrrhotite, chalcopyrite and bornite supported in a massive, fine-grainedgroundmas s (Figs. 2.4C and 2.4D). Individual phenocrysts range from l-15mm in size. Some intrusive suites also include individual intrusions that display interlocking, equigranular textures (HIS and GIS; Fig. 2.4E).
Centimetre-scale xenoliths are present in most intrusions and internal breccias, often tourmaline rich, occur, but are relatively rare (Fig. 2.4F).
The intrusions have lower to middle greenschist facies metamorphic assemblages
(chlorite, biotite, stilpnomelene and muscovite) accompanied by hydrothermal alteration assemblages. Sericite alteration of feldspar crystals is the most common alteration type, with feldspar phenocrysts ranging from fresh to completely obliterated depending on the degree of alteration (Figs. 2.4G & 2.4H). More intense sericite alteration is coupled with pervasive calcium-carbonate alteration (Fig. 2.41). Patchy iron-carbonate (ankerite) alteration, pervasive pink hematite alteration, strongly pervasive silicification, pervasive chlorite and weak, pervasive leucoxene alteration are all present locally within individual intrusions.
Although the intensity of deformation varies amongst intrusions of the different intrusive suites, all intrusions typically display two structural fabrics (Figs. 2.41 and 2.4J).
These two structural fabrics are subparallel, generally east-west trending, near vertical, millimetre-spaced cleavages (Figs. 2.41 and 2.4J; D2 and D3; Bateman et al. 2005, 2008).
A younger, near vertical, foliation is also present in some intrusions (D6; Bateman et al.
2005, 2008), as is a younger flat-lying foliation and conjugate sets of centimetre-sized, kink folds (D7; Bateman et al. 2005, 2008). 29
Multiple sets of veins cross-cut the different intrusive suites including quartz, quartz- tourmaline (Fig. 2.4K), quartz-ankerite and quartz-calcite. Smaller stringer veinlets of tourmaline also occur within some of the intrusions. Sulphide minerals are common in all suites and generally range from sub-millimetre to centimetre scale typically sub- euhedral disseminated grains, clusters, or clots (Fig. 2.4L) and/or veinlets.
The majority of Timmins porphyry intrusive suite intrusions were emplaced between
2687-2691 Ma (Corfu et al. 1989; Marmont and Corfu 1989; Ayer et al. 2002b, 2003;
MacDonald et al. 2005). Exceptions include the Hoyle Pond (TIS-other: 2684 ± 1.9 and
2687.2 ± 2.2 Ma: Bateman et al. 2005; Ayer et al. 2005), and Aquarius intrusions (TIS- other: 2705 ± 10 Ma: Corfu et al. 1989). The GIS was emplaced at 2677.5 ± 2.0 Ma: based on U-Pb zircon age (MacDonald et al. 2005; Ayer et al. 2005). The CIS and HIS have no U-Pb zircon ages, but are hypothesized to be younger than the TIS due to the lack of a D2 fabric, with an emplacement age estimated to be 2685-2665 Ma, which would correlate with other intrusions of the Abitibi subprovince outside of the Porcupine gold camp (Corfu et al. 1989; Ayer et al. 2002a).
Anomalous gold (>0.05 ppm) is associated with all of the intrusive suites. Intense sericite and calcium-carbonate alteration dominates in the vicinity of large tonnage gold mineralization (Hollinger, Mclntyre and Dome deposits) and moderately intense ankerite-sericite alteration is the dominant alteration in the vicinity of smaller deposits
(Paymaster 2-3, Buffalo Ankerite, Holmer and Aquarius). Anomalous copper (greater than 1000 ppm) is associated with hematite alteration in the larger intrusions (the Pearl
Lake porphyry/TIS-main, the Bristol Township porphyry/TIS-other and the Can-
Township porphyry/CIS). 30
2.4.2 Geological Attributes of the Felsic Volcanic Suite
The felsic volcanic suite (FVS) includes intermediate to felsic metavolcaniclastic rocks from both the Porcupine and Deloro Assemblages. The Krist Formation lies unconformably above the Tisdale Assemblage forming the base of the Porcupine
Assemblage, and felsic volcanic rocks near the top of the Deloro Assemblage south of the
PDDZ are included in this suite (Figs. 2.2 and 2.3).
The rocks of the FVS are conglomeratic volcaniclastic packages composed of varying amounts of granule (lapilli)- through pebble (breccia)-sized clasts of felsic material along with lesser mafic and massive sulphide (pyrite and lesser chalcopyrite) clasts, within a quartzo-feldspathic lapilli-tuff matrix (Figs. 2.4M and 2.4N). Metamorphism, alteration, deformation and veining of the FVS is similar to that described above for the rocks of the
Porcupine intrusive suites.
Multiple U-Pb zircon ages fromth e Krist Formation have yielded similar magmatic ages ranging from 2687.3 ±1.6 Ma to 2687.5 ±1.3 Ma (Ayer et al. 2002b). The felsic volcanic rocks from the top of the Deloro Assemblage (albeit not in the immediate vicinity of this research) have been dated at 2725 ±1 Ma (Corfu and Noble 1992).
2.5 Lithogeochemistry
2.5.1 Previous Geochemical Studies
There is little published lithogeochemical data for the porphyries in the Porcupine gold camp. Previous work by Davies and Luhta (1978), Mason and Melnik (1986),
Wood et al. (1986), Burrows and Spooner (1986, 1989), Burrows et al. (1993), Brisbin
(2000) and Gray and Hutchinson (2001) concentrated on the gold mineralization, but few discussed the lithogeochemistry of the intermediate to felsic porphyry intrusions.
McAuley (1983) studied the intrusions in the vicinity of the Dome Mine and found that 31 they were of calc-alkaline affinity and that immobile oxide geochemistry indicated that the Preston, Preston West and Paymaster porphyries were all genetically related and from the same magma source. McAuley (1983) also noted K-Rb enrichment coupled with Sr depletion in sericite altered samples and Sr enrichment with Ca, Fe and Mg depletions in albite-altered samples. Gorman et al. (1981) suggested that the alteration of the intrusions began as sodic (Na) and evolved into potassic (K) alteration. McAuley's
(1983) findings contrasted this as he noted that sericite alteration preceded or occurred coeval with regional deformation and that albite alteration post-dated it. Internal studies by Placer Dome (Wells, 2001) investigated whether the mineralogical variations between quartz-feldspar and feldspar porphyries in the vicinity of the Dome mine were related to separate intrusive events, but found that both were derived from the same magma.
2.5.2 Sampling and Analytical Procedures
Samples of the Porcupine intrusive and felsic volcanic suites were collected from surface exposures and drill core in 2003 and 2004. Twenty eight separate intrusive bodies and three separate felsic volcanic units were sampled for a total of 116 samples.
Each individual sample was approximately 3-5 kg. Weathered surfaces were removed and all samples were then crushed using a steel jaw crusher. Pulverization was done using an agate mortar in 2003 at the Ontario Geoscience Laboratory (GeoLabs) in
Sudbury, Ontario and a mild (carbon) steel in 2004 at Activation Laboratories Limited
(ActLabs) in Ancaster, Ontario. These powders were then analyzed utilizing wavelength- dispersive X-ray fluorescence spectrometry (XRF), inductively-coupled plasma atomic emission spectroscopy (ICP-ES) and inductively-coupled plasma mass spectrometry
(ICP-MS) at a combination of GeoLabs and ActLabs in 2003 and 2004. Major elements
(Si02, Ti02, Al203, Fe203T, MnO, MgO, CaO, Na20, K20 and P205) were determined 32 on fused disc XRF. Loss-on-ignition (LOI) was determined using conventional heating and weight difference methods. Some trace elements were determined by pressed pellet
XRF analysis at the GeoLabs in 2003 (Nb, Zr and Y) and ActLabs in 2004 (Ni, Cr, V,
Nb, Zr and Y). Other trace elements were determined by ICP-ES (Ba, Be, Cd, Co, Cr,
Cu, Li, Mo, Ni, S, Sc, Sr, V, W and Zn) and ICP-MS (Nb, Ta, Zr, Hf, Y, Cs, Th, U, La,
Ce, Pr, Rb, Nd, Sm, Eu, Gd, Tb, Dy, Ho, Er, Tm, Yb and Lu) at the GeoLabs in 2003 and
2004 utilizing closed-beaker multi-acid digestion prior to analysis (Burnham et al. 2002;
Burnham and Schweyer 2004; Tomlinson et al. 1998, 1999). Analytical results are presented in Table 2.3.
Completeness of digestion during ICP-ES and ICP-MS analysis was tested by comparing duplicate elements (Ni, Cr, V, Nb, Zr and Y) with the solid-source XRF method, which does not involve digestion. Values obtained by XRF are within 10% of values obtained by ICP-ES and ICP-MS, suggesting that the digestions were complete.
As such, ICP-ES (Ni, Cr and V) and ICP-MS (Nb, Zr and Y) trace element data are used in this thesis for consistency in the dataset and because of the superior detection limits and sensitivity.
Precision was calculated using the per cent of relative standard deviation (%RSD) of replicate analysis of known and unknown reference materials as well as analytical duplicates. Precision for major elements (including LOI) obtained via fused disc XRF methods is less than ±5% RSD with the exception of MgO and P205 (±7% RSD and
±10% RSD, respectively) from 2003 GeoLabs' analyses and K20 (±10% RSD) from 2004 ActLabs analyses. Precision for trace elements obtained via pressed pellet XRF were less than ±10%RSD for both 2003 and 2004 analyses at GeoLabs and ActLabs.
Precision for trace elements obtained via ICP-ES were generally less than ±15%RSD 33 with the exception of Cd, Mo, S and W which are not considered precise. Precision for trace and rare-earth elements obtained via ICP-MS were less than ±12%RSD. For more detailed information regarding the precision of the dataset used in this thesis refer to
Appendix A of MacDonald et al. (2005).
Accuracy was determined using the per cent of relative deviation (%RD) of reference materials of known or accepted values. Accuracy for major elements (including LOI) obtained via fused disc XRF methods and trace elements obtained from pressed pellet
XRF is generally less than ±10%RD from both 2003 GeoLabs and 2004 ActLabs analyses. Accuracy for trace elements obtained via ICP-ES and ICP-MS were generally acceptable (less than ±10% RD) with the exception of Cd, Mo, S and W, which are not considered accurate. For more detailed information regarding the accuracy of the dataset used in this thesis refer to Appendix A in MacDonald et al. (2005).
2.5.3 Alteration Geochemistry of the Porcupine Intrusive and Felsic Volcanic Suites
Every attempt was made to minimize the effects of alteration in the dataset, but as discussed above, most, if not all of the units studied showed some degree of alteration.
Samples from all of the Porcupine intrusive suites plot both within and outside of the least-altered field on an alteration box plot (Fig. 2.5A; Large et al. 2001). TIS samples show the most variability with some of both the TIS-main camp and TIS-other samples plotting towards albite alteration and many other TIS-main camp samples also plotting towards chlorite-pyrite alteration. Similar to that observed on the alteration box plot, many samples from all of the Porcupine intrusive suites show primary igneous trends on both a modified Spitz and Darling plot (Fig. 2.5B; Spitz and Darling 1978) and a Hughes plot (Fig. 2.5C; Hughes 1973); many samples from the Porcupine intrusive suites do not plot in the primary igneous spectrum, however. Many of these samples have Na20 34 values above 5 wt% indicating Na-alteration (Fig. 2.5B) replicated on the Hughes plot
(Hughes 1973) with samples plotting in the Na-metasomatism field (Fig. 2.5C). The remaining non-primary igneous plotting samples, entirely of the TIS-main camp grouping, also display Na20 values below 2 wt% and Al203/Na20 greater then 10 indicating Na-loss (Fig. 2.5B) replicated on the Hughes plot (Hughes 1973) with samples plotting in the K-metasomatism field (Fig. 2.5C). Na20 and K2O are inversely proportional (Fig. 2.5D) directly related to sericite alteration and replacement of albite within the Porcupine intrusive suites. The trace element Rb, which is also a substitute for
K within sericite, highlights this relationship showing proportion gains with increasing
K20 (Fig. 2.5E) and decreasing Na20 (Fig. 2.5F). 2.5.4 Lithogeochemistry of the Porcupine Intrusive and Felsic Volcanic Suites
Although alteration of the Porcupine intrusive and felsic volcanic suites have affected their mobile element geochemistry, elements such as AI2O3, TiC>2, Zr, Y, Nb, La, Yb, Ta,
Sc and rare-earth elements (REE), have largely remained immobile with their primary abundances unaffected by alteration (see Appendix B). As such, petrologic discussions will focus on the immobile element systematics of these elements. Other, less reliable elements are used as well, but only where they will not drastically affect petrogenetic interpretations and/or are supported by immobile element trends.
2.5.4.1 Lithogeochemistry of the Timmins Porphyry Intrusive Suite (TIS)
The TIS is dominantly composed of subalkaline (~Nb/Y < 0.7; Fig. 2.6A) dacite to rhyodacite (~Zr/Ti02 = 0.03-0.1; Fig. 2.6A; Winchester and Floyd 1977), with the exception of the Homestead porphyry which has alkaline affinities with Nb/Y>1.0
(Winchester and Floyd 1977; Pearce 1996). CIPW normative mineral calculation plots indicate the intrusions of the TIS are albitic with tonalite-trondhjemite-granodiorite 35
(TTG) compositions (Fig. 2.6B; O'Connor 1965) and although Na20 and K2O mobility
(see alteration discussion above) have modified these normative mineral calculations towards orthoclase, the least altered samples display TTG compositions that are consistent with observed mineralogy. La/Yb and Zr/Y ratios (>6 and >7, respectively) indicate the TIS is of cale-alkaline affinity (Figs. 2.6C and 2.6D; MacLean and Barrett
1993; Barrett and MacLean 1999). Zr and Y abundances further suggest the TIS samples have Fl-type affinities (Fig. 2.6D; Lesher et al. 1986) and AI2O3 abundances (>14.5 wt%) suggest the TIS are dominantly high-aluminum (high-Al) TTG, excluding the Hoyle
Pond and Homestead porphyries which are low-aluminum (low-Al) TTG intrusives (Fig.
2.6E; Arth 1979). Concentrations of Si02 (>56 wt%), A1203 (>15 wt%), MgO (<3 wt%), Y (<18 ppm) and Yb ( 1990; Castillo et al. 1999). Primitive mantle- and chondrite-normalized multi-element plots for the TIS are characterized by steep patterns with light REE (LREE)-enrichment and heavy-REE (HREE) depletion coupled with negative Nb and Ti anomalies and positive Zr, Hf and Al anomalies (Figs. 2.8A, 2.8B, 2.8C and 2.8D). Nb-Y and Ta-Yb plots suggest the TIS are related to volcanic and/or primitive arc magmatism (I-type; Figs. 2.9A and 2.9B; Pearce et al. 1984). Upper continental crust normalized (UCCn) La/Sm ratios (~1; Fig. 2.9C; McLennan 2001) suggest the source magmas for the TIS are at least partially upper crustal in nature and Sc/Y ratios -0.5 to 1.0 are consistent with generation at depth in the garnet-hornblende stability field (Fig. 2.9D; Feng and Kerrich 1992). 36 2.5.4.2 Lithogeochemistry of the Carr Township Porphyry Intrusive Suite (CIS) The CIS is composed of subalkaline (~Nb/Y < 0.7; Fig. 2.6A), dacite to rhyodacite (~Zr/Ti02= 0.03-0.1; Fig. 2.6A; Winchester and Floyd 1977). CIPW normative mineral calculations indicate the intrusions are of granitic to trondhjemitic composition (Fig. 2.6B; O'Connor 1965) and although NajO and K2O mobility could have modified these calculations the CIS is relatively unaltered (see Figs. 2.5A to 2.5C). La/Yb and Zr/Y ratios (>6 and >7, respectively) indicate the CIS is of calc-alkaline affinity (Figs. 2.6C and 2.6D; MacLean and Barrett 1993; Barrett and MacLean 1999). Zr and Y abundances further suggest the CIS has anFI-type affinity (Fig. 2.6D; Lesher et al. 1986) and AI2O3 abundances (>14.5 wt%) suggest the CIS is similar to high-Al TTG (Fig. 2.6E; Arth 1979). Concentrations of Si02 (>56 wt%), A1203 (>15 wt%), MgO (<3 wt%), Y (<18 ppm) and Yb (<1.9 ppm) as well as Sr/Y ratios indicate the CIS have adakite-like lithogeochemical affinities (Figs. 2.7A to 2.7E; Defant and Drummond 1990; Castillo et al. 1999). Primitive mantle- and chondrite-normalized multi-element plots for the CIS are characterized by slightly flatter patterns compared to those of the TIS (Figs. 2.8E and 2.8F). The CIS display weak LREE enrichment and slight HREE depletion coupled with weakly negative Nb and Ti anomalies and very weakly positive Zr, Hf and Al anomalies (Figs. 2.8E and 2.8F). Nb-Y and Ta-Yb plots suggest the CIS are related to volcanic and/or primitive arc magmatism (I-type; Figs. 2.9A and 2.9B; Pearce et al. 1984). Upper continental crust-normalized La/Sm ratios (~1; Fig. 2.9C; McLennan 2001) suggest the source magmas for the CIS had upper crustal influence and Sc/Y ratios ~0.3 to 0.7 are consistent with hornblende being present in the residue during crustal partial melting (Fig. 2.9D; Feng and Kerrich 1992). 37 2.5.4.3 Lithogeochemistry of the Holmer Intrusive Suite (HIS) The HIS is composed of subalkaline (~Nb/Y < 0.7; Fig. 2.6A), dacitic to rhyolitic magmas (-Zr/TiCh = 0.03-0.11; Fig. 2.6A; Winchester and Floyd 1977). CIPW normative plots indicate trondhjemite compositions (Fig. 2.6B; O'Connor 1965), although Na20 alteration have modified these calculations towards more albite-rich affinities (see Figs. 2.5A to 2.5C). The Thunder Creek porphyry is an exception to the above and has a granitic composition (Fig. 2.6B; O'Connor 1965). La/Yb and Zr/Y ratios (>6 and >7, respectively) indicate the HIS is of calc-alkaline affinity (Figs. 2.6C and 2.6D; MacLean and Barrett 1993; Barrett and MacLean 1999). The HIS have A1203 abundances >14.5 wt% suggesting they are high-Al TTG (Fig. 2.6E; Arth 1979). Primitive mantle- and chondrite-normalized multi-element plots for the HIS are characterized by three distinct profiles. The first HIS profile includes some of the samples from the Holmer porphyry as well as the samples from the Southwest Bristol syenite, and is characterized by a relatively steep pattern with both LREE and HREE enrichment compared to the TIS. This first HIS profile has negative Nb and Ti anomalies and does not have any positive anomalies (Figs. 2.8G and 2.8H). The second HIS profile is very similar to the first with a relatively steep profile but with proportionally decreased REE abundances, along with weak negative Nb and Ti anomalies and positive Zr, Hf and Al anomalies (Figs. 2.8G and 2.8H). The third HIS profile includes the sample of the Thunder Creek porphyry, and is characterized by a flat pattern with slight depletion of all REE compared to the TIS (Figs. 2.8G and 2.8H). This third HIS profile has atypical LREE (e.g. La, Ce and Pr) values in comparison to the TIS (slightly depleted), strong negative Ti, V and Sc anomalies and strong positive Zr, Hf and Al anomalies (Figs. 2.8G and 2.8H). The range in REE profiles for the HIS can be explained alteration as REE 38 depletions correlates well with Na-alteration and N2O mass gains (see Appendix B). Nb- Y and Ta-Yb plots suggest the HIS are related to volcanic and/or primitive arc magmatism (I-type; Figs. 2.9A and 2.9B; Pearce et al. 1984) although some samples lie near the arc field boundary with the non-arc fields. Upper crust normalized La/Sm ratios (-1; Fig. 2.9C; McLennan 2001) suggest the source magmas for the HIS were at least partially upper crustal, excluding the Holmer porphyry and Southwest Bristol syenite that have upper crust normalized La/Sm ratios <1, suggesting derivation from partial melting of a mafic source. Sc/Y ratios -0.1 to 0.4 are consistent with clinopyroxene and hornblende in the residue during crustal partial melting (Fig. 2.9D; Feng and Kerrich 1992). Less clinopyroxene in the source may also explain the flatter REE profile for the Thunder Creek porphyry in comparison to the rest of the HIS (Fig. 2.8G and 2.8H: Feng and Kerrich 1992). 2.5.4.4 Lithogeochemistry of the Granodiorite Intrusive Suite (GIS) The GIS is dominantly composed of subalkaline to weakly alkaline rocks (~Nb/Y = 0.7-1.0; Fig. 2.6A), with dacitic to rhyodacitic compositions (~Zr/TiC<2= 0.03-0.1; Fig. 2.6A; Winchester and Floyd 1977). They have CIPW normative mineral compositions consistent with trondhjemite (Fig. 2.6B; O'Connor 1965), although Na20 mobility (see alteration discussion above) may have modified the GIS samples to appear more albitic. La/Yb and Zr/Y ratios (>6 and >7, respectively) indicate the GIS has a calc-alkaline affinity (Figs. 2.6C and 2.6D; MacLean and Barrett 1993; Barrett and MacLean 1999). Zr and Y abundances within the GIS suggest the samples have Fl-type affinities (Fig. 2.6D; Lesher et al. 1986), although some have high Zr/Y ratios and plot above the FI- type rhyolite field. AI2O3 abundances (-14.5 wt%) suggest the GIS are borderline high- Al TTG (Fig. 2.6E; Arth 1979). Concentrations of SiQ2 (>56 wt%), A1203 (>15 wt%), 39 MgO (<3 wt%X Y (<18 ppm) and Yb (<1.9 ppm) as well as ratios of Sr/Y and La/Yb indicate the GIS has adakite-like lithogeochemical affinities (Figs. 2.7A to 2.7F; Defant and Drummond 1990; Castillo et al. 1999). Primitive mantle- and chondrite-normalized multi-element plots for the GIS are characterized by very steep patterns with strong LREE-enriehmentand strong HREE depletion coupled with negative Nb, Sm and Ti anomalies and positive Al anomalies (Figs. 2.81 and 2.8J). Nb-Y and Ta-Yb plots suggest the GIS are related to volcanic and/or primitive arc magmatism (I-type; Figs. 2.9A and 2.9B; Pearce et al. 1984). Upper continental crust normalized (UCC„) La/Sm ratios (~1; Fig. 2.9C; McLennan 2001) suggest the source magmas for the GIS were at least partially influenced by the upper crustal material and Sc/Y ratios -0.5 to 1.0 are consistent with garnet-hornblende in the residue during crustal partial melting (Fig. 2.9D; Feng and Kerrich 1992). 2.5.4.5 Lithogeochemistry of the Felsic Volcanic Suite (FVS) The felsic volcanic suite is composed of two separate members: the Krist Formation and the Deloro Assemblage. Krist Formation samples are dominantly subalkaline (~Nb/Y < 0.7; Fig. 2.6A) with dacite to rhyodacite lithogeochemistries (~ZT/TI02= 0.03- 0.1; Fig. 2.6A; Winchester and Floyd 1977). The Deloro Assemblage sample from the FVS is composed of alkaline (~Nb/Y > 0.7; Fig. 2.6A) dacite to rhyodacite (~Zr/Ti02= 0.03-0.1; Fig. 2.6A; Winchester and Floyd 1977; Pearce 1996). CIPW normative mineral calculation plots indicate the FVS is albitic with tonalite-trondhjemite-granodiorite (TTG) compositions (Fig. 2.6B; O'Connor 1965) and although Na20 and K2O mobility (see alteration discussion above) have modified these mineral calculations the results are consistent with observed mineralogy. La/Yb and Zr/Y ratios (>6 and >7, respectively) indicate the FVS is calc-alkaline (Figs. 2.6C and2.6D; MacLean and Barrett 1993; 40 Barrett and MacLean 1999). Zr and Y abundances further suggest the Krist Formation and Deloro Assemblage samples are Fl-type rhyolites (Fig. 2.6D; Lesher et al. 1986), although the Deloro Assemblage sample has very high Zr/Y ratios and above the Fl-type rhyolite field. AI2O3 abundances (>14.5 wt%) suggest the FVS are high-Al TTG (Fig. 2.6E; Arth 1979). The FVS has adakite-like lithogeochemieal affinities indicated by concentrations of Si02 (>56 wt%), AI2O3 (>15 wt%), MgO (<3 wt%), Y (<18 ppm) and Yb (<1.9 ppm) as well as ratios of Sr/Y and La/Yb (Figs. 2.7A to 2.7F: Defant and Drummond 1990; Castillo etal. 1999). Primitive mantle-and chondrite-normalized multi-element plots for the Krist Formation samples of the FVS are characterized by steep patterns with LREE enrichment and HREE depletion coupled with negative Nb and Ti anomalies and positive Zr, Hf, Yb, La and Al anomalies (Figs. 2.8K and 2.8L). Primitive mantle- and chondrite-normalized multi-element plots for the Deloro Assemblage sample of the FVS is also characterized by steep patterns with light REE (LREE) enrichment and strong heavy-REE (HREE) depletion coupled with a negative Nb anomaly and positive Zr, Hf, and Al anomalies (Figs. 2.8K and 2.8L). Nb versus Y and Ta versus Yb plots suggest the FVS are related to volcanic and/or primitive arc magmatism (I-type; Figs. 2.9A and 2.9B; Pearce et al. 1984). Upper continental crust normalized (UCC„) La/Sm ratios (~1; Fig. 2.9C; McLennan 2001) suggest the source magmas for the FVS were at least partially influenced by upper crust and Sc/Y ratios -0.5 to 1.0 are consistent with garnet-hornblende in the residue during partial melting (Fig. 2.9D; Feng and Kerrich 1992). 41 2.6 Discussion 2.6.1 Pedogenesis of the Porcupine Intrusive Suites All of the Porcupine intrusive suites display broadly similar geochemical signatures with minor, yet significant, differences that indicate distinct petrogenetic histories. The TIS has high-Al TTG and adakite-like lithogeochemical affinities (Figs. 2.6B, 2.6E and 2.7). Two main models have been proposed to explain the genesis of TTG suites in modern and ancient settings: 1) slab-melting of subducted oceanic crust; and/or 2) the delamination and melting of stacked and thickened mafic crust (Drummond and Defant 1990; Drummond et al. 1996; Martin 1999; Smithies 2000; Jackson et al. 2005; Martin et al. 2005; Bedard 2006; Jiang et al. 2007; Wang et al. 2007; Piercey et al. 2008; Wyman and Kerrich 2009). The presence of continental crustal influence in the TIS TTG suite rocks (La/SmuccN ~1; Fig. 2.9C) does impart some ambiguity as to which of the above models best explains the TIS suite TTG genesis. In the case of the slab melt model, workers have suggested that slab-melts would likely react with the mantle leading to enrichments in MgO, Cr, and Ni in associated TTG/adakites (e.g., Defant and Drummond 1990; Rapp et al. 1999; Martin et al. 2005; Bedard 2006; Richards and Kerrich 2007). The TIS suite rocks, however, have MgO, Cr, and Ni concentrations that are too low to support slab melt/mantle wedge interactions (Rapp et al. 1999; Martin et al. 2005; Bedard 2006; Richards and Kerrich 2007). The melting of mafic crust associated with delamination of stacked and thickened basaltic crust does not implicate mantle interaction in TIS magma generation and fits well in explaining the TIS suite lithogeochemistry and the geological evolution of the Timmins region. The syntectonic nature and coincidence of TIS suite porphyries with Dl compressional deformation at -2690 Ma (Fig. 2.10: Bateman et al. 2008) suggests that crustal thickening was important in the generation of 42 the TIS suite magmas. It is also possible that flat slab subduction might have been important in inducing crustal thickening and delamination and ultimately leading to TIS suite TTG genesis (e.g., Martin et al. 2005; Gutscher et al. 2000). For example, Gutscher et al. (2000) proposed that prolonged flat subduction could cause the elimination of a mantle wedge between the subducted slab and overriding crust (Martin et al. 2005). Structural underplating would also cause significant crustal thickening which could lead to delamination and lower crustal melting and thus form the TTG suite magmatism. Broadly similar thickening and delamination models have been proposed for Mesozoic TTG/adakite-like rocks in northern and central China (Wang et al. 2007b; Jiang et al. 2007). The CIS is similar to TIS in that the CIS has high-Al TTG and adakite affinities, but differs from the TIS in that the CIS has granitic to trondhjemitic affinities and was likely formed via partial melting of mafic crust at shallower levels in the crust (e.g., Feng and Kerrich 1992; Wyllie et al. 1997; Moyen and Stevens 2006; Piercey et al. 2008). The CIS does have broadly similar trace element compositions to TIS, but they are characterized by lower La/Yb, consistent with garnet not being in the residue during melting, suggesting that they formed at shallower depths (<40 kilometers; Rapp et al. 1991; Wyllie et al. 1997; Moyen and Stevens 2006; Richards and Kerrich 2007; Piercey et al. 2008). The timing of CIS TTG genesis is post-D2 crustal thickening (-2690-2680 Ma: Fig. 2.10) and coincides with post-D2 regional extension (-2685-2670 Ma: Fig. 2.10: Bateman et al. 2008). It is likely the initial crustal thickening produced sufficient heat to general crustal melting and coupled with extensional activity permitted genesis and emplacement of the CIS at higher crustal levels. 43 The GIS has geochemical features like the TIS and CIS, but has steeper REE patterns and more fractionated HREE consistent with derivation at greater depth than the TIS and CIS <>40 kilometers: Wyllie et al. 1997; Moyen and Stevens 2006; Piercey et al. 2008). This is noted by the much steeper REE profile of the GIS in comparison to the TIS (Fig. 2.81). In relation to the evolution of the crust in the immediate vicinity of Timmins, significant crustal thickening can be implicated between -2690 Ma (age of emplacement for the TIS) and -2677 Ma (age of emplacement for the GIS) via thrust fault stacking during D2, based on that both the TIS and GIS intruded in the immediate vicinity of each other and that lower crustal melting that generated the TIS was significantly shallower then the GIS just over 10 m.y. earlier (Fig. 2.10: Bateman et al. 2008). The HIS has high-Al TTG affinities like the TIS and CIS, but contains lower Si02, higher MgO, Y, and Yb and are more akin to sanukitoid magmatism (Shirey and Hanson 1984; Moyen et al. 2001; Moyen et al. 2003; Martin et al. 2005). This is further supported by higher Ti, Nb and Zr concentrations compared to typical TTG/adakite concentrations (Martin et al. 2005). While the TIS, CIS and GIS are consistent with generation from melting of thickened crust, the HIS sanukitoid suite likely due to remelting of slab-melt altered mantle lithosphere and would be further supported by their non-arc geochemical signatures and trace element signatures that differ from the UCC- like signatures present in the CIS and TIS (Figs. 2.9A, 2.9B and 2.9C: Martin et al. 2005). The HIS are not primary sanukitoid magmas, however, due to their lower values of MgO, Cr and Ni abundances compared to more primitive sanukitoid magmas, which may be the result of magmatic fractionation(Beakhous e 2001). The Sc/Y ratios in the HIS magmas suggest that hornblende and clinopyroxene were present in the residue during partial melting (Fig. 2.9D; Feng and Kerrich 1992), consistent with formation at 44 relatively shallow depths (<40 Mlometers; Wyllie et al. 1997; Moyen and Stevens 2006; Piercey et al. 2008), likely associated late- to post-tectonic extension at 2675-2665 Ma (Fig. 2.10: Bateman et al. 2008). In summary, the Porcupine intrusive suites are predominantly related to lower crustal melting of mafic crust at varying depths, excluding the HIS that originated from fractionated partial melts of slab melt altered mantle. Depths of mafic lower crustal melts in descending order are the CIS (>40 kilometres), TIS (<40 kilometers) and GIS (<40 kilometers). The porcupine intrusive suites also span the entire deformation of the Porcupine gold camp from the TIS being coeval with Dl, to the CIS and GIS being post- D2/pre-D3 and the HIS being late- to post-tectonic (Fig. 2.10). 2.6.2 Pedogenesis of the Felsic Volcanic Suite (FVS) The felsic volcanic suite is composed of two members: the Krist Formation and the Deloro Assemblage, each with distinct lithogeochemical identities. The Krist Formation has identical petrography, lithogeochemistry and ages to the TIS, suggesting that the Krist Formation is the extrusive equivalent to the TIS and as such, the TIS should be included as an intrusive member of the Porcupine Assemblage with the Krist Formation. Geochemical inconsistencies for the Deloro Assemblage sample compared to historical work (the sample plots as being highly alkaline when all historical work suggests it should plot as subalkaline; Ayer et al. 2002a) and a limited data set included within this thesis (i.e. only one sample) suggest a high likelihood of error when compared to historical results. As such, it will not be further discussed herein. 45 2.63 Relationship of Volcanism to the Emplacement of the Porcupine Intrusive Suites The TIS is the only intrusive suite with coeval volcanic rocks. The Krist Formation member of the FVS displays geographical, petrographical, geochronological attributes identical to the TIS (Ayer et al., 2003), as well as a similar lithogeochemical and petrogenetic history suggest that they are coeval and cogenetic. It should be noted that although the TIS and Krist Formation are magmatically related, no parent vent, vents, or conduit systems that link the two physically have been documented. There is evidence, however, that the TIS was emplaced at shallow depths not far removed from the eruptive centers that extruded the Krist formation. Evidence including the very fine grained matrix in the TIS imply quick cooling at potentially high crustal levels alluding to the TIS being near surface, subvolcanic intrusives as previous suggested by Mason and Melnik (1986a). The shallow emplacement of the TIS is further supported by flow-banded breccias observed in the Paymaster Porphyry which suggest that it may represent shallow, subvolcanic cryptodomes (Pyke 1982; Williams and McBiraey 1979; Cas et al. 1990). This evidence thus suggests that the TIS may represent the subvolcanic roots of fissures and vents that extruded the Krist Formation, but whose surface expression has been eroded. 2.6.4 Geological Differences between Gold Mineralized and Barren Intrusions All Porcupine intrusive suites display a spatial association with gold mineralization. There are lithogeochemical differences, however, between deposits associated with the largest gold systems and less productive systems. For example, the largest gold systems in the Porcupine gold camp (having produced >10 million ounces of gold), including the Hollinger, Mclntyre and Dome mines are only spatially associated with the TIS (Brisbin 46 2000). Similarly, moderate sized gold systems (produced or indicated gold reserves >1 million ounces) including the Coniaurium, Preston, Paymaster, Buffalo Ankerite, Hoyle Pond and Aquarius mines, and small gold systems (produced or indicated gold reserves <1 million ounces) including the Vipond, Moneta, Crown, Gillies Lake and Fuller (Vedron) mines are also associated with TIS (Brisbin, 2000; Cochrane 2006). The exceptions to this are the moderate sized Holmer mine (905, 000 indicated ounces of gold), which is spatially associated with the HIS (Darling et al. 2007), and the small Naybob mine (50, 733 ounces of gold produced), which is associated with the GIS (Brisbin 2000). The only barren intrusions in the TIS are those south of the PDDZ, and, for the most part, the GIS and CIS are not associated with significant Au accumulations. This suggests that the TIS is the most prospective suite of the Porcupine intrusive suites followed by the HIS, GIS and CIS in decreasing order of potential, in particular, those porphyries must also be north of the PDDZ. Alteration geochemistry appears to be useful in distinguishing gold mineralized versus barren intrusions. Samples associated with the large gold systems in the Porcupine gold camp (only TIS as discussed above) preferentially plot to the right side of the alteration box plot (Fig. 2.5A) and display Na-loss and K-metasomatism (Figs. 2.5B-C). In contrast, intrusions related to moderate sized gold systems, including the HIS, preferentially plot in the least altered fields or have experienced Na-metasomatism (Figs. 2.5A-C). Similarly, intrusions associated with small gold systems and anomalous mineralization, as well as barren intrusions, preferentially plot in the least altered field with some samples exhibiting Na-alteration (Figs. 2.5A-C). In general, there appears to be enhanced K-metasomatism associated with Au-rich intrusions, whereas less productive intrusions have Na-metasomatism or are relatively fresh. 47 Petrography generally correlates with the alteration geochemical trends. Large gold systems display an association with sulphidized (pyrite ± pyrrhotite ± chalcopyrite), strongly sericite-calcium carbonate altered intrusions. Moderate sized gold systems range from strong to weak sericite alteration coupled with moderate Fe-carbonate alteration. Small gold systems and barren associated intrusions generally appear unaltered. 2.6.5 The Relationship of the Porcupine Intrusive Suites to Gold Mineralization An important question concerning intrusive magmatism within the Porcupine gold camp is why so many of the gold deposits occurred proximal to Porcupine intrusive suites regardless of what intrusive suite they are part of. Previous workers have suggested that there is a genetic link between the Porcupine intrusive suite and gold mineralization, whereas others have suggested that there is a structural relationship, and others suggest a purely coincidental relationship (Davies and Luhta 1978; Mason and Melnik 1986a, 1986b; Burrows et al. 1993; Brisbin 2000; Gray and Hutchinson 2001). The results of this study, and other studies, clearly indicate that gold has no genetic relationship to the Porcupine intrusive suites. Firstly, much of the gold mined within the Porcupine gold camp does not occur directly within the intrusions but rather along the margins of the intrusions in iron-rich mafic volcanic rocks (Gray and Hutchinson 2001). Gold has been, and is still being, mined within the intrusions themselves, but most veins originate and are centered in volcanic rocks peripheral to the intrusions within favorable structural traps (Burrows et al 1993). Secondly, most of the ore veins mined in the camp crosscut a younger intrusive suite (the albitite dikes), which themselves crosscut the Porcupine intrusive suite suggesting a time gap between Porcupine intrusive suite magmatism and gold mineralization (Mason and Melnik 1986a, 1986b; Brisbin 2000). Thirdly, recent Re-Os age dating of molybdenite from both the Mclntyre and Dome ore systems yielded age dates 2670-2672 Ma (Ayer et al. 2003; Bateman et al. 2004), ages which are at least 15 Ma after the emplacement of the Porcupine intrusive suites (2677- 2691 Ma; Corfu et al. 1989; Gray and Hutchinson 1993; Ayer et al. 2003; MacDonald et al. 2005). While no genetic relationship exists between gold mineralization and the Porcupine intrusive suites, why is there a spatial association of porphyries to gold? Two models have been proposed to explain this relationship. The first suggests that Porcupine intrusive suite and subsequent gold systems utilized the same, long-lived and/or reactivated structural conduits for their emplacement (Brisbin 2000); evidence for this is that intrusions and gold have both developed along the same structures including the Hollinger shear zone, the Dome fault and the PDDZ. The fact that most of the intrusions are located along these major deformation zones suggests the Porcupine intrusive suites did utilize the fault zones for their emplacement. Furthermore, the coincidence of gold mineralization within the same fault zones adds support to the notion that intrusions and gold-bearing fluids utilized the same structures (Brisbin 2000). In this scenario the major deformation zones would have remained active for an extended period of time or more likely, were reactivated >15 Ma later. For example, the porphyries were emplaced ca. 2688Ma (Corfu et al. 1989; Ayer et al. 2003) and the gold mineralization occurred ca. 2670-2672 Ma (Ayer et al. 2003; Bateman et al. 2004) during reactivation of the same migration conduits the porphyries utilized. Alternatively, the competency contrast between competent Porcupine intrusive suite and less competent mafic volcanic country rocks could have acted as a locus for deformation (Gorman et al. 1981; Wood et al. 1986; Burrows and Spooner 1989; Burrows et al. 1993). The intrusions may have acted like 49 'pillars' (Wood et aL 1986) within the mafic volcanic rocks and the 'pillars' deflected deformation resulting in high strain and dilation zones around the margins of the intrusions into which the gold bearing fluids migrated (Wood et al. 1986; Burrows and Spooner 1989; Burrows et al. 1993). Furthermore, the reaction of the Au-bearing fluid with Fe-rich Tisdale Assemblage volcanic rocks likely resulted in the destabilization of gold thiocomplexes, allowing Au to be precipitated from solution (Seward 1973; Ropchan et al. 2002; Dinel et al. 2008). Key support for this hypothesis is that the majority of the gold was mined outside of the intrusions along the margins of the intrusive bodies within associated marginal high strain zones and volcanic rocks of the Tisdale Assemblage (Burrows et al. 1993; Brisbin 2000; Bateman et al. 2008). For example, at both the Hollinger-Mclntyre and Dome deposits these relationships are present (Mason and Melnik 1986a, 1986b; Burrows et al. 1993; Brisbin 2000; Gray and Hutchinson 2001). Although both hypotheses work individually, the close spatial association of intrusive magmatism and gold mineralization within the Porcupine camp suggests that both porphyry emplacement and gold mineralization were controlled by regional deformation zones despite significant differences in timing of emplacement. It is proposed that the porphyry intrusions utilized regional faults for emplacement and later during regional deformation the location and competency contrasts of the porphyry bodies in comparison to surrounding lithologies caused the reactivation of the structures creating fluid conduits and dilation zones surrounding the porphyries that were favourable for gold bearing fluid migration and precipitation. It is notable that larger gold deposits within the Porcupine camp (e.g., Hollinger, Mclntyre and Dome) are located where there are multiple intrusions coalescing (e.g., Preston and Paymaster porphyries at Dome), and intrusion coalescence likely caused larger dilation zones during deformation, 50 larger structural traps and thus the ability to contain (and trap) more gold mineralization than in smaller deposits. This coalescing of intrusive rocks near structures may be a potential tool for further exploration in both Timmins and other similar gold camps, globally. 2.6.6 The Relationship of the Porcupine Intrusive Suites to Copper Mineralization The association of copper mineralization to the Porcupine intrusive suites in the Porcupine gold camp has been debated since the discovery of the copper ore zone in the Mclntyre mine. Some workers noted similarities to Phanerozoic porphyry copper deposits and suggested that the Mclntyre copper ore zone may represent an Archean analog (e.g. Pyke and Middleton 1971; Davies and Luhta 1978; Mason and Melnikl986a, 1986b), whereas others have argued against a porphyry Cu-Mo origin (e.g. Wood et al. 1986; Burrows et al. 1993; Richards and Kerrich 2007). There is copper mineralization in the Pearl Lake porphyry of the TIS (Davies and Luhta 1978; Mason and Melnikl986a, 1986b; Wood et al. 1986; Burrows et al. 1993; Richards and Kerrich 2007), in the Bristol Township porphyry of the TIS, and the Carr Township porphyry of the CIS. These intrusions have similarities to younger porphyry copper systems including: host rock chemistry (intermediate to felsic), host rock texture ('porphyritic'), potassic alteration halos surrounding a central ore zone, sulphide mineralogy (chalcopyrite ±bornite), sulphide occurrence (disseminated, clustered and stringers) and mineralized vent breccias. Furthermore, the rocks are geochemically similar to I-type arc granites (Fig. 2.9B: Christiansen et al. 1996) and adakite-like rocks in the case of the TIS, of which, both affinities have been documented to be hosts for Phanerozoic porphyry mineralization (Oyarzun et al. 2001) 51 There are numerous lines of evidence against a porphyry Cu-Au deposit origin, however. One line of opposing evidence is the relatively small size of known porphyry hosted Cu-Au zones in relation to most Phanerozoic porphyry Cu systems. For example, the majority of known, economic grade porphyry ore deposits range from 29 to 1,100 million tonnes (Mt), with a median of 180 Mt (Singer et al. 2002). In contrast the Mclntyre copper ore zone produced approximately 9 Mt at 0.85 % Cu (Mason and Melnik 1986a), far less, and thus smaller, than the majority of known Cu-Au porphyry deposits and also near the upper limits of typical Cu porphyry grades (0.24-0.88% Cu: Singer et al. 2002). Geochronological evidence also argues against a magmatic- hydrothermal origin for the Cu-Mo-Au. In particular, Bateman et al. (2004) reported a Re-Os age on molybdenite from the Cu-Mo-Au zone in the Pearl Lake porphyry of 2672 ±7 Ma, which is interpreted to reflect the age of gold and copper mineralization in the Mclntyre gold system; this age is at least 9 Ma (accounting for the maximum errors in the geochronological ages) younger than the age of emplacement of the Pearl Lake porphyry, which is far longer then would be the expected life of a single hydro-magmatic mineralizing system. This data strongly argue against any role for magmatic- hydrothermal activity in the genesis of the Cu-Mo-Au in the Timmins area. 2.7 Conclusions The main conclusions of this study are: 1. There are four petrogenetic suites of porphyry intrusions along the PDDZ in the Porcupine gold camp. The majority of the intrusions are related to magma generated via crustal thickening related to uplift and extension as a result of flat subduction and underplating of mafic crust, and resultant delamination and partial melting ca. 2690 Ma during Dl deformation at depths <40 kilometers. These Timmins porphyry intrusive suite 52 (TIS) magmas were emplaced near-surface and eruptive equivalents produced the deposition of Krist Formation volcanic rocks. Approximately 10-15 Ma after TIS-Krist Formation two other lower crustal sourced magma suites were generated from mafic source rocks. The Carr Township porphyry intrusive suite (CIS) was generated by lower crustal melting at shallower depths than the TIS, whereas the granodiorite intrusive suite (GIS) was generated at greater depths then the TIS. The time gap between TIS and GIS, the deepening of the source and that the two intrusive suites have intruded within the immediate vicinity of one another, suggests that D2 thrust stacking significantly thickened the crust between 2690-2678 Ma causing the deeper magma generation. The Holmer intrusive suite (HIS), the youngest intrusive suite in the Porcupine camp (2675- 2665 Ma) formed via the partial melting and fractionation of magma sourced from slab- melt altered mantle at depths >40 kilometers. 2. The Krist formation has petrographic, lithogeochemical, petrogenetic and geochronological similarities to the TIS and is interpreted to have a similar petrogenesis via the melting of underplated mafic crust at lower crustal depths <40 kilometers. The Krist is cogenetic with the TIS and the TIS is interpreted to be the near subvolcanic intrusions that fed the pyroclastic volcanism recorded in the Krist Formation. 3. Gold is associated with all of the Porcupine intrusive suites. Large gold systems (>10 million ounces) are only related to the TIS and display strong sulphidation and potassic alteration. Moderate sized gold systems (>1 million ounces) are dominantly associated with the TIS, but also the HIS, and are related geochemically to weak sodium alteration and to weak-moderate potassic and iron-carbonate alteration. Similar to the moderate sized gold systems, small gold systems (<1 million ounces) and anomalous gold showings are associated dominantly with the TIS, but also the GIS, and are related 53 geochemically to weak sodium alteration and petrographical appear relatively unaltered. Barren intrusions (no known historical resources) are geographically controlled either TIS intrusions south of the PDDZ or CIS and GIS intrusions east of the Burrows- Benedict Fault. 4. Gold has no genetic relationships to the Porcupine intrusive suites (i.e., it is not magmatically derived from the Porcupine intrusive suites). The spatial association is related to the Porcupine intrusive suites and gold mineralizing fluids utilizing the same migration conduits (i.e. reactivated regional faults) and that regional deformation created dilation zones along the margins of the intrusions that gold was deposited into as a result of favourable volcanic rock chemistry and hydrodynamic trap. 5. The idea of the TIS, in particular the Pearl Lake porphyry as Archean analogues to Phanerozoic porphyry-copper mineralization is not valid. Although the TIS displays many common features with modern systems, geochronological evidence argues strongly against a porphyry Cu-type origin for the Cu accumulations in the Porcupine Camp. 2.8 References Arth, J.G. 1979. Some trace elements in trondhjemites - their implications to magma genesis and paleotectonic setting; in Barker, F., ed., Trondhjemites, Dacites and Related Rocks: New York, Elsevier Scientific Publishing Co., p. 123-132. Ayer, J.A., Berger, B.R. and Trowell, N.F. 1999. 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Toronto, p.56-80. Wyllie, P.J., Wolf, M.B., and van der Laan, S.R. 1997. Conditions for formation of tonalites and trondhjemites: Magmatic sources and products: Oxford Monographs on Geology and Geophysics, v.35, p.256-266. Wyman, D. and Kerrich, R. 2009. Plume and arc magmatism in the Abitibi subprovince: Implications for the origin of Archean continental lithospheric mantle: Preeambrian Research, v. 168, p.4-22. 60 Figure 2.1. Regional geological map displaying the location of differing Assemblages within the Abitibi greenstone belt in the vicinity of the Porcupine gold camp, Timmins, Canada (modified from Ayer et al. 1999a, 1999b). Map also highlights the Porcupine intrusive suites examined for this study. 61 474080 475000 476000 477000 478000 479000 480000 481000 482000 \//A Deloro Assemblage o Fault —\ Fold - Anticline \ Fold - Syncline ^Z Gold Mine 474000 475000 476000 477000 478000 479000 480000 481000 482000 Figure 2.2. Surface geological map of the Porcupine gold camp showing the location of historically significant producing gold mines and the felsic volcanic suite in relation to some of the Porcupine intrusive suites (specifically TIS - main camp: modified from Ferguson 1968; Brisbin 1997; Ayer et al. 1999a, 1999b; Hall et al. 2003). 62 Timiskaming Assemblage: Dominantly composed of interbedded medium- to coarse-grained siliciclastic metasedimentary rocks. Unconformity Porcupine Assemblage: Beatty Formation Dominantly composed of turdibidic fine- to medium-grained siliciclastic metasedimentary rocks. Krist Formation Dominantly composed of intermediate to felsic conglomeritic volcaniclastic, lapilli tuff and lappillistone rocks. Unconformity Tisdale Assemblage: Gold Centre Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows. Vipond Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows. Central Formation Dominantly composed of Mg-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanic flows. Hersery Lake Formation Dominantly composed of komatiitic to basaltic- komatiite metavolcanic flows. Porcupine-Destor Deformation Zone Deloro Assemblage: Dominantly composed of mafic, calc-alkaline metavolcanic flows interbedded with felsic volcaniclastic and banded iron formations at the top. Stratigraphic horizons at which the • Porcupine Intrusive Suites occurs. Figure 2.3. Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt. Assemblages included are the Deloro, Tisdale, Porcupine and Timiskaming (modified from Pyke 1982; Ayer et al. 2002b). Maximum thicknesses of Assemblages is presented excluding the Deloro Assemblage. 63 Figure 2.4. Photographs and photomicrographs showing features of the Porcupine intrusive suites and the felsic volcanic suite: A) Sharp contact between a porphyry dike and host mafic volcanic rocks, Shaw Dome, Deloro Twp., scale = lcm:2m; B) 2 meter long transposed dike off of larger porphyry intrusions, north Vedron property, scale = lcm:40cm; C) Porphyritic texture with feldspar and quartz phenocrysts within a quartzo-feldspathic matrix, Gillies Lake porphyry; D) Porphyritic texture with quartz and feldspar phenocrysts within a quartzo- feldspathic matrix, Naybob porphyry, XPL, scale = lcm:2mm; E) Equigranular texture of interlocking feldspars and quartz crystals, Porphyry Hill, XPL, scale = lcm:2mm; F) Porphyry diatreme with sericite and hematite altered fragments of porphyry within a tourmaline rich matrix, Pearl Lake porphyry; G) Relict feldspar phenocrysts that have undergone partial sericite replacement (alteration), Preston porphyry, XPL, scale = 1cm: 1mm; and H) Complete sericite replacement (alteration) of feldspar phenocrysts yielding quartz-sericite schist, Preston porphyry, XPL, scale =lcm: 1mm. 64 Figure 2.4, continued. Photographs and photomicrographs showing features of the Porcupine intrusive suites and the felsic volcanic suite: I) Strongly sericite-calcium carbonate ("dirty") altered porphyry with feldspar phenocrysts completely replaced displaying D2 and D3 spaced cleavages, Pearl Lake porphyry, PPL, scale = 1cm: 1.5mm; J) Well developed D2 and D3 spaced cleavages, Buffalo Ankerite #5 porphyry; K) Quartz-tourmaline vein, Edwards porphyry; L) Large sulphide (pyrite) fragment ("clot"), Carr Township porphyry; M) Mafic clasts within a conglomerate fades of the Krist Formation, Kayorum Syncline; and N) Elongate, stretched porphyry clasts along transposed S0/S2 fabric, Krist Formation, Kayorum Syncline. epidote Legend ifi calcite 4»1i •A" TIS-main * TIS-other a CIS A HIS o GIS • FVS K-feldspar 40 60 80 100 Hashimoto Alteration Index I Fresh to Weakly I Altered Na-Altered T^Tttftrrflniftr W\ *™V"*- 4 6 Na20 C| Spillite ' T a-Metasomatism) 7° Igneous Spectrum o(weakly altered^ r . • / Keratophyre _ ** !^. ~itc *& (K-Metasomatism]_ •"i X J_ _L 20 40 60 80 100 100*K2O/Na2O+K2O Figure 2.5. Mobile element plots for the Porcupine intrusive suites and the felsic volcanic suite, including: A) alteration box-plot (from Large et al. 2001) with Hashimoto alteration index [(MgO+K20)/(MgO+K20+Na20+CaO)] (Date, Watanabe and Saeki 1983; Saeki and Date 1980) plotted against chlorite-carbonate-pyrite-index [(MgO+Fe203T)/(MgO+Fe203T+ Na2 Legend i—«—r it TIS-main • TIS-other 6 t~ Na-Loss = K-Alteration D CIS « * o A HIS a4 O GIS • FVS 4 6 10 12 Na20 20OEI T ISH— Fignre 2.5, continued. Mobile element plots for the Porcupine intrusive suites and the felsie volcanic suite, including: D) Na20 versus K2O plot; E) K2O versus Rb plot; and F) NaaO versus Rb plot. Legend note: TIS - Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsie volcanic suite. 67 T—i i I IIII| 1—r Anorthite £T Subalkaline A: tonaiite B: granodiorite ife- C: adamellite D: trondhjemite E: granite o H .1 "S N •oib- .001 .01 Nb/Y Orthoclase 120 ET 80 w I ' I ' I ' I ' I ' I ' I 100 80 f- -i eon i&d&to*- - 20 l^*"^ 201- __ — — "~ iVYb=££,«Ii»£2?i',n—_ ^ ^ n: I — — i^yt=ii *a!ai,i,; " O1 2 3 Yb 100 K Legend 10 • TIS-main if US-other Slr • A**h&&&8^J< m D CIS A HIS o GIS .lk * FVS .01 10 12 14A120316 Figure 2.6. Immobile element discrimination plots for the Porcupine intrusive suites and the felsic volcanic suite, including: A) Nb/Y versus Zr/Ti02 discrimination diagram of Winchester and Floyd (1977); B) typical CIPW normative mineral calculation feldspar diagram from O'Connor (1965); C) Yb versus La plot showing tholeiitic, transitional and calc-alkaline magmatic affinity fields (Barrett and McLean 1999); D) Y versus Zr/Y of Lesher et al. (1986) with tholeiitic, transitional and calc-alkaline magmatic affinity fields (Barrett and McLean 1999); and E) AI2O3 versus Yb diagram of Arth (1979) classifying different types of tonalite- trondhjemite-granodiorite (TTG). Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 68 12 Bj ' 1 ' 1 Legend 10- "A" TIS-main 8 -A" TIS-other O ." O CIS U6 — A HIS 4 — ^ O GIS ~ir... T&rfc^r j_WAdakite * FVS 0 1 * | """A^lTtg^T^ ^ ^ 80 50 60 70 80 Si02 50 ET 5 ^r 40 r- ~i 4h 30; - 3 A 20 f- -I 2k - Adakite' Adakite 10r~ • H 1 • A I 0 50 60 70 80 50 60 70 80 Si02 S1O2 -1 200 1 ' 1 ' 9 150 '_* ^as§ — Adakite _„ NJ A Normal Arc A A 50 Adakite - . Normal Arc X BB 1 1 1 I 20 40 60 80 2 Y Yb Figure 2.7. Classification plots of adakite-like rocks for the Porcupine intrusive suites and the felsic volcanic suite, including: A) Si02 versus AI2O3 with adakite fields (Si02 > 56 wt% and AI2O3 > 15 wt%); B) Si02 versus MgO with adakite field (MgO < 3 wt%); C) Si02 versus Y with adakite field (Y < 18 ppm); D) Si02 versus Yb with adakite field (Yb < 1.9 ppm); E) Y versus Sr/Y with adakite and normal arc magmatism modified from Defant and Drummond (1993); and F) Yb versus La/Yb (modified from Castillo et al. 1999). Adakite fields from Defant and Drummond (1990). Legend note: TIS = Timmins porphyry intrusive suite (-main camp and - other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 69 10001n r i i i i i i i i ^r T—I—I—r ~t—r—I—I—I—r Timmins Porphyry Intrusive Suite Timmins Porphyry Intrusive Suite «100 (Main Camp) (Main Camp) o. <3 Th La ft Sm Hf Ti Tb YYbAISc La ft Pm Eu Tb Ho Tm Lu NjCeNdZrEuGiDyErLu V Ce Nd Sm Gd Dy Er Yb luuoj^p-r i J i i i i i i i i—i i J T—i—i—i—i—r «» J—' Timmini s Porphyry Intrusive Suite nr Timmins Porphyry Intrusive Suite (Other) (Other) 1 la ft Sn Hf Ti lb YYb La ft Pm Eu Tb Ho Ttn NbCeNd&EuGdDyErLu Ce Til Sm Gd Dy Er Yb 1000 • i i i i i i i i i i nr T—i—i—i—r- -i—r—i—r r Carr Township Porphyry Intrusive Suite Carr Township Porphyry Intrusive Suite glUI100 . 1 lot •c PH iW i ThLaftSmHfTilb YYbAISc La ft Pm Eu Tb Ho Tm Lu NbCeNa&EuGdDyErLu V Ce >U Sm Gd Dy Er Yb Figure 2.8. Primitive mantle- (PMN) and chondrite-normalized (CHN) plots for the Porcupine intrusive suites and the felsic volcanic suite, including: A) PMN - Timmins porphyry intrusive suite (main camp; TIS); B) CHN - Timmins porphyry intrusive suite (main camp; TIS); C) PMN - Timmins porphyry intrusive suite (other; TIS); D) CHN - Timmins porphyry intrusive suite (other; TIS); E) PMN - Carr Township porphyry intrusive suite (CIS); and F) CHN - Carr Township porphyry intrusive suite (CIS). Shaded region in all of the plots is the spectrum of the respective PMN or CHN TIS-main camp REE profile. Primitive mantle values from Sun and McDonough (1989) and chondrite values from McDonough and Sun (1995). 70 i i i i i i i i i i i i i i i i i i i Holmer Intrusive Suite Th La ft Sm Hf Ti lb YYbAl^ La ft Pm Eu Tb Ho Tm Lu Ce Nd Sm Gd Dy Er Yb 1000 U] ' ' ' ' ' ' ' ' ' ' Granodiorite Intrusive Suite Th la ft Sm Hf 1 lb YYbAl La ft Pm Eu Tb Ho Tm Lu NjCtWSBiQi^BIiiV Cfe Nd Sm Gd Dy Er Yb 1000] u w Felsic Volcanic Suite Felsic Volcanic Suite (Krist Formation) 4*F>k (Krist Formation) 3~io^ 1 lb- Th La ft Sm Hf 15 lb YYbAl La ft Pm Eu Tb Ho Tm Lu NbCbNd&EuGdDyErLu V Cb Nd Sm Gd Dy Er Yb Figure 2.8, continued. Primitive mantle- (PMN) and chondrite-normalized (CHN) plots for the Porcupine intrusive suites and the felsic volcanic suite, including: G) PMN - Holmer intrusive suite (HIS); H) CHN - Holmer intrusive suite (HIS); I) PMN - granodiorite intrusive suite (GIS); J) CHN - granodiorite intrusive suite (GIS); K) PMN - felsic volcanic suite (FVS); and L) CHN - felsic volcanic suite (FVS). Shaded region in all of the plots is the spectrum of the respective PMN or CHN TIS-main camp REE profile. Primitive mantle values from Sun and McDonough (1989) and chondrite values from McDonough and Sun (1995). 71 -7TT—1 ' 1 l"l| 111 III 1-TTTTTTIJ- Al ' — t -n Rl 1—1 1 1 mil r—1 1 1 nil) 1 000 ~-1= 100 ~ Legend : "A" TIS-main within plate ^ N. within plate ir TIS-other Imii i _ 1 10 - 100 n cis ^ ^\s^ ; syn-collisional >< ^^*^ V^ A HIS - syn-collisional o GIS 10 _ volcanic arc > *\E ocean ridge 1 * FVS " =- volcanic arc ocea n ridge _ 1 "TIB^L ,,l r' • ill mil = • i • i mil • i i ii ill i i i i mil = 10 100 1000 10 100 Yb cj ' i /I ' 20 4 - 1 A 2 - - 1 1 Sfl^. i 0' 8 0 Sm(UCCn) Figure 2.9. Discrimination plots for the Porcupine intrusive suites and the felsic volcanic suite, including: A) Y versus Nb diagram from Pearce et al. (1984); B) Yb versus Ta diagram from Pearce et al. (1984); C) Upper continental crustal normalized Sm versus La plot (McLennan 2001); and D) Y versus Sc plot from Feng and Kerrich (1992). Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 72 ASSEMBLAGES Deloro Tisdale Porcupine Timiskaming Unconformity Unconformity VOLCANISM SEDIMENTATION \ m INTRUSIONS -SYNVOLCANIC- »H SYNTECTONIC N« LATE TECTON1C- TIS CIS GIS Albitite HIS DEFORMATION ^*D1*|-—D2—4* *M>3, D4, D5-" METAMORPfflSM MINERALIZATION Gold Copper I 1 n 2760 2740 2720 2700 2680 2660 2640 Age (Ma) Figure 2.10. Geochronology for volcanism, sedimentation, intrusive magmatism, deformation, metamorphism and mineralization within the Porcupine gold camp. Modified from Bateman et al. (2005). Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; GIS = granodiorite intrusive suite; and HIS = Holmer intrusive suite. 73 Name Suite Age (Ma) Source Crown porphyry TIS - main camp 2688 ± 2 Corfu etal. 1989 Millerton porphyry TIS - main camp 2691 ± 3 Corfu etal. 1989 Miller Lake porphyry TIS - main camp - - Northern porphyry TIS - main camp - - Acme porphyry TIS - main camp - - Gillies Lake porphyry TIS - main camp - - Pearl Lake porphyry TIS - main camp 2689 ±1 Corfu et al. 1989 Coniauriuro porphyry TIS - main camp - - Dome Fault Zone porphyry TIS - main camp 2688 ±2 Gray and Hutchinson 2001 Preston porphyry TIS - main camp ca. 2690 Corfu etal. 1989 Paymaster porphyry TIS - main camp 2690 ± 2 Corfu etal. 1989 West porphyry TIS - main camp - - Northwest porphyry TIS - main camp - - Edwards porphyry TIS - main camp - - Buffalo Ankerite #5 porphyry TIS - main camp - - Buffalo Ankerite porphvrv TIS - main camp - - Bristol Twp. porphyry TIS - other 2687.7 ±1.4 Ayer et al. 2003 Bristol Lake porphyry TIS - other - - South Bristol Lake porphyry TIS-other - - northern Deloro Twp. porphyry dike swarm TIS - other - - Mt. Logano porphyry TIS - other 2689.0 ±1.4 MacDonald et al. 2005 Hoyle Pond porphyry TIS - other 2684.4 ±1.9 Bateman et al. 2005 Hoyle Pond porphyry sill TIS - other 2687.2 ±2.2 Ayer et al. 2005 Aquarius porphyry TIS - other 2705 ±10 Corfu et al. 1989 Aquarius Mine porphyry TIS - other - - Homestead porphyry TIS - other - - Crowley porphyry TIS - other - - Pominex oorphvrv TIS - other - - Carr Twp. porphvrv CIS - - Holmer porphyry HIS - - Southwest Bristol syenite HIS - - Thunder Creek porohvrv HIS - - Naybob porphyry GIS - - Porphyry Hill granodiorite GIS - - Pamour porphyry GIS 2677.5 ±2.0 MacDonald etal. 2005 Bob's Lake granodiorite GIS - - Porcupine Syncline - Krist Formation FVS 2687.3 ±1.6 Ayer et al. 2002b Kayorum Syncline - Krist Formation FVS 2687.5 ±1.3 Ayer et al. 2002b South of PDDZ - Deloro Assemblage FVS - - Table 2.1. Table of porphyry intrusions and felsic volcanic rocks included in this study. Information includes the name, Porcupine intrusive suite designation, age of crystallization (if known) and published source of age date. Porcupine intrusive suites include: TIS - Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. FVS = felsic volcanic suite. 74 Category Subcategory TIS-main camp TIS-other CIS Field Trend east-northeast/west-soulhwesl generally east-west east-west Relationships Size of trend? 2 trends: one is 8 x 2 km; and 3 groups total 50+ km along over 15x5 km one is 4 x 1.5 km PDDZ Join at depth? ves yes and ??? composite? Plunge east west and ??? ??? direction? Strarigraphic 1) northern margin of the PDDZ 1) upper Deloro l)Tisdale/Porcupine level Assemblage/ Deloro-Tisdale Assemblages contact Assemblages contact (lower/middle Tisdale -Vipond Formation) 2) Hersey Lake-Central 2) Hersey Lake-Central Formation contact Formation contact 3) Central and Vipond 3) base of the Porcupine Formations (Tisdale Assemblage/ Tisdale- Assemblage) Porpcupine Assemblages contact Stratigraphy generally semi-conformable semi-conformable semi-conformable? conformable? Other 1) pillowed mafic flows of the 1) Assemblage contacts N/A favourable zones Tisdale Assemblage for intrusion? 2) 'carb rock' alteration zones 2) fault zones (PDDZ and related splays) 3) fault zones (e.g. Dome fault) 3) fold margins (Shaw Dome) 4) fold hinges (e.g. Northern anticline) Sizes & shapes 1) small dikes, sills and plugs 1) small dikes, sills and 1) one large composite plug (up to 500 x 300 m) plugs (up to 1 km x 200 m) (over 12x5 km) 2) dikes and sills (up to 2 x 0.5 2) large dikes and sills (up km) to 5 x 0.5 km) 3) large oval (~2 x 0.6 km) 3) large thin dikes and sills (up to 5 km x 50 m) 4) large oval (6x3 km) Margins -generally straight and sharp -generally straight and sharp -generally straight and sharp with small apophyses with small apophyses (primary or tectonic) -lesser marked by breccias -lesser marked by breccias -lesser marked by breccia (Edwards, Paymaster and (Bristol Township and Mt. Crown) Logano porphyries) -minor gradational contacts (Aquarius porphyry) Table 2.2. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al. 2005. Category Subcategory HIS GIS Field Trend northeast-southwest east-northeast/west-southwest Relationships Size of trend? 2km 2 trends: one is 2 x 0.5 km; and one is 5 x 2.5 km Join at depth? ??? ??? Plunge ??? ??? direction? Stratigraphic 1) Tisdale/Porcupine 1) upper Deloro Assemblage/ level Assemblages contact Deloro-Tisdale Assemblages (lower/middle Tisdale contact -Vipond Formation) 2) Hersey Lake-Central Formation contact Stratigraphy semi-conformable semi-conformable conformable? Other 1) fault zones (PDDZ and 1) fault zones (Dome fault favourable zones related splays) extension and PDDZ) for intrusion? 2) fold margins (Shaw Dome?) Sizes & shapes 1) small plug (lxl km) 1) smali dikes and sills (up to 1 km x 1000 m) 2) small dikes and sills (up 2) plug (~500 x 200 m) to 500 x 100 m) 3) large elongate plug (~5 x 2 km) Margins -generally straight and sharp -generally straight and sharp (primary or tectonic) (primary or tectonic) -lesser marked by heterolithic breccia (Holmer porphyry) Table 2.2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. 76 Category Subcategory TIS-main camp TIS-other CIS Petrology Texture aphanitic and porphvritic DorDhvritic porphvritic Phenoerysts sub- to euhedral plagioclase sub- to euhedral plagioclase sub- to euhedral plagioclase and quartz up to 8mm and quartz up to 6mm and quartz up to 15mm Matrix aphanitic to very fine grained very fine grained fine grained Minor Minerals apatite and tourmaline apatite and tourmaline N/A Sulphides pyrite, chalcopyrite, pyrite, chalcopyrite, pyrite and chalcopyrite pyrrhotite, molybdenite and pyrrhotite and molybdenite bornite Foreign clasts green mica and porphyry green mica and porphyry rounded porphyry fragments fragments up to 10cm fragments up to 10cm Metamorphic stilpnomelene biotite, chlorite and trace chlorite and biotite minerals muscovite Alteration, Alteration white mica (sericite), calcium sericite, calcium-carbonate, sericite, chlorite, hematite Veining and carbonate, hematite, iron- chlorite, hematite, iron- and silicification Mineralization carbonate (ankerite), chlorite carbonate (ankerite), and tourmaline silicification and albite Veining quartz-tourmaline, quartz- quartz sweats, quartz-calcite quartz sweats and quartz- ankerite, quartz-calcite and and quartz-ankerite calcite quartz Mineralization gold mineralization gold mineralization anomalous gold cooper mineralization anomalous coooer anomalous copper Deformation Deformation D2 foliation, D3 spaced D2 foliation and D3 spaced D3 foliation cleavage, D? stretching cleavage lineation and D6 foliation Geochronology Geochronology -Paymaster = 2690 ±2 Ma (1) -Bristol Township = 2687.7 -unknown; suspected -2685- ±1.4 Ma (3) 2670 Ma -Preston = ca. 2690 Ma (1) -Mt. Logano = 2689.0 ±1.4 Ma (4) -Dome Fault Zone = 2688 ±2 -Hoyle Pond = 2684.4 ±1.9 Ma (2) Ma (5) -Hoyle Pond sill = 2687.2 -Crown = 2688 ±2 Ma (1) ±2.2 Ma (6) -Aquarius = 2705 ±10 Ma -Millerton = 2691 ±3 Ma (1) 0) -Pearl Lake = 2689 ±1 Ma (1) Table 2.2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. 77 Category Subcategory HIS GIS Petrology Texture porphvritic and eouigranular porphvritic and equigranular Phenocrysts sub- to euhedral feldspars sub- to euhedral plagioclase (othoclase and plagioclase) ± and quartz up to 6mm quartz up to 5mm Matrix fine grained finegrained Minor Minerals N/A biotite, muscovite and apatite Sulphides pyrite and trace arsenopyrite pyrite Foreign clasts N/A N/A Metamorphic N/A biotite, chlorite and muscovite minerals Alteration, Alteration sericite, chlorite, calcium- sericite, calcium-carbonate, Veining and carbonate, hematite and iron- chlorite and iron-carbonate Mineralization carbonate (ankerite) (ankerite) Veining quartz sweats and quartz- quartz sweats and quartz- calcite calcite Mineralization gold mineralization gold mineralization no copper known no copper known Deformation Deformation D3 foliation D3 foliation Geochronology Geochronology -unknown; suspected -2675- -Pamour = 2677.5 ±1 Ma (4) 2665 Ma Table 2.2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. Sample 03-PJM-132e 03-PJM-132f 03-P.IM-132g 03-PJM-132B 03-PJM-139d 03-PJM-139e 03-PJM-139h 03-PJM-139i OTM-E Qad27 478,103 478,103 478,103 478,103 478,435 478,435 478,435 478,435 UTM-Nnad27 5,369,503 5,369,503 5369,503 5,369,503 5,369,481 5,369,481 5,369,481 5,369,481 Bote Number PJV # MC03-39 PJV * MC03-39 PJV # MC03-39 PJV#MC03-39 PJV#MC034l PJV#MC034t PJV#MC03-41 PJV » MC03-4I Dip —* Azinuttb 45—160 45—160 45—160 45—160 45—160 45 — 160 45 — 160 45 — 160 Deptnfin) 155 77 175 310 85 89 234 248 Suite TIS-main camp TIS-mam camp TIS-maiBcamp TIS-mam camp TIS-main camp TIS-main camp TTS-maincamp TIS-main camp Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Intrusion - Unit Poiphyiy Poiphyiy Poiphyiy Potphyry Poiphyiy Porphyry Porphyry Porphyry SK)! (wt%; XRF) 65.02 66.19 38.86 66.33 64.59 66.67 66.67 66.24 T1Q2 (wt%; XRF) 0.39 0.4 0.56 0.35 0.37 0.4 0.38 0.47 AKOJ (wt%; XRF) 16.98 16.28 26.3 15.73 16.28 17.51 17.13 18.01 FerOs (wt%: XRF) 3.36 4.51 7.65 3.95 5.95 4.5 3.64 6.18 MnO (wt%; XRF) 0.03 0.03 0.06 0.06 0.02 N.D. 0.07 0.07 MeO (wt%; XRF) 1.39 2.59 3.01 1.96 1.1 0.37 1.31 2.72 CaO(wt%;XRF) 2.14 0.92 4.72 2.61 1.39 0.28 2.98 0.47 NalO (wt%; XRF) 0.56 0.98 0.51 1.05 0.72 0.74 1.19 0.67 K2O (wt%: XRF) 4.45 2.9 7 256 3.51 4.1 2.21 2 P!05 (wt%: XRF) 0.21 0.1 0.2 0.12 0.13 0.19 0.15 0.18 Cr(wr%;XRF) LOI (wt%; XRF) 4.4-7 4.-6 7.2-9 5.46 4.9-3 4.4-3 4.77 3.63 Total (wt%: XRF) 99.01 99.49 96.16 ion 17 9899 99.19 100.51 100.64 Ti (Bum; ICP-ES) - - Al (ppm; ICP-ES) ------Fe(ppm:ICPrES) - - - - Mn (ppm; ICP-ES) - - - Ms (com: ICP-ES) - - - - - Ca (Bum; ICP-ES) ------Nafopm: ICP-ES) - - - - K (ppm; ICP-ES) - - - - Pfnnm: ICP-ES) ------Cr (ppm; XRF) ------Ni (ppm; XRF) V (ppm; XRF) ------Nb (ppm; XRF) 3- 3 4 2- 3- 3 2- 3- Y (ppm; XRF) 8 7 10 9 7 9 7 9 Zr 11mm: XRF) 114 108 186 107 109 123 117 no Ni (ppm: ICP-ES) 26 13 31 18 22 18 18 26 Cr (ppm: ICP-ES) Co (ppm; ICPrES) 2-1 13 14 9- 22 1-6 1-2 1-6 Sc (ppm; ICP-ES) 2.5 2.4 4.7 3.4 3.7 4.1 3.6 2.5 CB (ppm; ICP-ES) 5 53 219 32 114 9 3 17 Zn (ppm; ICP-ES) 21 87 43 58 29 16 144 238 Cd (ppm; ICP-ES) Mo (ppm; ICP-ES) N.D. N.D. 8- N.D- . N.D. N.D- . N.D. N.D. W (ppm; ICP-ES) NJ). 3 11 NT). NJ>. 4 2 5 S (ppm: ICP-ES) Be (ppm; ICP-ES) 0.57 0.5-9 1.3-5 0.49 0.52 0.5-7 0.62 0.45 Li (ppm; ICP-ES) Ba (ppm: ICP-ES) ------Sr (ppm; ICP-ES) 108.4 11-9 73.-9 74 46.9 56.6 188.1 107.5 V (Bum: ICP-ES) Vlppm; ICP-MS) 33.8 36.-6 79._6 37.-9 47.-4 53.-1 45.4 49.4 Zr (ppm; ICP-MS) 125 124 192.1 122.4 118 131.6 125.9 1472 Hf (ppm; ICP-MS) 3.3 3.2 5 3.2 3 3.4 3.3 3.8 Nb(ppm;ICP-MS) 4 3.6 5.5 3.5 4.1 4.4 3.8 5.3 Ta (ppm; ICP-MS) 0J26 0.25 0.41 0.25 026 0.28 0.25 0.32 Y (ppm; ICP-MS) 7.61 6.66 9.25 8.62 6.8 9.22 7.18 8.61 Cs (ppm; ICP-MS) 1.652 2.56 2.075 1.63 1.603 1.728 2.346 1.503 RMppnuKP-MS) 96.4 66.14 107.42 59.33 60.26 86.78 40.44 38.44 Sr (ppm; ICP-MS) J27.7 143.2 92.6 84.7 56.6 66.4 217.4 131.6 T» (ppm; ICP-MS) 3.21 2.6 4.16 2.51 2.42 2.89 2.61 2.72 U (ppm; K3>-MS) 1.941 1.014 1.714 1.041 101 1.003 0.919 1.389 La (ppm; ICP-MS) 18.51 19.89 30.36 12.4 1326 23.66 15.77 17.11 Ce (ppm; TCP-MS) 39.98 40.82 61.62 26.01 28.32 48.48 34 37.14 Pr (00m: ICP-MS) 4.885 4.95 7.151 3.202 3.529 5.86 4.267 4.614 Nd (ppm: ICP-MS) 19.69 19.48 26.05 13.02 13.74 22.8 16.86 1835 Sm (ppm; ICP-MS) 3.37 3.27 4.29 2.4 2.47 3.87 3.08 328 Eo (ppm; ICP-MS) 0.985 0.962 1.108 0.713 0.738 1.023 0.869 0.868 CtKpum; ICP-MS) 2.546 2.266 3.188 2.234 2.056 2.775 2.262 2.538 Tb (ppm; ICP-MS) 0.293 0.257 0.365 0.299 0.253 0.327 0.275 0.305 Dy (ppm; TCP-MS) 1.462 1.322 1.884 1.663 1.359 1.781 1.389 1.703 Ho (ppm; ICP-MS) 0.286 0.244 0.362 0.309 0.249 0.334 0.257 0.324 Er (ppm; ICP-MS) 0.775 0.713 1.048 0.85 0.735 0.932 0.722 0.882 Tin (ppm: ICP-MS) 0.108 0.101 0.161 0.119 0.107 0.134 0.105 0.131 Yb (ppm: ICP-MS) 0.71 0.7 1.13 0.75 0.73 0.9 0.68 0.84 Ln (onm: ICP-MS) 0.111 0,107 0.179 0.112 0.115 0.134 0.107 0.129 Table 23. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Tirnmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 03-JUM-139J 03-PJM-I40O 03-PJM-MOb O3-PJM-140C 03-PJM-M0h 03-PJM-140I 03-PJM-143C 03-WM-143e UTM-E nad27 478,435 478,283 478,283 478,283 478,283 478,283 477,464 477,464 UTM-N oa Hole Number PJVSMC03-41 PJV # MC03-02 PJV # MC03-02 PJV#MC03-02 PJV * MC03-02 PJV # MC03-02 PJV 8 MC02-21 PJVKMC02-2I Dip—* Azimuth 45 — 160 50— 160 50—160 50—160 50—160 50—160 50—180 50—180 Depth (m) 253 45 67 125 92 98 76 127 Suite TTS-mam camp TfS-mam camp TTS-mam camp TIS-main camp TIS-main camp TIS-main camp TIS-mam camp TTS.mgin camp Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake iBtrnsion - Unit Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry SiOi (wt%; XRF) 74.39 59.1 60.34 61.52 58.27 55.38 67.78 72.5 TiOz(wt%:XRF) 0.43 0.37 0.39 0.37 0.36 0.46 0.36 0.39 A1203 (wt%; XRF) 18.6 15.62 15.81 15.52 13.92 19.44 17.68 18.37 Fetffc (wt%: XRF) 0.57 698 7.53 5.8 9.77 7.37 4.48 0.7 MnO(wt%:XRF) N.D. 0.1 0.13 0.05 0.04 0.04 N.D. N.D. MeO ( UTM-E nad27 477,464 477,464 478J47 478,347 478,347 478,347 477,733 477,733 UTM-N oad27 5,369,367 5,369,367 5,369,610 5,369,610 5,369,610 5,369,610 5,369,696 5,369,696 Hole Number PJV # MC02-21 PJVSMC02-21 PJV # MC03-01 PJV * MC03-01 PJV tt MC03-0I PJV » MC03-01 PJV # MC02-24 PJV * MC02-24 Dip —* Azimuth 50-. 180 50 — 180 50-. 160 50— 160 50—160 50—160 62 — 335 62 — 335 Deptb(m) 239 383 424 312 261 214 512 663 Suite US-main camp tis-mam camp TiS-main camp US-main camp US-main camp TIS-main camp TTS-mamcamp TTS-main camp Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Pearl Lake Gillies Lake Gillies Lake Intrusion - Unit Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry SiOl (wt%; XRF) 74.77 75.64 64.07 61.32 60.62 60.29 64.73 64.11 TKM (wt%; XRF) 0.4 0.39 0.38 0.36 0.36 0.37 0.33 0.36 AlzOa (wt%; XRF) 16.46 17.42 16.86 16.37 15.32 15.83 16.06 15.25 Fe!()3 (wt%: XRF) 0.76 014 3.59 6.54 3.12 5.61 3.03 3.95 MnO(wt%:XRF) N.D. N.D. 0.03 0.09 0.06 0.05 0.06 0.07 MEO (wt%; XRF) 0.1 0.12 1.54 2.38 2.57 2.46 1.2 1.62 CaO(wt%;.XRF) 0.19 0.15 3.12 3.15 5.16 3.43 3.87 3.69 NaiO (wt%; XRF) 0.64 i.04 1.89 0.77 1.01 0.42 4.68 5.76 KJO (wt%; XRF) 3.9 3.68 1.91 2.89 3.09 4.21 2.05 1.26 P20s{wt%: XRF) 0.16 0.12 0.16 0.15 0.14 0.19 0.14 0.14 Cr(wt%;XRF) LOI (wt%; XRF) 2.55 2.3-5 5.38 6.7-1 8.79 8.6-1 3.7-3 3.58 Total lm%: XRF) 99.93 100.47 98.94 100.74 100.23 101.48 99.87 99.79 Ti (ppm; ICP-ES) - . - Al (ppm ICP-ES) Fe (pom: ICP-ES) - - - - - Mo (ppm; ICP-ES) ------Ms (man; ICP-ES) ------Ca (ppm ICP-ES) ------Na (ppm ICP-ES) - - - - K (ppm; ICP-ES) ------Pftmm: ICP-ES) ------Cr (ppm; XRF) - - - - Ni (ppm XRF) ------V (ppm; XRF) ------Nb (ppm; XRF) 3- 3- 2- 3 3- 3 2- 2- Y (ppm; XRF) 6 4 7 7 8 8 6 8 Zr (onm XRF) 106 119 123 112 114 99 107 107 Ni (ppm; ICP-ES) 4 N.D. 15 17 14 18 15 15 Cr (ppm; ICP-ES) Co (ppm; ICP-ES) 4- 1- 27 1-0 7 1-2 1-0 10 Sc (ppm ICP-ES) 2.9 4.4 3.6 3.6 3.4 4 3.3 4.2 Cu (ppm; ICP-ES) 3 N.D. 138 72 14 N.D. N.D. ND. ZB (ppm; ICP-ES) 1439 8 38 123 51 89 310 49 Cd (ppm ICP-ES) Mo (ppm; ICP-ES) N.D. N.D. N.D. 8- ND. N.D- . N.D. N.D. W (ppm; ICP-ES) N.D. 7 3 N.D. 3 6 3 4 S (ppm ICP-ES) Be (ppm: ICP-ES) 0.39 0.57 0.5-8 0.49 0.37 0.4-9 0.5-9 0.-6 Li (ppm; ICP-ES) Ba (ppm; ICP-ES) - - - - - Sr (ppm ICP-ES) 8-6 197.- 2 202.- 7 69.-8 99.6 44.-1 223.- 6 180.- 6 Y Irmm: ICP-ES) V (ppm: ICP-MS) 46.. 6 56.. 2 4_6 4-4 42.4 50.5 39.. 9 36.3 Zr (ppm ICP-MS) 120.1 127.7 141.4 130 120.5 122 112.3 114 Hf (ppm: ICP-MS) 3.1 3.3 3.5 3J 3.1 3.1 3 3 Nb (ppm ICP-MS) 3.7 3.8 4.3 4.3 4 3.7 3.5 3.6 Ta (ppm ICP-MS) 0.23 0.24 0.28 0.28 0.26 0.23 0.26 0.24 Y (ppm ICP-MS) 6.35 4.85 8.45 7.59 7.59 7.53 5.83 8.87 Cs (ppm; ICP-MS) 1.731 1.964 2.381 1.336 2.444 2.593 1.13 0.515 Kb (ppm; ICP-MS) 72.38 76.29 50.38 78.08 92.12 119.75 59.5 33.68 Sr (ppm; ICP-MS) 102.8 235.7 240 78.9 114 48.7 253.6 202.5 Tb (ppm ICP-MS) 2.58 3.42 2.61 2.7 2.62 2.58 2.5 2.47 H (ppm ICP-MS) 0.747 0.674 0.772 1.132 0.966 1.491 0.838 0.835 La (ppm ICP-MS) 10.56 11.51 16.03 22.85 21.36 16.47 14.35 15.87 Ce (ppm ICP-MS) 24.03 21.77 34.11 46.28 44.34 34.53 29.36 32.05 Pr (ppm; ICP-MS) 3.173 2.563 4.261 5.393 5.207 4.276 3.58 4.009 Nd (ppm; ICP-MS) 13.47 10.05 16.78 20.38 20.28 16.3 14.18 16.5 Sm (ppm ICP-MS) 2.92 1.88 3.09 3.31 3.48 2.73 2.42 3.08 En (ppm; ICP-MS) 0.89 0.811 0.949 0.94 0.966 0.797 0.618 0.792 Cd (ppm: ICP-MS) 2.21 1.455 2.371 2.39 2.575 2.091 1.837 2.627 Tb (ppm; ICP-MS) 0.252 0.154 0.291 0:274 0.297 0.25 0.203 0.314 Dy (ppm; ICP-MS) 1.25 0.8 1.592 1.462 1.525 1.385 1.065 1.659 Ho (ppm ICP-MS) 0.221 0.156 0.295 0.262 0.274 0.265 0.212 0.324 Er (ppm; ICP-MS) 0.618 0.485 0.814 0.729 0.786 0.77 0.593 0.931 Tin (ppm ICP-MS) 0.091 0.074 0.12 0.108 0.112 0.111 0.092 0.136 Yb (ppm ICP-MS) 0.64 0.57 0.83 0.74 0.75 0.74 0.63 0.95 Ln iDm ICP-MS) 0.1 0.093 0.121 0.113 0.116 0.117 0.099 0.151 Table 23, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 03-PJM-134d 03-P]M-134e 03-PJM-150a 03-PJM-150h 04-PJM-200 03-PJM-148 03-PJM-005 O3-PJM-O06 UTM-E nad27 477,495 477,495 476,559 476,559 476,563 482392 482,221 482,187 UTM-Noad27 5,369,818 5,369,818 5,368255 5368,255 5368,243 5,367364 5,367,261 5,367,274 Hole Number PJV * MC02-23 PJV » MC02-23 outcrop outcrop outcrop Dome Pit Dome Pit Dome Pit Dip—.Azimuth 62 — 335 62 — 335 - - - - - Deptb(m) 233 241 - - - - Suite TlS-maincamp ITS-main camp 1 id-main camp TG-main camp US-main camp US-main camp TiS-main camp TIS-maincamp Gillies Lake Gillies Lake Dome Fault latnisioa - Unit Crown Poiphyry Crown Poiphyry Crown Poiphyiy Preston Porphyry Preston Porphyry Porphyry Poiphyry Zone Porphyry SiOl(wt%;XRF) 59.7 61.26 66.79 66.63 58.57 62.43 6038 63.24 Ti02(wt%;XRF) 0.43 033 034 0.33 03 038 0.32 0.32 A»OJ(wt%;XRF) 19.64 14.88 16.09 16.08 14.16 16.74 15.92 15.93 Fe!OJ (wt%; XRF) 2.86 2:62 2.54 2.53 2.1 4.88 3.22 2.8 MnO(wr%;XRF> 0.05 0.07 0.03 0.03 0.042 0.03 0.06 0.04 MeO(wt%;XRF) 1.09 0.7 1.1 1.1 0.94 Z42 1.64 1.65 CaO (wt%; XRF) 2.53 6.87 2.48 2.38 2.13 2.02 4.47 3.73 N«JO(M%;XRF) 9.97 3.64 5.91 5.94 4.9 1.05 3.06 0.5 K20(wt%;XRF) 0.53 2.44 1.48 1.49 134 424 336 4.41 P205 (wt%; XRF) 0.21 0.14 0.14 0.14 0.14 0.12 0.15 0.15 Cr(wt%;XRF) 0.01 LOI (wr%; XRF) 2.0-7 5.6-4 3.0-4 3- 14.955 4.-5 7.15 6:-8 Total UTM-E nad27 482,130 482,130 482,039 482,084 481,913 481,257 481,257 481,616 DTM-N nar)27 5,367,289 5,367,289 5,367,324 5,367,317 5,367,201 5,367,171 5367,171 5,366,383 Hole Number Dome Pit Dome Pit Dome Pit Dome Pit Dome Pit oatcrop outcrop outcrop Dip —* Azimuth - - - - - Depth (m) Suite TIS-mai-n camp TTS-mai-n camp TIS-mai-n camp TIS-main camp TIS-mai-n camp TIS-mai-n camp TIS-mai-n camp TIS-mai-n camp Paymaster Paymaster Paymaster Paymaster Paymaster Paymaster Intrusion - Unit Prestos Porphyry West Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Sr02(wt%;XRF) 62.41 65.2 62.61 63.74 61.07 64.95 65.11 62.59 TiO! (M%; XRF) 0.32 0.34 0.35 0.33 0.31 0.31 0.3 0.39 AUOs (wt%; XRF) 15.74 16.76 17.5 15.77 15.19 16.34 15.94 16.03 FeK» (wt%: XRF) 2.73 3.69 3.34 4.7 6.16 2.42 2.3 5.13 MnO(wt%;XRF) 0.01 0.07 0.1 0.11 0.16 0.06 0.07 0.03 MsO (wt%: XRF) 1.55 1.96 1.72 2.19 1.97 1.29 1.2 1.66 CaO(wt%;.XRF) 337 1.72 2.45 2.19 4.14 4.05 4.48 3.02 Nart) rwr%: XRF1 5.82 0.24 2.54 2.02 3.72 3.66 3.06 5.2 K!0(wt%:XRF) 2.05 4.85 3.65 3.15 2.15 2.17 Z29 1.65 PiOs (M%; XRF) 0.11 0.13 0.13 0.11 0.11 0.1 0.1 0.15 Cr(wt%:XRF) LOI(wt%;XRF) 4.7 4.6-2 4.8-2 4.65 3.4-9 4.71 5.-1 3.3-9 Total (wt%: XRF) 98.81 99.59 99.2 98.97 98.48 100.04 99.95 99.24 Ti (pom ICP-ES) Al (pom: ICP-ES) - Fe (ppm: ICP-ES) - - - Mu (ppm: ICP-ES) ------Me room; ICP-ES) - - - - - Ca (ppm: ICP-ES) - - - Na (ppm; ICP-ES) - - - - - K (ppm; ICP-ES) ------P(nnm: ICP-ES) - - - - Cr (ppm; XRF) - - Ni (ppm; XRF) - - - - V (ppm; XRF) - Nb (ppm; XRF) N.D- . 2 2- N.D- . 2 N.D. N.D- . 2 Y (ppm; XRF) 4 6 6 5 5 4 4 6 Zr (nom: XRF) 88 93 101 90 84 89 86 101 Ni (ppm: ICP-ES) 18 23 18 26 21 24 19 15 Cr(ppm;K;P-ES) Co (ppm; ICP-ES) 8- 9- 1-0 9- 1-4 8- 6- 5- Sc (ppm; ICP-ES) 2.9 3.4 3.5 3.4 3.4 2.6 2.6 3.9 Cu (ppm; ICP-ES) 160 14 12 4 289 N.D. N.D. 7 Zn (ppm; ICP-ES) 10 46 1223 89 91 53 54 32 Cd (ppm; ICP-ES) Mo (ppm; ICP-ES) ND. N.D. N.D. N.D. N.D- . N.D- . N.D- . N-D W (ppm; ICP-ES) 8 9 3 4 7 4 4 6 S (ppm; ICP-ES) Be (ppm; ICP-ES) 0.57 0.6-3 0.63 0.4-9 0.4-4 0.5-3 0.5-6 0.5 Li (ppm; ICP-ES) Ba (ppm; ICP-ES) - - Sr (ppm; ICP-ES) 232.-9 52.-7 89.7 82 103.4 194.- 5 201,7 203.-6 Y (nmn: ICP-ES) V (ppm; ICP-MS) 35.3 45.6 45.8 42.5 37.7 35.. 7 33.9 51.7 Zr(ppm;ICP-MS) 91.8 110.1 116.8 97.3 89.6 88.9 89.2 107 Hf (ppm; ICP-MS) 2.6 3.1 3.1 2.6 2.4 2.4 2.5 2.8 Nb (ppm; ICP-MS) 2.9 3.1 3.3 3 2.9 2.3 2.4 3.5 Ta (ppm: ICP-MS) 0.22 0.24 0.25 0.22 0.21 N.D. 0:2 0.22 Y (ppm; ICP-MS) 3.91 5.56 5.6 5.67 5.68 3.85 4.39 5.99 Cl (ppm: ICP-MS) 0.571 1.361 1.251 0.99 2.405 1.755 1.78 0.189 Rb (ppm; ICP-MS) 49.61 111.21 92.61 86.84 53.38 59.06 59.08 34.77 Sr (ppm: ICP-MS) 256.1 57.7 105.3 94.2 117.8 227.8 229 232.8 Th (ppm; ICP-MS) 1.74 2.47 2.45 2.3 2.13 1.64 1.64 2.48 U (ppm; ICP-MS) 0.712 0.841 0.856 0.672 0.773 0.627 0.576 0.842 La (ppm: ICP-MS) 9.95 13.88 15.15 16.02 12.41 10.18 9.78 14.11 Ce (ppm: ICP-MS) 23.35 28.75 31.11 32.12 25.62 20.77 20.19 29.24 FT (ppm: ICP-MS) 2.815 3.528 3.787 3.958 3.15 2.479 2.404 3.528 Nd (ppm; ICP-MS) 10.86 13.38 14.94 15.29 12.61 9.6 9.36 13.83 Sm (ppm; ICP-MS) 1.8 2.35 2.54 2.69 2.22 1.77 1.62 2.24 Eu (pom; ICP-MS) 0.536 0.679 0.696 0.778 0.738 0.478 0.482 0.694 Gd (ppm: ICP-MS) 1.357 1.814 1.906 1.982 1.713 1.281 1.256 1.769 Tb (ppm; ICP-MS) 0.156 0.207 0.213 0.226 0.2 0.15 0.155 0.199 Dv (ppm: ICP-MS) 0.798 1.112 1.117 1.144 1.077 0.757 0.827 1.07 Ho (ppm; ICP-MS) 0.149 0.211 0.204 0.203 0.197 0.139 0.154 0.205 Er (ppm; ICP-MS) 0.407 0.582 0.568 0.556 0.529 0.397 0.437 0.575 Tm (ppm: ICP-MS) 0.061 0.088 0.078 0.078 0.079 0.058 0.062 0.088 Yb (ppm; ICP-MS) 0.41 0.58 0.55 0.52 0.53 0.39 0.44 0.59 mtoBticr-M5) 0.065 0.089 0.081 0.078 0.082 0.06 0.062 0.098 Table 23, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample (1J-PJM-I49 03-PJM-001 03-PJM-002 03-PJM-084 03-PJM-011 03J>JM-S15 03JMM-022 03-PJM-028 UTM-E nad27 481,277 480,487 480,466 480,486 479,424 479,453 479,413 479,458 UTM-N nad27 5,366,102 5,365,925 5,365,896 5,365,859 5,366\297 5,366,278 5,366,339 5,366,358 Hole Number outcrop outcrop outcrop outcrop outcrop outcrop outcrop outcrop Dip—»AziuiuUi - - - Depth (m) - - - - Suite TIS-mamcamp US-main camp TlS-main camp TIS-mamcamp TIS-main camp TIS-main camp TIS-marn camp TIS-raam camp Northwest Northwest Northwest Edwards Edwards Edwards Edwards Intrusion - Unit West Porphyry Porphyry Potphyry Porphyry Porphyry Porphyry Porphyry Porphyry SKfc (wt%; XRF) 61.05 63.37 60.98 66.63 69.47 68.52 70.56 72.05 Ti02 (wt%; XRF) 0.43 0.34 0.38 0.36 0.22 0.2 0.2 0.23 AfcOs (wt%; XRF) 16.3 16.19 17.14 16.75 14.93 15.19 15.45 15.33 Fe203 (wt%; XRF) 2.06 2.97 2.83 3.53 1.34 1.52 1.7 1.26 MnO(wt%:XRF) 0.03 0.03 0.04 N.D. 0.03 0.03 0.06 0.01 MEO (wt%: XRF) 1.93 1.32 1.24 1.15 0.62 0.61 0.69 0.53 CaO(wt%:XRF) 3.94 3.19 325 0.8 2.75 32 1.31 1.04 Natf)(wt%;XRF) 4.98 6.62 9.97 7.52 3.77 4.32 2.98 4.33 KIO (wt%: XRF) 2.46 1.13 0.28 0.94 2.96 2.46 3.48 2.67 P!Os(wt%;XRF> 0.18 0.14 0.2 0.15 0.07 0.08 0.08 0.08 Cr (wt%; XRF) LOI(wt%;XRF) 5.7-7 3.87 3.23 1.68 3.37 3.7-1 2.7-7 1.98 Total (wt%: XRF) 99.14 99.17 99.54 99.52 99.52 99.82 99 28 99.5 Ti (ppm; ICP-ES) Al (ppm: ICP-ES) - - Fe (ppm; ICP-ES) ------Mn (pom: ICP-ES) ------Me (ppm; ICP-ES) - - - - Ca (ppm; ICP-ES) - - Na (ppm; ICP-ES) - - - - - K (ppm; ICP-ES) - - - - - T (rrnnv ICP-ES) . . . . Cr (ppm; XRF) ------Ni (ppm; XRF) V (ppm; XRF) - - - - - No (ppm; XRF) 3- 2- 3- 2 N.D- . N.D. N.D- . N.D- . Y (ppm; XRF) 6 6 6 5 3 2 4 2 Zr(DDm:XRF) 103 100 106 109 96 93 97 95 Ni (ppm; ICP-ES) 14 13 12 10 11 8 20 12 Cr (ppm; ICP-ES) Co (ppm; ICP-ES) 9 7- 11 6- 4- 4- 7 5- Sc (ppm; ICP-ES) 4.4 3.5 2.8 2.8 2.1 2.1 2.2 2 Ca (ppm; ICP-ES) to N.D. 34 154 N.D. 3 N.D. N.D. Za (ppm; ICP-ES) 15 45 9 18 23 21 22 12 Cd (ppm; ICP-ES) Mo (ppm; ICP-ES) N.D- . N.D- . N.D- . N.D- . N.D- . N.D- . N.D. NX)- . W (ppm; ICP-ES) 8 7 12 8 11 6 9 8 S (ppm: ICP-ES) Be (ppm; ICP-ES) 0.6-1 0.66 0.39 0.-5 0.5-2 0.5-1 0.5-7 0.4-9 LI (ppm; ICP-ES) Ba (ppm: ICP-ES) - - - - - Sr (ppm: ICP-ES) 321.- 8 351.- 2 173.- 2 280.- 1 52.3 68.-9 4-1 5-4 Yftmm: ICP-ES) V (ppm: ICP-MS) 58.. 4 44.4 14.1 37.-3 21.4 2.1 22.. 6 22.3 Zr(ppm;ICP-MS) 105.3 108.4 109.2 117.8 105.3 103.9 107.8 103.4 Hf (ppm; ICP-MS) 2.8 2.9 3 3.1 2.8 2.9 2.9 28 Nb (ppm; ICP-MS) 3.8 3.3 3.6 3.5 1.5 1.4 1.6 1.5 Ta (ppm; ICP-MS) 0.23 0.24 0.25 0.25 N.D. N.D. N.D. N.D. Y (ppm: ICP-MS) 6.95 6.32 6.64 6.06 2.86 2.79 4.25 2.48 C« (ppmUCP-MS) 0.263 0.156 0.044 0.104 0.444 0.23 0.55 0.354 Rb (ppm; ICP-MS) 51.44 25.62 5.41 17.11 71.16 51.24 82.9 66.68 Sr (ppm; ICP-MS) 370.2 397.4 199.6 324.4 57.7 76.6 452 61.4 To (ppm; ICP-MS) 2.91 253 2.43 225 1.88 1.87 2.04 2.02 U (ppm; ICP-MS) 0.558 0.801 0.749 0.771 0.642 0.668 0.505 0.656 La (ppm: ICP-MS) 16.4 15.94 18.83 14.45 9.92 10.12 11.44 10.34 Ce (ppm: ICP-MS) 37.83 32.64 35.88 30.18 19.16 19.06 20.6 19.62 Pr (ppm; ICP-MS) 4.956 3.987 4.328 3.72 2.19 2211 2.46 2.261 Nd (ppm: ICP-MS) 20.2 16.11 17.44 15.01 8.36 8:23 9.24 8.43 Sm (ppm; ICP-MS) 3.42 2.84 2.9 2.6 1.54 1.55 1.66 1.46 En (ppm; ICP-MS) 0.88 0.739 0.784 0.69 0.404 0.424 0.456 0.373 Cd (ppm; ICP-MS) 2.39 2.091 2.133 1.935 1.181 1.208 1.355 1.036 Tb (ppm; ICP-MS) 0.272 0.249 0.244 0.231 0.125 0.129 0.142 0.11 DT (ppm; ICP-MS) 1.436 1.279 1.305 1.17 0.588 0.586 0.709 0.533 Ho (ppm; ICP-MS) 0.256 0.235 0.24 0.213 0.102 0.099 0.131 0.092 Er (ppm: ICP-MS) 0.685 0.653 0.69 0.587 0.263 0.266 0.346 0.248 Tn (ppm; ICP-MS) 0.101 0.094 0.096 0.086 0.036 0.038 0.048 0.035 Yb (ppm: ICP-MS) 0.66 0.69 0.64 0.55 0.24 025 0.3 0.24 Lu (ppm; ICP-MS) Sample 03-PJM-O37 03-PJM-045 03-PJM-084 03-PJM-105 04-PJM-230 04-PJM-23I 04-PJM-300 (1) O4-PJM-300 (2) UTM-E nad27 47V13 479,537 479,624 479,700 479,929 479,861 ??? ??? UTM-N oad27 5,366,261 5366,340 5,366339 5,366,480 5,365,581 5365,544 ??? 979 Hole Number outcrop outcrop outcrop outcrop outcrop outcrop Hoyfe Pond Mine Hoyle Pond Mine Dip —* Azimuth ------Depth (m) ------720m level 720m level Suite TIS-main camp TTS-main camp TiS-main camp TTS-main camp TTS-main camp TTS-main camp TlSH>ther TTS-other Edwards Edwards Edwards Edwards Buffalo- Ankerite Buffalo Ankerite Hoyle Pond Hoyle Pond Intrusion - Unit Porphyry Porphyry Porphyry Porphyry #5 Porphyry #5 Porphyry Porphyry Porphyry SiOl (wt%; XRF) 70.19 66.74 69.53 65.59 63.09 65.77 55.52 55.22 TKte (wt%; XRF) 0.24 0.28 0.21 0.24 0.25 0.2 046 0.46 AUOJ (wt%; XRF) 14.94 161 1437 15.05 14.96 13.85 11.61 11.54 FezOi (wt%; XRF) 1.42 1.96 1.46 1.86 2.05 1.76 4.84 4.84 MnO (TW%: XRF) 0.03 0:05 0:03 0:09 0.029 0.058 0.106 0.106 MeO(wt%;XRF) 1.22 1.35 0.67 1.07 2.1 0.67 4.57 4.58 CaO (wr%; XRF) 0.36 1.67 334 4.92 0.15 1.96 8.34 8.24 NaM) (wt%: XRF) 9.51 9.14 4.63 3.59 7.66 2.81 2.68 2.58 KJO(wt%;XRF) 0.11 0.07 1.63 2.32 0.1 2.52 1.56 1.52 P2OS (wt%: XRFI 0.08 0.08 0.07 0.07 0.08 0.09 0.1 0.11 Cr (wt%; XRF) N.D. ND. 0.03 0.03 LOl (wl%; XRF) 0.8-3 1-8 3.7-4 5.1-1 9.8935 10.6592 10.1988 10.8066 Total lwt%- XRF) 98.91 99.22 99.68 99 92 1003525 1003372 1000148 100 0326 Ti (pom; ICP-ES) 1242 979 2108 AI (own: ICP-ES) - - - - 81338 72886 57700 - Fe (mm: ICP-ES) - - - - 16496 13763 32681 - Ma room; ICP-ESI - - - - 200 388 628 - Ma (oom: ICP-ES) - - - - 13953 4207 26530 - Ca loom; ICP-ES) - - - - 1198 15816 60137 - Na (oom: ICP-ES) - - - - 59410 21844 20438 - K (oom; ICP-ES) - - - 274 20172 12490 - P 11mm: ICP-ES) . . . . 275 279 350 _ Cr (pom; XRF) - - - - N.D. 35 274 276 Ni (ppm; XRF) N.D. 19 S3 86 V (ppm; XRF) - - - 37 23 129 126 Nb (opm; XRF) N.D- . N.D- . N.D- . N.D- . NJJ. N.D. 2 3 V loom; XRF) 2 2 2 3 7 7 9 9 Zr fnnm: XRF) 100 73 92 66 80 98 69 67 Ni (opm; ICP-ES) 13 8 9 6 10 24 91 Cr (oom; ICP-ES) 9.67 34.18 184.93 Co loom; ICP-ES) 5- 1-0 5- 4- 8 6 19 - Sc (opm; ICP-ES) 2.1 2.7 2 23 2.9 2.4 9.8 - C11 (oom; ICP-ES) 8 5 N.D. N.D. N.D. N.D. 8 - Ztr (ppm: ICP-ES) 28 68 43 51 5 N.D. 71 - Cd (oom; ICP-ES) N-D. N.D. 4 - Mo (opm; ICP-ES) N.D- . N.D- . N.D- . N.D- . N.D. N.D. N.D. - W (oom; ICP-ES) 5 6 4 2 N.D. N.D. 3 - S (pom; ICP-ES) >400 N.D. >400 - Be (com; ICP-ES) 0.2-2 0.-4 0.4-2 0.-4 0-28 0.48 0.52 - Li (ppm; ICP-ES) - - - - 15 3 14 - Ba (oom; ICP-ES) - - - - 26 677 1088 - Sr (oom: ICP-ES) 31.9 69.1 140.3 75 29.2 763 188 - Vlraim: ICP-ES) - - - 3 29 5.8 _ V (pom: ICP-MS) 16.4 30 192 27 31.7 22 93.7 - Zr (pom; ICP-MS) 107.6 79.3 104.5 71.8 79.1 102 75 Hf (pom; ICP-MS) 2.9 2.2 2.9 2 2.2 2.7 2 - Nb (ppm; ICP-MS) 1.5 1.9 1.7 1.7 2 1.6 2.9 - Ta (ppm; ICP-MS) ND. 0:17 N.D. N.D. N.D. N.D. N.D. - Y (pom; ICP-MS) 2.62 3.48 2.89 332 3.48 3.39 631 - CJ (nom: ICP-MS) 4.346 0.028 1.149 1.35 0.041 2.22 1.277 - Hb (oom; ICP-MS) 4.83 0.8 45.87 53.66 0.28 71.85 39.24 - Sr(opm; ICP-MS) 36.3 78.7 158.5 84.7 30.9 79.6 207 - Th (pom; ICP-MS) 1.99 0.95 1.82 0.83 0.98 1.86 0.8 - V (oom; ICP-MS) 0.654 0.349 0.594 0.305 0.335 0.564 0.357 - La (ppm; ICP-MS) 7.29 6.16 9 4.54 6.06 9:52 8.2 Ce (ppm; ICP-MS) 15.19 12.96 17.05 9.68 12.96 17.82 18.25 - Pr (ppm; ICP-MS) L.901 1.617 2.01 1.22 U616 2.076 2-399 - Nd (pom; ICP-MS) 7.5 6.72 7.67 5.22 6.44 8.15 10.18 - Sm (ppm; ICP-MS) 1.41 1.35 1.42 1.06 132 1.47 2.05 - En (pom; ICP-MS) 0.354 0338 0375 0.306 0.366 0.415 0.705 - Gd (pom: ICP-MS) 1.028 1.085 1.109 0.901 1.101 1.119 1.738 - Tb (opm; ICP-MS) 0.118 0.136 0.122 0.114 0.14 0.133 0.225 - Dv (ppm; ICP-MS) 0.574 0.718 0:613 0.63 0.696 0.659 1.221 - Ho (ppm; ICP-MS) 0.098 0.133 0.109 0.126 0.131 0.116. 0.233 - Er (ppm; ICP-MS) 0.276 0.364 0.277 0.349 0354 0314 0.626 - TB (pom; ICP-MS) 0.038 0.049 0.039 0.05 0.05 0.043 0.092 - Yb (ppm; ICP-MS) 031 0.35 0.25 032 0.33 03 0.61 - Lflfrmm: ICP-MS) 0,935 0049 0.038 0.047 0.049 0.041 0.09 - Table 2.3, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 04-PJM-299 04-PJM-299 (1) 04-PJM-299 (2) 04-PJM-234 04-P.1M-235 04-PJM-238 04-PJM-239 04-PJM-241 UTM-Enad27 Tn ??? ??? ??? ??? ??? 7?? ??? UTM-N nad27 rn ??? 777 77? ??? ??? ?7? ??? EBM# Hole Number Hoyle Pond Mine Hoyle Pond Mine Hoyle Pond Mine EBM » A96-414 EBM # A96-414 EBM # 97-78 EBM # 97-78 C-02-2 Dip —* Azimntb - - - 55 — 344 55 — 344 55 — 344 55 — 344 50 — 342 Depth (m) 720m level 720m level 720m level 66.5 117 244.9 252.5 198 Suite TIS-other TB-other TIS-other TB-other TIS-other TlS-other TIS-other TLS-other Hoyle Pond Hoyle Pond Hoyle Pond Aquarius Aquarius Crowley Crowley Crowley Intrusion - Unit Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry SH)!(wt%:XRF) 54.03 53.87 53.96 66.17 57.85 64.45 58.42 57.29 TiOl (wr%; XRF) 0.54 0.55 0.55 0.12 0.2 0.12 0.15 0.44 AUOj(wt%;XRF) 13.57 13.6 13.54 14-29 17 2 14J6 16.93 14.85 FelOJ (wt%; XRF) 5.01 4.93 4.93 0.95 1.44 0.99 0.78 3.72 MnO (wt%; XRF) 0.091 0.095 0.093 0.016 0.019 0.011 0.047 0.059 MeO(wt%:XRF) 4.59 4.56 4.6 0.22 0.61 0.52 0.79 2.39 CaO.(wt%:XRF) 5.58 5.63 5.6 1.83 2.04 1.33 2.37 3.08 NmO (wt%; XRF) 4.93 5.08 5.04 5.43 9.22 5.88 9.01 6.52 KiO(wt%;XRF) 0.96 0.87 0.87 1.4 0.14 1.63 0.64 1.26 P2OS (wfifc XRF) 0.15 0.15 0.14 0.05 0.05 0.04 0.12 0.17 Cr (wt%: XRF) 0.03 0.04 0.03 0.01 N.D. N.D. N.D. 0.01 LOI (wr%; XRF) 108124 10.866 10.866 9.9895 10.9623 10.931 11.1214 10:5294 Total (wt%: XRF) 100.2934 100.241 100.219 100.4755 99.7213 100.252 100.3684 100.3184 TMppm; ICP-ES) 2665 57.9 944 596 684. 2113 Al (pom; ICP-ES) 71805 78419 94728 78055 90897 77595 Fe (ppm: tCP-ES) 36297 7615 11658 7711 6075 28333 Ma (ppm; ICP-ES) 588 - - 97 117 75 322 401 Ma (ppm: ICP-ES) 28113 1549 4060 3369 4938 15085 Ca (ppm; ICP-ES) 42335 - 15592 16789 11219 20088 25009 Na (ppm; ICP-ES) 38080 - 44673 >70900 47216 >70000 52384 K (ppm; ICP-ES) 821.8 - - 11956 1132 13655 5090 10269 Pfnnm: ICP-ES) 562 91 114 126 438 704 Cr (ppm; XRF) 274 295 293 68 N.D. 50 12 62 Ni (ppm; XRF) 106 107 106 N.D. ND. N.D. N.D. 34 V (ppm; XRF) 134 134 135 13 18 17 5 97 Nb (ppm; XRF) 1 1 1 6 4 N:D. N.D. 4 Y (ppm; XRF) 9 8 9 7 6 5 5 12 Zr (nnm: XRF) 86 87 85. 84 101 83 85 117 Ni (ppm; ICP-ES) 106 - ND. 4 7 5 43 Cr (ppm; ICP-ES) 226.25 - - 50 8.25 31.95 11.31 52.84 Co (ppm; ICP-ES) 24 - - 3 5 4 4 16 Sc (ppm; ICP-ES) 11.5 - 1.6 2.1 1.4 1.6 7.8 Cu (ppm; ICP-ES) 7 - - N.D. N.D. N.D. ND. 14 Zn (ppm; ICP-ES) 50 - - 177 N.D. N.D. N.D: N.D. Cd (ppm; ICP-ES) N.D. - N.D. N.D. N.D. ND. ND. Mo (ppm; ICP-ES) N.D. - ND. ND. N.D. N.D. N.D. W (ppm; ICP-ES) 5 - N.D. N.D. N.D. 7 N.D. S (ppm; ICP-ES) >400 - - N.D. 85 >4O0 >400 MOO Be (pom; ICP-ES) 0.65 - - 0.59 0.29 0.84 0.44 0.98 Li (ppm: ICP-ES) 22 - 5 1 4 ND. 5 Ba (ppm; ICP-ES) 698 - - 440 65 629 461 >1400 Sr (ppm; ICP-ES) 162.5 - - 371.2 337.5 219.4 131.5 304.6 ¥ loom: ICP-ES) 5.7 . 2.6 2.3 1.5 1.8 7.5 V (ppm; ICP-MS) 110.1 - - 11.8 19.8 15.7 5.7 75.5 Zr(ppm;ICP-MS) 90.7 88.4 102.4 86.4 87.8 121.4 Hf (ppm; ICP-MS) 2.6 - 2.6 2.9 2.9 3 3.4 Nb (ppm; ICP-MS) 3.6 - - 1.2 1.4 1.3 1.1 2.7 Ta (ppm; ICP-MS) 0.21 - N.D. N.D. N.D. N;D. N.D. Y (ppm; ICP-MS) 6.2! - 2.94 2.46 1.65 1.83 8.69 Cs (ppm; ICP-MS) 0.877 - - 0.629 0.072 0.69 0.087 0.216 Kb (ppm; ICP-MS) 24.65 - - 40.57 1.55 42.11 9.58 23.35 Sr (ppm: ICP-MS) 173.7 - 393.4 368.1 233.4 139.5 322 Tb (ppm; ICP-MS) 1 - - 1.32 1.5 1.16 1.1 5.28 U (ppm; ICP-MS) 0.424 - 0.567 0.585 1.13 0.871 1.659 La (ppm; ICP-MS) 9.08 - 8.86 7.53 6.78 7.07 34.54 Ce (ppm; ICP-MS) 20 - - 14.96 16.05 14.59 14.89 70.37 Pr (ppm; ICP-MS) 2.648 - 2.165 1.948 1.753 1.794 8.269 Nd (ppm: ICP-MS) 11.08 - - 8.79 7.62 7.23 7.14 31.24 Sra (ppm; ICP-MS) 2.18 - - 1.68 1.51 1.36 1.43 5.04 En (ppm; ICP-MS) 0.722 - - 0.465 0.479 0.381 0.399 1.331 Gd (ppm; ICP-MS) 1.81 - 1.288 1.155 0.856 0.94 3.165 Tb (ppm; [CP-MS) 0.222 - - 0.142 0.125 0.091 0.106 0.35 Dy (ppm: ieP'MSV 1.21 - - 0.64 0.537 0.37 0.444 1.769 Ho (ppm; ICP-MS) 0.24 - - 0:103 0.091 0.057 0.067 0.315 Er (ppm; ICP-MS) 0.673 - 0.288 0.24 0.135 0.152 0.886 Tm (ppm; ICP-MS) 0.099 - 0.039 0.034 0.019 0.019 0.128 Yb (ppm; KP-MS) 0.65 - - 0.24 0.23 0.13 0.13 0.85 Ln (mm: ICP-MS) 0.098 - - 0.035 0.035 0.018 0.017 0.124 Table 2.3, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 04-PJM-243 04-PJM-244 04-PJM-245 04-PJM-248 04-PJM-249 04-PJM-251 04-PJM-252 04-PJM-275 UTM-E nad27 ??? ??? ??? ??? ??? ??? ??? 464,871 UTM-N uad27 ??? 171 ??? 77? ??? ??? ??? 5361,827 EBM# EBM# EBM» TX# Hole Number EBM # 97-68 EBM # 97-68 EBM » 97-68 EBM #9642 P-00-2 P-00-2 P-00-2 BRS04-24 Dip -* Azimuth 55 — 344 55 — 344 55 — 344 60 — 344 60 — 344 60 — 344 60 — 270 58.7— 188.8 Deptb (m) 75.5 102.5 190 117.7 141.5 183 81 44 Suite TIS-otber TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other Homestead Homestead Homestead Pominex Pominex Pominex Aquarius Mine Bristol Township iDtmsiOD - Unit Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry Porphyry SIC»(wr%;XRF) 65.77 66.22 67.23 66.13 66.33 63.78 54.96 59.41 TiOl (wt%: XRF) 0.17 Oil 0.11 0.05 0.06 0.06 0.21 0.26 AI2O3 (wt%; XRF) 13.12 13.16 13.02 14.31 14.12 15.23 15.82 15.83 Fe203(wt%;XRF> 0.98 1.03 0.91 1.31 0.96 1.01 1.56 3.34 MuO (wt%; XRF) 0.019 0.019 0.018 0.003 0:01 0.014 0.03 0.041 MeO (wt%; XRF) 0.5 0.19 0:2 0.29 0.14 0.43 3.33 1.12 CaO (wt%; XRF) 0.96 0.59 0.72 0.12 0.5 1.1 3.9 3.4 NalO (wl%; XRF) 7.77 7.79 7.75 6.02 694 8.82 9.36 4.45 K20(wt%;XRF) 0.22 0.1 0.09 1.35 0.86 0.07 0.12 1.33 P203 (wt%; XRF) 0.04 0.03 0.06 0.05 0.06 0.05 0.05 0.1 Cr fwt%; XRF) N.D. ND. NJJ. 0.03 N.D. N.D. N.D. NJ>. LOI (wr%; XRF) 10:8255 11.1111 10.2245 10.6514 10.3734 9.8208 10.7801 10.8505 Total (wt%: XRF) 100.3645 100.3401 100.3225 100.3144 100:3434 100.3748 100.1101 100.1215 Ti (ppm; ICP-ES) 730 513 517 281 283 259 895 1269 Al (ppm; ICP-ES) 68628 71820 70080 75575 76643 81368 79740 8S974 Fe (ppm: ICP-ES) 7647 8478 7583 10339 7583 8060 11360 25364 Mil (ppm; ICP-ES) 120 102 134 33 54 102 195 249 Me (ppm; ICP-ES) 3129 1295 1341 1851 936 2763 20827 7039 Ca (ppm; ICP-ES) 8157 5135 6151 925 4030 9149 29386 26784 Na (ppm; ICP-ES) 62813 64778 62496 48617 52913 65986 >70000 37541 K (ppm ICP-ES) 728 366 435 10974 7218 444 319 11851 P (com: ICP-ES) 49 24 185 103 180 101 114 390 Cr (ppm; XRF) 16 39 ND. 58 11 49 23 44 NI (ppm; XRF) N.D. N.D. N.D. NX). N.D. N.D. 41 6 V (ppm; XRF) N.D. N.D. N.D. N.D. N.D. N.D. 12 36 Nb (ppm; XRF) N.D. N.D. ND. NX>. N.D. N.D. N.D. 12 Y (ppm; XRF) 6 6 6 5 5 5 6 6 Zr (ram: XRF) 98 71 71 53 54 50 72 76 NI (ppm; ICP-ES) 4 N.D. N.D. N.D. N.D. 6 46 15 Cr (ppm; ICP-ES) 12.9 41.2 10.32 41.11 7.37 64 29.33 44.39 Co (ppm; ICP-ES) 3 3 2 2 2 4 8 10 Sc (ppm; ICP-ES) 1.5 1.1 1.3 0-6 0.6 0.6 3.8 3.1 Cu (ppm; ICP-ES) 7 6 8 N.D. N.D. 37 20 109 Zn (ppm; ICP-ES) N.D. 16 N.D. N.D. N.D. N.D: N.D. N.D. Cd (ppm ICP-ES) N.D: N.D, 12 N.D. N.D. ND. N.D. N.D. Mo (ppm; ICP-ES) N.D. N.D. N.D. N.D. N.D. N.D. N.D. N.D. W (ppm; ICP-ES) N.D. N.D. N.D. N.D. N.D. N.D. N.D. 3 S (ppm; ICP-ES) >400 >400 >400 >400 >400 >400 >400 >400 Be (ppm; ICP-ES) 0.63 0.67 0.54 0.7 0.46 0.37 0.15 0.51 Li (ppm; ICP-ES) N.D. N.D. N.D. 2 I 2 N.D. 11 Ba (ppm; ICP-ES) 108 91 60 473 373 67 57 242 Sr (ppm; ICP-ES) 102.4 83.8 121.9 62.9 73.4 108.7 142.5 497.6 Y (rant ICP-ES) 2.3 2.4 2.7 1.7 1.8 1.8 2.9 2.7 V(ppm;ICP-MS) 5.8 3.3 5.7 2.9 4 4.6 11.8 32.7 Zr(ppm;ICP-MS) 99.8 73.8 72.3 48.5 49.7 49.7 80 79:9 Hf (ppm; ICP-MS) 2.9 2.5 2.4 1.9 1.9 1.8 2.1 2.1 Nb (ppm; ICP-MS) 3.3 4.2 3.8 1.8 1.8 1.8 1.7 2.2 To (ppm: ICP-MS) 0.25 0.33 0.32 N.D. N.D: N.D. N.D. N.D. Y (ppm; ICP-MS) 2.56 2.74 3:17 202 1.97 2.11 3.18 3.2 Cs (ppm; ICP-MS) 0.036 0.041 0.606 0.327 0.275 0.055 0.032 0.469 Rb (ppm; ICP-MS) 0.96 0.33 1.08 37.77 20.8 0.82 0.31 27:83 Sr (ppm; ICP-MS) 110.5 88.9 130.9 68.9 78.9 120.6 155.8 548 Tb (ppm; ICP-MS) 3.16 1.54 1.76 0.84 0.82 0.81 1.2 0.93 V (ppm; ICP-MS) 1.931 1.745 1.817 0.88 0.885 0.882 0.367 0.284 La (ppm; ICP-MS) 12.78 5.69 6.52 1.9 4.7 4.56 7.07 6.85 Ce (ppm; ICP-MS) 24.64 11.42 13.33 4.38 9.65 9.06 14.21 15.36 Pr (ppm; ICP-MS) 2.723 1.326 1.54 0.589 1,164 1.112 1.695 2.0O5 Nd (ppm; ICP-MS) 9.48 4.98 5.67 2.68 4.48 4.49 6.51 8.1 So (ppm; ICP-MS) 1.5 0.96 1.12 0.76 0.97 1 1.17 1.44 En (ppm; ICP-MS) 0.392 0.297 0.345 0.3 0.311 0.296 0.326 0.429 Cd (ppm; ICP-MS) 0.943 0.769 0.929 0.653 0.738 0.765 0.871 1.042 Tb (ppm ICP-MS) 0tl3 0.102 0.125 0.082 0.085 0.089 0.114 0.122 Dv (ppm; ICP-MS) 0.52 0.522 0:634 0.386 0.411 0.403 0.61 0.65 Ho (ppm; ICP-MS) 0.092 0.093 0.106 0.063 0.069 0.066 0.116 0.111 Er (ppm: ICP-MS) 0.237 0.238 0.259 0.165 0.155 0.156 0.319 0.304 Tm (ppm: ICP-MS) 0.036 0.033 0.037 0.021 0.021 0.021 0.044 0.044 Yb (ppm; ICP-MS) 0.24 0.22 0.22 0.12 0.13 0.13 0.29 0.3 Lu loom; ICP-MS) 0.034 0.028 O.03 0.017 0.018 0.018 0.044 0.043 Table 23, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TTS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 04-PJM-276 04-PJM-277 04-PJM-278 04-PJM-283 04-PJM-286 04-PJM-287 04-PJM-288 04-PJM-292 UTM-E nad27 464,871 464,871 464,871 464,871 464,871 464,871 464,871 464,871 UTM-N nad27 5,361,827 5,361,827 5,361,827 5,361,827 5,361,827 5J61,827 5,361,827 5,361,827 TX# TX# TX# TX# TX# TX# TX# TX# Hole Number BRS04-24 BRS04-24 BRS04-24 BRS04-24 BRS04-24 BRS04-24 BRS04-24 BRS04-24 Dip —» Azimuth 58.7— 188.8 58.7— 188.8 58.7— 188.8 58.7— 188.8 58.7— 188.8 58.7— 188.8 58.7— 188.8 58. — 188.8 Deptb(m) 65 89 98 248 309 354 375 566 Suite TTS-other TIS-other TIS-other TIS-other TTS-other TIS-other TIS-other TE-othet Bristol Township Bristol Township Bristol Township Bristol Township Bristol Township Bristol Township Bristol Township Bristol Township lotrusioo - Unit Porphyry Porohyry Porphyry Porphyry Porphyry Porphyry Porphyry Poiphyry SiO! (wt%: XRF) 58.21 61.02 60.21 54.53 58.64 59.21 60.44 58.69 TiOl (wt%: XRF) 0.26 0.22 0.22 0.41 0.27 0.25 0.23 0.25 AU03(wt%:XRF) 16.01 15.82 15.81 15.58 15.67 15.82 15.72 16.55 FetOj (wt%; XRF) 2.94 3.02 2.4 5.17 3.2 1.72 1.45 2.33 MnO (wt%; XRF) 0.045 0.036 0.033 0.113 0.088 0.071 0.06 0.055 MsO(wt%;XRF) 1.22 0.96 0.91 3.43 1.87 1.13 0.94 1.26 CaO (wt%; XRF) 3.82 2.47 2.27 5.45 4.46 4.4 3.57 2.66 NaiO (wt%; XRF) 3.81 4.98 5.7 1.94 2.28 4.3 4.62 6.64 K2O (wt%; XRF) 2.27 1.65 1.16 2.07 3.03 2.49 2.18 0.77 P!Os UTM-E uad27 464,871 464,871 464,871 464,871 461,657 462,033 462,033 478,500 UTM-N nad27 5,361,827 5,361,827 5,361,827 5,361,827 5,361,212 5,360,669 5,360,669 5,363,889 TX# TXS TX# TX# Hole Number outcrop outcrop outcrop outcrop BRS04-24 BRS04-24 BRS04-24 BRS04-24 Dip —* ATiimitli 58.7— 188.8 58.7— 188.8 58.7— 188.8 58.7— 188.8 - - - Depth (m) 604 653 717 732 - - Suite TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other Deloro Bristol Township Bristol Township Bristol Township Bristol Township Bristol Lake South Bristol South Bristol Township iBtrusioD - Unit Porphyry Porphyry Porphyry Porphyry Porphyry Lake Porphyry Lake Porphyry Porphyry Dike Swarm SIO! (wt%; XRF) 58.73 59.09 59.67 58.7 61.87 62.26 62.37 66.65 TiCte (wl%; XRF) 0.29 0.26 0-29 0.31 0.21 0.15 0.15 0.21 AUOl (wt%; XRF) 15.83 15.82 15.81 16.64 15.75 14.74 14.74 13.93 Fe203 (wt%; XRF) 3.14 2.01 3.04 2.79 1.69 1.64 1.65 0.69 MnO(wt%;XRF) 0.094 0.1 0.069 0.068 0.026 0.023 0.025 0.01 MsO (wt%; XRF) 1.52 1.4 1.56 1.38 0.89 0.81 0.82 0.06 CaO(wt%;XRF) 4.28 4.39 3.18 4.11 2.21 2.78 2.74 0.16 Na!0(wfii;XRF) 3.71 4.18 5.4 4.77 6.83 6.62 6.64 8.2 K20(wt%;XRF) 1.84 1.69 0.86 1.06 0.93 0.81 0.79 0.08 P20s(wt%;XRF) 0.09 0.1 0.08 0.09 0.08 0.05 0.05 0.09 Cr (wt%; XRF) N.D. N.D. N.D. NX). N.D. N.D. N.D. N.D. LOI(wt%;XRF) 10.5769 11.0087 10.3259 10.0915 9.8745 10.1546 10.5413 10.4649 Total (wt%: XRF) 100.0909 100.0387 100.2749 995995 100.3505 100.0276 100.5063 100.5349 TI (ppm; ICP-ES) 1416 1207 1467 1601 1005 702 - 1060 Al (ppm; ICP-ES) 82686 79911 83241 88716 86244 78774 76686 Fe (ppm; ICP-ES) 23611 14753 22531 21347 12947 12126 - 5587 Ma (ppm; ICP-ES) 607 646 438 459 158 146 - 62 ME (ppm; ICP-ES) 9430 8290 9259 8605 5623 4965 555 Ca (ppm; ICP-ES) 33472 31377 24466 31702 17296 21332 - 1513 Na (ppm; ICP-ES) 31473 31982 41087 37192 55459 50940 - 65280 K (ppm; ICP-ES) 16164 14180 7336 9383 8128 6932 338 Pftjpm; ICP-ES) 294 358 297 310 311 112 349 Cr (ppm; XRF) 19 42 23 61 31 23 1-5 N.D. Ni (ppm; XRF) 12 7 10 15 4 N.D. N.D. 4 V (ppm; XRF) 48 36 50 52 33 21 22 8 Nb (ppm; XRF) 3 5 9 8 6 3 2 N.D. Y (ppm; XRF) 7 6 7 7 5 6 5 7 Zr (rmm: XRF) 70 75 72 74 69 50 51 135 NHppm; ICP-ES) 19 14 19 19 11 8 9 Cr (ppm; ICP-ES) 23.51 37J29 29.08 54.72 36.29 18.9 13.82 Co (ppm; ICP-ES) 11 7 11 7 7 5 - 5 Sc (ppm; ICP-ES) 3.9 2.7 4.3 4.5 2.2 2.3 - 1 Co (ppm; ICP-ES) N.D. 7 ND. N.D. 66 9 12 Zn.(ppm; ICP-ES) 26 2 41 17 4. NX). - N.D. Cd (ppm; ICP-ES) ND. ND. N.D. NX). ND. N.D. N.D. Mo (ppm; ICP-ES) N.D. N.D. N.D. N.D. ND. N.D. - N.D W (ppm; ICP-ES) NX). NX). N.D. N.D. N.D. N.D. 14 S (ppm; ICP-ES) >400 >400 >400 >400 366 76 120 Be (ppm; ICP-ES) 0.62 0.55 0.77 0.73 0.57 0.42 - 0.5 U (ppm; ICP-ES) 12 11 13 15 9 9 1 Ba (ppm; ICP-ES) 304 319 162 229 1165 205 - 132 Sr (ppm; ICP-ES) 261.9 292.5 400 384.8 368.6 255.1 184.9 Ylrmnt: ICP-ES) 3 2.4 3 3.1 1.8 2 - 3 V (ppm; ICP-MS) 43.5 29.3 45 2 50.6 23.8 20.2 - 8.6 Zr (ppm; ICP-MS) 71.8 75.7 75 78.6 71.1 51.4 133.4 Hf (ppm; ICP-MS) 2 2 2.1 2.2 2 1.4 3.7 Nb (ppm; ICP-MS) 2.4 2 2.6 2.7 1.8 1.6 3.2 Ta (ppm; ICP-MS) 0.24 N.D. 0.24 0.26 N.D. N.D. - N.D. Y (ppm; ICP-MS) 3.27 2.65 3.48 3.46 1.98 2.31 3.63 Cs(ppm; ICP-MS) 1.768 1.63 0.91 1.16 0.615 0.662 0.053 Rb (ppm; ICP-MS) 50.2 43.04 227 28.99 22.92 20.05 - 0.47 Sr (ppm; ICP-MS) 279.5 322.8 442.3 415.7 398.3 284 193.1 Th (ppm; ICP-MS) 0.82 0.79 0.86 0.84 0.71 0.43 - 4.1 U (ppm; ICP-MS) 0:395 0.265 0.367 0.432 0.252 0,176 - 1.521 La (ppm; ICP-MS) 5.77 6.59 5.24 5.42 5.03 3.52 26.93 Ce (ppm; ICP-MS) 12.64 14.02 11.34 11.73 10.84 7.5 - 56.84 FT (ppm; ICP-MS) 1.605 1.737 1.489 1.569 1.357 0.951 6.888 Ndfcjpm; ICP-MS) 6.72 7.06 6.29 634 5.56 3.92 - 26.09 Sm (ppm; ICP-MS) 1.35 1.26 1.26 1.37 1.01 0.77 - 4.15 Eo (ppm; ICP-MS) 0.426 0.347 0.404 0.435 0.297 0.309 0.92 Gd (ppm; ICP-MS) 1 0.875 1.003 1.065 0.694 0;71 2.31 Tb (ppm; ICP-MS) 0.123 0.103 0.128 0.133 0.079 0.09 0.218 Dy (ppm; ICP-MS) 0.661 0.532 0.699 0.7 0.399 0.457 - 0.903 Ho (ppm; ICP-MS) 0.119 0.099 0.13 0.133 0.072 0.082 - 0.132 Er (ppm; ICP-MS) 0J14 0.253 0.368 0.359 0.194 0.211 0.311 Tm (ppm; ICP-MS) 0.O47 0.037 0.051 0.051 0.027 0.031 - 0.039 Yb (ppm; ICP-MS) 0.32 0.24 0:34 0.33 0.19 0.19 - 0.24 Lu (oran: ICP-MS) 0.046 0.037 005 0.05 0.027 0.029 - 0:033 Table 23, continued. Table of bulk rock limogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. Sample 04-PJM-222 04-PJM-223 04-PJM-224 04-PJM-225 03-PJM-1S3 04-PJM-227 04-PJM-228 UTM-E nad27 478,506 478,567 478,574 478,628 492,142 490,744 490,678 UTM-Nnad27 5,363,513 5,363,333 5,363,112 5,362,883 5,364,796 5,365,416 5,365,748 Hole Number outcrop outcrop outcrop outcrop outcrop outcrop outcrop Dip —* Azinratb ------Depth (m) ------Suite TlS-other TIS-other TTS-other TIS-other TIS-other TIS-other TIS-other Deloro Deloro Deloro Deloro Township Township Township Township Mt Logano Ml. Logano ML Logano Intrusion - Unit Porphyry Dike Porphyry Dike Porphyry Dike Porphyry Dike Porphyry Porphyry Porphyry Swarm Swarm Swarm Swarm SK>2 (wt%; XRF) 62.33 59.24 60.27 61.15 68.83 66.87 63.98 TiOl (wt%; XRF) 0.32 0.37 0.36 0.37 0.19 0.23 0.18 A1203 (wt%; XRF) 14.72 15.49 14.56 14.6 14.95 14.23 14.35 FelOJ (wt%; XRF) 2.12 3.04 2.84 2.89 1.74 0.38 1.62 MnO (wt%; XRF) 0.037 0.054 0.044 0.077 0.04 0.014 0.021 MaO (wt%;.XRF) 0.91 1.75 1.85 1.5 0.7 0.36 0.74 CaO (wt%; XRF) 3.36 1.87 3.03 2.57 3.47 1.6 2.14 Na20(wt%;XRF) 3.25 6 4.52 3.59 5 3.02 4.33 K2O (wt%; XRF) 2.11 0.95 1.66 2.14 0.87 2.57 1.68 P2OS (wt%; XRF) 0.11 0.11 0.11 0.12 0.07 0.07 0.06 Cr (wt%; XRF) N.D. N.D. N.D: N.D. N.D. N.D. LOI(wl%;XRF> 11.0683 11.305 10.9908 11.4366 3.8-5 10.9965 10.6621 Total (wt%; XRF) 100.1253 100.169 100.2248 100.4336 99.72 100.3305 99.7531 Ti (ppm; ICP-ES) 1628 1983 1731 1859 - 1184 831 AJ {ppm; ICP-ES) 79084 87753 80881 82092 - 81571 78307 Fe (ppm; ICP-ES) 16639 25027 22609 23510 - 3087 L2881 Mn (ppm; ICP-ES) 245 368 309 552 - 99 128 Ms (ppm; ICP-ES) 5909 11965 12303 10126 - 2348 4878 Ca (ppm; ICP-ES) 27774 15594 24563 21955 - 13471 17339 Na (ppm; ICP-ES) 25686 50027 38205 29382 - 24472 33102 K (ppm; ICP-ES) 16672 8159 14235 18514 - 20884 14016 P (00m: ICP-ES) 406 431 399 436 - 210 198 Cr (ppm; XRF) 38 63 54 40 - 36 12 Nl (ppm; XRF) 9 40 34 25 6 N.D. V (ppm; XRF) 39 57 57 64 - 31 15 No (ppm; XRF) 1 ND. 2 N.D. 2- N.D. 2 Y (ppm; XRF) 9 10 10 9 3. 7 7 Zr (ppm; XRF) 121 129 109 118 88 107 92 Ni (ppm; KP-ES) 15 47 41 32 6 13 7 Cr (ppm; ICP-ES) 27.6 52,17 47.18 34.39 25.84 10.99 Co (ppm; ICP-ES) 8 14 13 8 4- 8 5 Sc (ppm; ICP-ES) 2.8 5.3 5.2 4.8 1.6 2.8 2 Cu (ppm; ICP-ES) 10 N.D; 28 7 N.D. NO. N.D. Zn (ppm; ICP-ES) 13 39 4 134 50 784 N.D. Cd (ppm; ICP-ES) N.D. N.D. N.D. N.D ND. N.D. Mo (ppm; ICP-ES) N.D. N.D. N.D. N.D. N.D- . N.D. N.D. W (ppm; ICP-ES) N.D. N.D. N.D. N.D. 3 ND. N.D. S (ppm; ICP-ES) N.D. N.D. 48 54 >400 N.D. Be (ppm; ICP-ES) 0:71 0.63 0.67 0.68 0.4-5 0.52 0.61 Li (ppm; ICP-ES) 28 45 25 16 9 18 Ba (ppm; ICP-ES) 593 464 612 769 - 552 470 Sr (ppm; ICP-ES) 169 137.8 188.1 150.1 148.- 2 196.3 219.5 V (pom: ICP-ES) 5 6.8 5.8 5.1 3.4 3.3 V (ppm; ICP-MS) 31,6 47.3 48.8 44.9 12.-9 25.3 14.7 Zr (ppm; ICP-MS) 134 133.4 109.8 120.9 91.4 108.1 95 Hf (ppm; ICP-MS) 3.7 3.6 3 3.3 2.7 3.1 2.8 Nb (ppm; ICP-MS) 5.5 4.6 4 4.1 3 2.8 3.1 Ta (ppm; ICP-MS) 0.45 0.34 0.29 0.31 0.24 0.21 0.24 Y (ppm; ICP-MS) 5.59 7.42 6.54 5.73 3.65 3.85 3.74 Cs (ppm; ICP-MS) 2.47 2.393 2.985 2.782 0.203 0963 0.968 Hi. (ppm; ICP-MS) 73.01 25.36 50.08 65.18 18.28 48.39 37.24 Sr (ppm; ICP-MS) 172.4 139.6 192 150.4 166 198 232.6 Th (ppm; ICP-MS) 3.04 3.16 2.78 3.24 1.26 1.79 1.34 U (ppm; ICP-MS) 1 259 1.043 0.908 1.127 0.49 0.793 0.47 La (ppm; ICP-MS) 17.26 17.46 15.81 16.39 19.33 13.65 1238 Ce (ppm; ICP-MS) 34.96 35.84 32.09 34.58 2.252 27.15 25.41 Pr (ppm; ICP-MS) 4.228 4.313 3.781 4.185 8.66 3.131 3.013 Nd (ppm; ICP-MS) 15.86 16.63 14.97 16.23 1.56 11.88 11.17 Sn (ppm; ICP-MS) 2.78 3.07 2.77 2.93 0.385 2.03 1.92 Eu (ppm; ICP-MS) 0.742 0.843 0.746 0.759 1.175 0.562 0.506 Gd (ppm; ICP-MS) 1.93 2.253 2.042 2.026 NO. 1.339 1.336 Tb (ppm; ICP-MS) 0.244 0.288 0.247 0.235 0.141 0.164 0.158 Dv (ppm; ICP-MS) 1.137 1.507 1.296 1.185 0.131 0.792 0.774 Ho (ppm; ICP-MS) 0.194 0.273 0.241 0.216 0.348 0.144 0.138 Er (ppm; ICP-MS) 0.539 0.774 0.663 0.585 N.D. 0.381 0.346 Tm (ppm; ICP-MS) 0.075 0.111 0.095 0.087 0.048 0.056 0.05 Yb (ppm; ICP-MS) 0.5 0.74 0.62 0.56 0.32 0.38 0.33 La (ppm; ICP-MS) P,»7? 0.114 0.099 0.085 N.D. 0.056 0,048 Table 23, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. 90 Sample 03-PJM-142a 03-PJM-142I 03-PJM-142h 03-PJM-1421 03-PJM-142J 03-PJM-142I UTM-E Dad27 535,691 535,691 535,691 535,691 535,691 535,69! UTM-S nad27 5,383,412 5,383,412 5,383,412 5,383,412 5,383,412 5,383,412 PJV# PJV# PJV# PJVtf PJV# PJV# ilore Number CR02-1 CR02-1 CR02-1 CR02-1 CR02-1 CR02-1 Dtp — Azimuth 50—.180 50—180 50—180 50—180 50—180 50— 180 Depth Carr Township Carr Township Can- Township Carr Township Carr Township Carr Township iDtmsion - Unit Porphyry Porphyry Porphyiy Porphyry Porphyry Porphyry SiOz(w[%;XRF) 68.59 67.72 67.66 68.8 68.34 68.24 TiO! (wl%; XRF) 0.25 0-27 0.28 0.26 0.27 0.26 AI203 (wt%; XRF) 14.45 15.04 15.17 14.67 15.06 14.76 Fe!OJ(wt%;XRF) 1.82 2.81 2.9 2.06 1.91 2.31 MnO{wt%;XRF) N.D. N.D. 0.01 N.D. NX). N.D. MaO (wt%; XRF) 0.91 0.97 0.9 0.82 1.01 0.65 CaO (wr%; XRF) 1.88 0.95 1.65 1.06 1.34 1.85 NalO(wt%;XRF) 5.52 4.53 5.7 4.93 3.49 8.19 K20(WI%;XRF) 1.98 5.52 2.45 4.8 3.47 0.5 P20S (wt%; XRF) 0.07 0.09 0.08 0.08 0.08 0.08 Cr (wt%; XRF) LOI (wt%; XRF) 3.2-1 1.5-5 2.8-3 1.5-9 4.4-2 1.89 Total (wt%; XRF) 98.7 99 45 99.66 99.09 99.4 98.74 Ti (ppm; ICP-ES) - - - - - Al (ppm; 1CP-ES) ------Fe (ppm; ICP-ES) ------Mn (ppm; ICP-ES) ------MB (ppm; ICP-ES) ------Ca (pom; ICP-ES) ------Na (ppm; ICP-ES) - - - - - K (ppm; ICP-ES) ------P (mm; ICP-ES) . . . . _ . Cr(ppiKXRF) ------Ni (ppm; XRF) V (ppm; XRF) ------Nb (pom; XRF) N.D- . N.D- . N.D- . N.D- . N.D- . N.D- . Y (ppm; XRF) 8 8 9 9 5 9 ZriDonrXRF) 108 105 106 98 103 106 Ni (ppm; ICP-ES) 13 16 13 11 13 9 Crfppm; ICP-ES) Co (ppm; ICP-ES) 11 1-3 1-0 6- 5- 6- Sc (ppm; ICP-ES) 3.1 3.4 3.8 3.3 3.4 2.9 Co (ppm; ICP-ES) 244 463 163 2187 595 293 Zn (ppm; ICP-ES) 14 19 15 12 12 9 Cd (ppm; ICP-ES) Mo (ppm; ICP-ES) N.D- . N.D- . N.D- . N.D- . N.D- . 5-8 W (ppm; ICP-ES) 8 N.D. 6 3 4 N.D. S (ppm; ICP-ES) Be (ppm; ICP-ES) 0.7-5 0.6-3 0.8-4 0.6-1 0.6-4 0.6-2 Li (ppm; ICP-ES) Ba (ppm; ICP-ES) - - - - - Sr (ppm; ICP-ES) 295.- 8 235.- 4 296.- 4 169.- 3 128.- 8 242.- 9 V (ppm; ICP-ES) V (ppm; ICP-MS) 35.. 7 35.. 7 38.-5 31 31.-9 22.-3 Zr (ppm; ICP-MS) 110.4 1083 112.5 110.1 113 108.9 Hf (ppm; ICP-MS) 3.3 3.2 3.3 3.2 3.3 3.2 Nb (ppm; ICP-MS) 2.7 2.8 2.8 2.9 2.5 3 Ta (ppm; ICP-MS) 0.19 0.19 0.19 0.19 0.18 0.19 Y (ppm; ICP-MS) 8.89 8.8 10.19 9.31 5.16 9.59 Cs (ppm; ICP-MS) 0.889 I.S74 1.179 0.707 0.775 0.265 Rb{ppm; ICP-MS) 58.36 89.23 65.35 63.33 63.52 12.87 Sr (ppm; ICP-MS) 328.3 263.7 332.1 190.1 144.7 276.4 Th (ppm; ICP-MS) 1.57 1.58 1.62 1.55 1.63 1.41 II (ppm; ICP-MS) 0.736 1.079 0.804 1.084 1.083 1.059 La (ppm; ICP-MS) 12.11 8.28 8.79 5.74 7.22 14.16 Ce (ppm; ICP-MS) 25.27 19.63 19.63 14.4 17J2 31.67 Pr (ppm; ICP-MS) 3.266 2.787 2.692 1.99 2.134 4.174 Nd (ppm; ICP-MS) 13.78 12.04 12.12 8.96 8.53 17.34 Sm (ppm; ICP-MS) 2.92 2.88 3.08 2J2 1.64 3.77 En (ppm; ICP-MS) 0.864 0.732 0.964 0.72 0.544 0.862 Gd (ppm; ICP-MS) 2.52 2.595 2.814 2.339 1.459 3.088 Tb (ppm; ICP-MS) 0.327 0.321 0.377 0.318 0.172 0.375 By (ppm; ICP-MS) 1.799 1.792 2.032 1.821 0.98 2.046 Ho (ppm; ICP-MS) 0.337 0.324 0.375 0.342 0.191 0.37 Er (ppm; ICP-MS) 0.97 0.907 1.045 0.982 0.564 1.01 Tm (ppm; ICP-MS) 0.136 0.129 0.146 0.14 0.088 0.14 Yb (ppm; ICP-MS) 0.88 0.82 0.92 0.88 0.61 0.9 Ln fonrn: ICP-MS) 0.136 0.125 0.137 0.13 0.111 0.135 Table 23, continued. Table of bulk rock lithogeochemical data for the Porcupine intrusive suites and the felsic volcanic suite (FVS) that were sampled and examined within this study. Porcupine intrusive suites include: TIS = Timrnins porphyry intrusive suite [-main camp and -other]; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. 91 Sample 04-PJM-258 04-PJM-259 04-PJM-262 04-PJM-263 94-PJM-265 04-PJM-261a UTM-E nad27 459,491 459,491 459,049 459,049 458,680 458,526 LTM-N r.ad27 5,358,728 5,358,728 5,359,313 5,359,313 5,357,015 5,358,056 LSG# LSG# LSG# LSG# LSG* Hole Number outcrop TG03-10 TG03-10 TG04-48 TG04-48 TC03-06 Dip —» Azimntli 45 — 180 45-.180 55—180 55 — 180 - 45 -> 125 Depth (m) 217 221 69 79 - 334 Suite HIS HIS ms HIS HIS HIS Southwest Bristol Thunder Creek Iptrasiop - Unit Holmer Porphyry Holmer Porphyry Hoimer Porphyry Holmer Porphyry Syenite Porphyry SHU (wr%: XRF) 52.35 56.37 56.5 59.27 61.18 63.02 TK>2 (wt%: XRF) 0.56 0.45 0.3) 0.29 0.28 0.08 AllOJ (wt%: XKF) 16.12 13.03 18.72 17.07 17.24 14.01 Fel03 (wt%; XRF1 5.22 4.41 2.41 1.46 2.62 0.59 MnO (wt%; XRF) 0.087 0.113 0.033 0.021 0.051 0.014 MsO(wt%;XRF) 3.18 2.86 1.13 0.69 0.56 0.06 CaO (wt%; XRF) 3.94 6.53 0.75 1.4 3.12 1.34 NaiO (wt%; XRF1 6.97 5J4 8.74 8.97 4.51 5.13 KlO (wt%; XRF) 0.12 0.13 0.7 0.49 0.81 4.85 PiOsrwt%;XRF) 0.69 0.54 0.14 0.12 0.13 0.03 Cr (wt%: XRF) 0.02 0.01 N.D. ND. N.D. N.D. LOI (wl%; XRF) 11.0938 10.4202 10.724 10.5739 10.0276 11.0817 Total (wt%: XRF) jpp.3508 100,2032 100.147 100.3449 100.5186 100.1957 Ti (pom; ICP-ES) 2827 2107 1558 1435 1537 368 Al (ppm; 1CP-ES) 85216 66174 >100000 91991 73609 75649 Fe {pom; ICP-ES) 38737 31034 18196 10904 20020 4456 Ma (ppm; ICP-ES) 573 718 228 136 423 70 Me (rami; ICP-ES) 19624 17055 6942 4199 3624 381 Ca (ppm: ICP-ES) 29605 46134 5677 10880 37406 10463 Na (ppm; ICP-ES) 53317 39592 67955 >70000 21467 39667 K (ppm; ICP-ES) 723 909 6231 4142 >50000 41473 P loom; ICP-ES) 3206 2353 545 422 1186 16 Cr (ppm; XRF) 151 127 22 44 24 40 Ni Ippm; XRF) 81 73 15 16 15 NX). V Ippm; XRF) 77 88 37 36 65 13 Nb (ppm; XRF) 42 44 9 N.D. 18 14 Y Ippm; XRF) 35 29 7 10 19 8 Zr (onm: XRF) W 357 83 65 228 120 Nl (ppm; ICP-ES) 82 70 22 19 21 NX). Cr (ppm; ICP-ES) 123.99 96.71 29.12 44.18 28.88 45.82 Co (ppm; ICP-ES) 19 15 8 3 8 3 Sc (ppm; ICP-ES) 9.8 8.8 2.9 2.9 5 0.7 Cu (ppm; ICP-ES) 11 15 3 N.D. N.D. 4 Zn (ppm; ICP-ES) 64 45 N.D. N.D. N.D. ND. Cd (ppm; ICP-ES) NX) N.D, N.D. N.D. NX). N.D. Mo (ppm; ICP-ES) ND. NX). ND. N.D. N.D. N.D. W (ppm; ICP-ES) 5 N.D. N.D. N.D. 50 6 S (ppm; ICP-ES) >400 383 66 58 >400 >400 Be (ppm; ICP-ES) 1.48 1.48 0.54 0.4 0.48 0.98 Li (ppm; ICP-ES) 44 34 21 15 8 N.D Ba (ppm; ICP-ES) 267 361 168 107 >1400 >1400 Sr (ppm; ICP-ES) 947 1077 390.4 151.7 461.7 554.8 Y (oom: ICP-ES) 28.2 23.2 2.3 5.7 13.7 4.1 V(ppm;ICP-MS) 60.8 66.4 31.6 30 55.3 5.5 Zr Sample W-PJM-253 04-PJM-233 04-PJM-229 OJ-TJM-Ulg 03-PJM-141b 03-PJM-14K 03-PJM-141a UIM-E uad27 473,806 474,544 489,709 490,035 489,964 489,964 489,964 UTM-N naC7 5,363,103 5,363,207 5,370,755 5,373,031 5,373,248 5,373,248 5,373,248 Hole Number outcrop outcrop outctop PIVS 18985 PJV# 18986 PJV8 18986 PJV# 18986 Dip —» A/fuiuth 50 — 162 50—162 50—162 50-. 162 Depth (m) - - - 137 344 353 217 Suite GIS OS GIS GIS GIS GIS • Porphyry Hrtl Bob's Lake Pamour IstrnsJoa - Uait Naybob Porphyry ParnoBr Porphyry PamourPorphyry Pamour Porphyry Graoodioiite Granodiorite Laroprophyre SiOiWAXRF) 66.75 67.09 64.5 67.9 64.42 65.59 44.28 HO! (i«%; XRF) 024 0.23 0.25 0.31 0.3 0J1 0.64 AbOifin%;XKF) 12.77 13.84 14.12 15.24 15.04 16-5 10.29 FelOs (wt%: XRF) 0.87 1.35 1.31 1.69 1.91 1.59 9.69 MnOfwBtXRFl 0.008 0.006 0.024 0.02 0.03 0.02 0.17 MsO(wt%;XRF) 0.12 0.42 0.45 0,77 1.14 0.85 12.01 CaO(wt%:XRF) 0-23 0-2 1.51 137 339 2.07 833 NaM)ft»t%;XRF) 5.79 5.62 4.91 6.26 7.6 8.18 3.28 K!0(wt%;XRn 1.7 1.83 3.33 3.4 1.88 2.54 3.92 PIOSfivfifcXIlF) 0.15 0.12 0.15 0.13 0.11 0.12 0-35 Cr («%; XRF) 0.01 ND. 0.01 LOI (wr%; XRF) 11.2975 9.5788 9.2539 1.0-1 2.93 1.4-7 6.9-6 Toml Sample 04-PJM-217(l) 04-PJM-2l7<2) 04-PJM-ZIS 04-PJM-255 UTM-E nad27 476^72 476^72 479,421 480,743 480,743 UTM-J«jiajl27 5,368,066 5,368,066 5,364,094 5,369,297 5,369,297 Hole Number outcrop outcrop outcrop outcrop outcrop Dip —> Azimuth - - - - - Depth (m) - - - - - Suite FVS FVS FVS FVS FVS Krist Krist Krist Krist Formation - Formation- Deloro Formation - Formation - Intrusion - Unit Kayorum Kayorum Assemblage Porcupine Porcupine SIOl (wt%; XRF) 60.74 60.92 66.11 59.87 59.89 TI02 (wt%; XRF) 0.39 0.39 0.22 0.42 0.42 Ab03(wr%;XRF) 15.92 15.85 14.16 15.76 15.82 FelOa (wt%; XRF) 3:29 3.29 1.03 3.21 3.21 MnO (wr%; XRF) 0.063 0.062 0.016 0.059 0.06 MeO (wt%; XRF) 0.8 0,82 0.38 1.49 1.48 CaO(wt%;XRF) 2.99 3.02 0.81 3.41 3.35 NarO I'M0/.; XRF) 4.47 4.46 S.48 3.65 3.67 KtO(wt%;XRF) 1.62 1.62 1.31 1.51 1.51 P!05(wt%;XRF) 0.17 0.17 0.05 0.18 0.18 Cr (wt%; XRF) ND. ND. ND. N.D. ND. LOI(wt%;XRF) 9.9118 9.9118 10.6218 10.836 10.836 Total lwt%: XRF) 100.3548 100.5038 1O0.I778 100385 100.416 Ti (ppm; 1CP-ES) 1919 - 1136 2156 - Al (ppm; ICP-ES) 85158 40802 85040 Fe (ppm; ICP-ES) 25566 - 8167 24122 - Mn (ppm; ICP-ES) 413 - 45 386 - MB (ppm; ICP-ES) 5133 - 2302 9162 - Ca (ppm; ICP-ES) 25091 - 1791 26276 - Na (ppm; ICP-ES) 36091 - 41719 29851 - K (ppm; ICP-ES) 13316 - 10663 12884 - P (mm: ICP-ES) 708 - 177 740 - Cr (ppm; XRF) 25 2-5 36 9 9- Ni (ppm; XRF) 16 18 N.D. 10 9 V (ppm; XRF) 74 76 33 68 68 Nh (ppm; XRF) 11 11 5 15 14 V (ppm; XRF) 13 12 9 11 11 Zr (nom: JCRF) 128 128 107 126 128 Nl (ppm; ICP-ES) 24 - 6 15 - Cr (ppm; ICP-ES) 16.38 - 37.08 13.13 - Co (ppm; ICP-ES) 22 - 2 9 - Sc (ppm; ICP-ES) 8.2 - 0.8 4.9 - Cuippm; ICP-ES) 8 - 6 5 - Zn (ppm; ICP-ES) ND. - ND. 15 - Cd (ppm; ICP-ES) ND. - ND. ND. - Mo (ppm; ICP-ES) ND. - N.D. N.D. - W (ppm; ICP-ES) ND. - ND. ND. - S (ppm; ICP-ES) 68 - 138 99 - Be (ppm; ICP-ES) 0.71 - 0.84 0.61 - Li (ppm; ICP-ES) 15 - 5 20 - Ba Chapter 3: Summary and Direction for Future Research 3.1 Key Conclusions The Porcupine gold camp is one of the richestan d most prolific gold mining camps in the world, and although the bulk of the gold is not hosted within quartz-feldspar porphyritic intrusions, the intrusions show a strong spatial association with mineralization (Burrows 1925; Ferguson 1968; Davies and Luhta 1978; Pyke 1980, 1982; Burrows and Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986; Mason et al. 1988; Colvine 1989; Marmont and Corfu 1989; Burrows et aL 1993; Robert and Poulsen 1997; Brisbin 2000; Kerrich et al. 2000; Gray and Hutchinson 2001; Bateman et al. 2008). The field, petrographic and lithogeochemical observations and interpretations of the quartz- feldspar porphyritic intrusions presented in this thesis relates magma pedogenesis to crustal thickening in the Porcupine gold camp, and explains the relationship of porphyry intrusions with lode gold and copper mineralization. The main conclusions of this thesis are: 1. There are four petrogenetic suites of porphyry intrusions along the PDDZ in the Porcupine gold camp. The majority of the intrusions are related to magma generated via crustal thickening related to uplift and extension as a result of flat subduction and underplating of mafic crust, and resultant delamination and partial melting ca. 2690 Ma during Dl deformation at depths <40 kilometers. These Timmins porphyry intrusive suite (TIS) magmas were emplaced near-surface and eruptive equivalents produced the deposition of Krist Formation volcanic rocks. Approximately 10-15 Ma after TIS-Krist Formation two other lower crustal sourced magma suites were generated from mafic source rocks. The Carr Township porphyry intrusive suite (CIS) was generated by lower 95 crustal melting at shallower depths than the TIS, whereas the granodiorite intrusive suite (GIS) was generated at greater depths then the TIS. The time gap between TIS and GIS, the deepening of the source and that the two intrusive suites have intruded within the immediate vicinity of one another, suggests that D2 thrust stacking significantly thickened the crust between 2690-2678 Ma causing deeper magma generation. The Holmer intrusive suite (HIS), the youngest intrusive suite in the Porcupine camp (2675- 2665 Ma) formed via partial melting and fractionationo f magma sourced from slab-melt altered mantle at depths of >40 kilometers. 2. The Krist formation has petrographic, lithogeochemical, petrogenetic and geochronological similarities to the TIS and is interpreted to have a similar pedogenesis via the melting of underplated mafic crust at lower crustal depths of <40 kilometers. The TIS is interpreted to be the near subvolcanic intrusions that fed the pyroclastic volcanism recorded in the Krist Formation. 3. Gold is associated with all of the Porcupine intrusive suites. Large gold systems (>10 million ounces) are only related to the TIS and display strong sulphidation and potassic alteration. Moderate sized gold systems (>1 million ounces) are dominantly associated with the TIS, but also the HIS, and are related geochemically to weak sodium alteration and to weak-moderate potassic and iron-carbonate alteration. Similar to the moderate sized gold systems, small gold systems (<1 million ounces) and anomalous gold showings are associated dominantly with the TIS, but also the GIS, and are related geochemically to weak sodium alteration and their petrography indicates that they are relatively unaltered. Barren intrusions (no known historical resources) are geographically 96 controlled, and are either TIS intrusions south of the PDDZ or intrusions of the CIS and GIS suites east of the Burrows-Benedict Fault. 4. Gold has no genetic relationships with the Porcupine intrusive suites (i.e., it is not magmatically derived by the Porcupine intrusive suites). The spatial association is related to the Porcupine intrusive suites and gold mineralizing fluids utilizing the same migration conduits (i.e. reactivated regional faults) and that regional deformation created dilation zones along the margins of the intrusions that gold was deposited into as a result of favourable volcanic rock chemistry and hydrodynamic trapping. 5. The idea of the TIS, in particular the Pearl Lake porphyry as Archean analogues to Phanerozoic porphyry-eopper mineralization is not valid. Although the TIS displays many common features with modern systems, geochronological evidence argues strongly against a porphyry Cu-type origin for the Cu accumulations in the Porcupine Camp. 3.2 Potential Directions for Future Research This thesis has made a contribution to understanding magmatism related to crustal thickening in the Porcupine gold camp, as well as the relationship of porphyry intrusions to lode gold and copper mineralization. However, there are still many outstanding questions on the Porcupine intrusive suites that provide possible directions for future research in the Porcupine gold camp. Although this thesis utilized geochronology to complement the field relationships, petrography and lithogeochemistry of the different intrusions to characterize the Porcupine intrusive suites, some of the suites have had little to no geochronological work obtained on them. Age dating on the CIS and HIS, along with further dating on the GIS should confirm and compliment this study, but also be a useful tool to determine and 97 constrain regional deformation events and crustal evolution (i.e. thickening) in the Porcupine gold camp. Another avenue of further research could be conducted on the CIS. The CIS was the furthest east intrusive suite investigated within this study. It is unique in many regards compared to the intrusive suites located west of it, but might not necessarily be unique compared to other intrusions east of it. As a result of this, lithogeochemical and geochronological work could be done to compare the CIS to other intrusions along the PDDZ east of Matheson. Research on the HIS should also be completed. Due to the HIS close proximity to Lake Shore Gold's Timmins West and Thunder Creek gold deposits, further understanding is needed on how the HIS is related to gold mineralization. This research could be beneficial as it may lead to further understanding of late crustal processes under the western Abitibi Subprovince and its implication to gold mineralization. The felsic volcanic units in the Porcupine gold camp should also be considered as a potential avenue of future research. Aspects of this research could include a volcanological study of the Krist Formation and/or of the felsic rocks south of the PDDZ (i.e., are they affiliated with the Krist Formation/Porcupine assemblage or the Deloro assemblage?). This study has dismissed the role of the Porcupine intrusive suites having a genetic hydromagmatic relationship to gold mineralization, but the question of what is the source of the mineralizing fluids still remains. Future work could focus on fluid inclusion studies of mineralization in the Porcupine gold camp to possible identify mineralized fluid source. 98 With regards to more far reaching implications within this thesis, similar studies could be completed on many of the world's Archean gold terranes. Syn-tectonic intrusions could be studied, utilizing lithogeochemistry and geochronology to help further understand and constrain deformation events and crustal evolution in the Archean. 3.3 References Bateman, R., Ayer, J.A. and Dube, B. 2008. The Timmins-Porcupine Gold Camp, Ontario: Anatomy of an Archean Greenstone Belt and Ontogeny of Gold Mineralization. Economic Geology, v.103, p.1285-1308. Brisbin, D.I. 2000. World Class Intrusion-Related Archean Vein Gold Deposits of the Porcupine Gold Camp, Timmins Ontario: in Geology and Ore Deposits 2000: The Great Basin and Beyond; edited by Cluer, J.K., Price, J.G., Struhsacker, E.M., Hardyman, R.F. and Morris, C.L. Geological Society of Nevada Symposium Proceedings, May 15-18, 2000, p.19-35. Burrows, A.G. 1925. The Porcupine gold area. Ontario Bureau of Mines, v.33, pt.2, 112p. Burrows, D.R. and Spooner, E.T.C. 1986. The Mclntyre Cu-Au Deposit, Timmins, Ontario, Canada: in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A.J. Macdonald. Toronto, p.23-39. Burrows, D.R. and Spooner, E.T.C. 1989. Relationships between Archean Gold Quartz Vein-Shear Zone Mineralization and Igneous Intrusions in the Val d'Or and Timmins Areas, Abitibi Subprovince, Canada. Economic Geology, Monograph 6, p.424-444. Burrows, D.R., Spooner, E.T.C, Wood, P.C. and Jemielita, R.A. 1993. Structural Controls on Formation of the Hollinger-Mclntyre Au Quartz Vein System in the Hollinger Shear Zone, Timmins, Southern Abitibi Greenstone Belt, Ontario. Economic Geology, v.88, p. 1643-1663. Colvine, A.C. 1989. An empirical model for the formation of Archean gold deposits: Products of final cratonization of the Superior Province, Canada. Economic Geology, Monograph 6, p.37-53. Davies, J.F. and Luhta, L.E. 1978. An Archean "Porphyry-type" Disseminated Copper Deposit, Timmins, Ontario. Economic Geology, v.73, p.383-396. Ferguson, S.A. et al. 1968. Geology and ore deposits of Tisdale Township, District of Cochrane. Ontario Department of Mines, Geological Report 58,117p. Gray, M.D. and Hutchinson, R. W. 2001. New Evidence for Multiple Periods of Gold Emplacement in the Porcupine Mining District, Timmins Area, Ontario, Canada. Economic Geology, v.96, p.453-475. Kerrich, R., Goldfarb, R., Groves, D. and Garwin, S. 2000. The Geodynamics of World-Class Gold Deposits: Characteristics, Space-Time Distribution and Origins. Reviews in Economic Geology, v.13, p.501-551. 99 Mannont, S. and Corfu, F. 1989. Timing of Gold Introduction in the Late Archean Tectonic Framework of the Canadian Shield: Evidence from U-Pb Zircon Geochronology of the Abitibi Subprovince. Economic Geology, Monograph 6, p.101-111. Mason, R., Brisbin, D.I., and Aitken, S. 1988. The Geological Setting of Gold Deposits in the Porcupine Mining Camp: in Geoscience Research Grant Program. Summary of Research, 1987-19&8. Ontario Geological Survey, Miscellaneous Paper 140, p. 133- 145. Mason, R. and Melnik, N. 1986. The Anatomy of an Archean Gold System -The Mclntyre-Hollinger Complex at Timmins, Ontario, Canada: in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A.J. Macdonald. Toronto, p.40-55. Pyke, D.R. 1980. Relationship of Gold Mineralization to Stratigraphy and Structure in Timmins and Surrounding Area: in Genesis of Archean, Volcanic Hosted Gold Deposits; edited by Pye, E.G. and Roberts, R.G. Ontario Geological Survey, Miscellaneous Paper 97, p. 1-15. Pyke, D.R. 1982. Geology of the Timmins Area, District of Cochrane. Ontario Geological Survey, Geological Report 219, 141p. Robert, F. and Poulsen, K.H. 1997. World-class Archean gold deposits in Canada: an overview. Australian Journal of Earth Science, v.44, p.329-351. Wood, P.C., Burrows, D.R., Thomas, A.V. and Spooner, E.T.C. 1986. The Hollinger- Mclntyre Au-Quartz Vein System, Timmins, Ontario, Canada; Geologic Characteristics, Fluid Properties and Light Stable Isotope Geochemistry: in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A.J. Macdonald. Toronto, p.56-80. Appendix A: Porphyry Intrusions of the Porcupine Gold Camp, Western Abitifoi Subprovince, Ontario. A.1 Abstract Porphyritic felsic intrusive rocks are an important component of the Porcupine gold camp and surrounding areas. Porphyry intrusions were studied from Bristol Township, west of Timmins, to Carr Township, east of Timmins, so as to compare porphyries within the main gold camp to those outside of the main camp in both directions along the Porcupine-Destor Deformation Zone. The porphyry intrusions in the Porcupine gold camp and area have been subdivided into five suites depending on geographic location and geological relationships. These porphyry suites form generally east-trending belts ranging from 4-20 kilometers long that are typically composed of numerous intrusions ranging from small dikes a few hundred meters long to oval stocks that are up to 11 kilometers long. The porphyry intrusive suites generally intrude the Vipond Formation of the Tisdale Assemblage, but also at the Deloro-Tisdale and Tisdale-Porcupine Assemblages contacts, and the porphyry intrusive suites are generally semi-conformable to stratigraphy. The intrusions are generally porphyritic with 2-3 millimeter phenocrysts of plagioclase and quartz within a very fine grained feldspathic matrix, but also display aphanitic and equigranular textures. Minor to trace accessory minerals and xenoliths are present in all of the porphyry intrusions examined. Metamorphism of the inlrusive suites is dominantly lower greenschist facies. Alteration fades of the porphyry intrusive suites includes sericite, calcium-carbonate, chlorite, iron-carbonate, hematite, leucoxene, silica and albite. Deformation of the intrusions ranges from weak to strong. Spatially associated with most of the intrusions is both gold and copper mineralization. The intrusive suites can be distinguished based on emplacement ages into numerous suites, 101 including; 1) the Timmins Intrusive suite (TIS) intrusions, including those from the main camp area (TlS-main) and those outside of the camp (TIS-other) emplaced between -2687 and 2691 Ma. There are minor exceptions, including the Aquarius porphyry which was emplaced at 2705 Ma and the Hoyle Pond porphyry emplaced at 2684.4 Ma; 2) the Carr Township intrusive suite (CIS) and Holmer intrusive suite (HIS) emplaced between 2680-2665; and 3) the granodiorite intrusive suite (GIS) emplaced at -2677.5 Ma based on the emplacement age of the Pamour porphyry. A.2 Introduction Porphyry intrusions are spatially associated with most gold deposits along the Poreupine-Destor Deformation Zone (PDDZ) in the Porcupine gold camp, near Timmins, Ontario. Even though most of the porphyry bodies have been the partial focus of numerous past studies (Hurst 1936; Holmes 1944; Griffis 1962, 1978; Luhta 1974; Davies 1977; Davies and Luhta 1978a, 1978b; Gorman et al. 1981; Karvinen 1982; Pyke 1982; Colvine 1983; Marmont 1983; Cherry 1983; Burrows and Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986; Colvine et al. 1988; Mason et al. 1988; Colvine 1989; Proudlove et al. 1989; Jackson and Fyon 1991; Moritz and Crocket 1991; Piroshco and Kettles 1991; Melnik-Proud 1992; Burrows et al. 1993; Gray 1994; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Gray and Hutchinson 2001; Robert 2001; Wells 2001; MacDonald and Piercey 2003; MacDonald et al. 2004, 2005; Dinel and Fowler 2004; Bateman et al. 2005, 2008; Dinel et al. 2008) much debate exists regarding their genesis and relationship to gold mineralization in the Porcupine camp. It is the aim of this appendix to: 1) document the field relations, petrography and geochronology of the various porphyry intrusions along the PDDZ within the Porcupine gold camp; 2) compare 102 and contrast the porphyry intrusions; and 3) test correlations of the porphyries with the extrusive felsic volcanic units (e.g. foist Formation) in the Timmins area. The appendix will begin with a brief discussion of the previous descriptive work done on the porphyries of the Porcupine gold camp. The regional geology of the Porcupine gold camp will then be addressed, followed by a report on geological observations collected over 2003 and 2004 on the porphyry intrusions in the Porcupine gold camp as previously reported on by MacDonald and Piercey (2003), MacDonald et al. (2004) and MacDonald et al. (2005). The geology of the felsic volcanic suite will then be discussed, followed by a comparison of the various porphyry intrusion suites and possible relations with the felsic volcanic suite. This appendix will conclude with a summary of key observations. A.3 Previous Work The spatial association between gold mineralization and felsic porphyry bodies has long been recognized in the Porcupine gold camp {e.g. Burrows 1925). Over the years since discovery, much of the research done on the camp has been, at least, partially focused on the porphyry bodies (e.g. Ferguson et al. 1968; Davies and Luhta 1978a; Pyke 1982; Burrows and Spooner 1986, 1989; Mason and Melnik 1986; Wood et al. 1986; Corfu et al. 1989; Burrows et aL 1993; Brisbin 2000; Gray and Hutchinson 2001; Ayer et al. 2002a, 2002b, 2003, 2005; Bateman et al. 2004, 2005, 2008; Dinel et al. 2008). But although a wealth of research has been completed, very little descriptive documentation of the porphyry bodies has been brought into the public domain. Most geological descriptive work done on the porphyry bodies has been performed by academic research and documented within unpublished theses, including: Luhta (1974); 103 MeAuley (1983); Melnik-Proud (1992); Gray (1994); and Brisbin (1997). These theses describe the porphyry bodies within the main Timmins portion of the Porcupine gold camp (in and around the Hollinger, Mclntyre and Dome mines) but they did not study porphyries outside of the main camp , including those east and west of Timmins along the PDDZ that are spatially associated with gold mineralization. A.4 Regional Geology The oldest rocks within the Porcupine gold camp are the calc-alkaline volcanic rocks of the Deloro Assemblage (~2730 Ma), which are exposed within the Shaw Dome south of the PDDZ (Figs. Al and A2; Pyke 1980,1982; Jackson and Fyon 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002a, 2002b, 2005; Bateman et al. 2005, 2008; Thurston et al. 2008). Volcanic rocks of the Deloro Assemblage are mafic to felsic and occur as both flows and pyroclastic deposits that are intercalated with banded iron formations in the upper portion of the assemblage (Pyke 1980, 1982; Jackson and Fyon 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999). The majority of gold deposits in the Porcupine camp occur north of the PDDZ hosted by volcanic flows of the overlying Tisdale assemblage (2710-2703 Ma: Figs. Al and A2: Pyke 1980, 1982; Burrows and Spooner 1989; Jackson and Fyon 1991; Moritz and Crocket 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002a, 2002b, 2005; Bateman et al. 2005, 2008). The volcanic flows of the Tisdale Assemblage range in composition from ultramafic at the bottom of the assemblage (Hersey Lake Formation) through tholeiitic (Central, Vipond and Gold Centre Formations) in the middle to upper units (Fig. Al: Pyke 1980, 1982; Jackson and Fyon 1991; Bnsbin 1997,2000; Ayer et al. 2002b). Intercalated within the volcanic stratigraphy of the Tisdale Assemblage are minor carbonaceous argillites and wackes (Pyke 1982; Brisbin 1997, 2000; Brisbin and Pressaco 1999). The Tisdale Assemblage volcanic rocks were intruded by numerous ca. 2687-2691 Ma porphyritic felsic intrusions that are described below (Fig. Al and A2: Corfu et al. 1989; Gray and Hutchinson 2001; Ayer et al. 2003, 2005; MacDonald et al. 2005). Coeval with the porphyry intrusions are felsic metavolcanic rocks of the Krist Formation (ca. 2687 Ma), which predominantly form the base of the unconformably overlying Porcupine Assemblage (Fig. Al: McAuley 1983; Ayer et al. 2002a, 2002b, 2005; Bateman et al. 2005, 2008); geological descriptions of the Krist Formation are given below. Locally, the base of the Porcupine Assemblage is a thin carbonaceous argil lite unit (Mason et al. 1988; Brisbin 1997, 2000; Bateman et al. 2005, 2008). Stratigraphically above the Krist Formation, within the Porcupine Assemblage, are interbedded wacke and argillaceous rocks, which formed -2687 Ma (Figs. Al and A2: Ferguson et al. 1968; Pyke 1982; Jackson and Fyon 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002b, 2005; Bateman et al. 2005, 2008). The Porcupine Assemblage at a regional scale lies within regional scale basins, such as the Porcupine and Kayorum Synclines (Fig. Al: Ferguson et al. 1968; Pyke 1982; Mason et al. 1988; Jackson and Fyon 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2005; Bateman et al. 2005, 2008). The Timiskaming Assemblage metasedimentary rocks unconformably overlie the Porcupine Assemblage and were deposited between 2676 and 2670 Ma ago within isolated topographical lows (Figs. Al: Ayer et al. 2002b, 2003,2005; Bateman et al. 2005, 2008). Clastic sedimentation of the Timiskaming Assemblage includes interbedded polymictic conglomerates and arenites with lesser wackes and argillites (Pyke 1982; Jackson and Fyon 1991; Piroshco and Kettles 1991; Brisbin 1997, 2000; Brisbin and Pressaco 1999; Ayer et al. 2002b, 2005; Bateman et al. 2005, 2008). Late stage intrusive magmatism within the Porcupine camp occurred at 2672.8 ±1.1 Ma with the emplacement of late albitite dikes {Marmont and Corfu 1989; Corfu et al. 1989; Ayer et al. 2005). These albitite dikes represent the last magmatic event prior to gold mineralization and although volumetrically minor, only occurring in a few isolated localities within the Porcupine gold camp, they have a very strong spatial association with gold mineralization similar to the porphyry intrusions (Melnik-Proud 1992; Brisbin 1997, 2000; Brisbin and Pressaco 1999). Gold mineralization events in the Porcupine gold camp post-dates albitite dike emplacement at 2672.8 ±1.1 Ma (Marmont and Corfu 1989; Corfu et al. 1989) as the gold-bearing veins crosscut the albitite dikes within the Mclntyre mine (Melnik-Proud 1992; Brisbin 1997, 2000). Recent Re-Os molybdenite geochronology further supports this assertion as molybdenite from the Dome mine gold zone has been dated at 2670 ±10 Ma (Ayer et al. 2003) and molybdenite from the Mclntyre mine copper zone has been dated at 2672 ±7 Ma (Bateman et al. 2004). Although the albitite dikes are cross-cut by the copper-gold veins, the Mclntyre mine copper zone date of 2672 Ma is similar to the emplacement age of the albitite dike documented within the Mclntyre mine working (2673 Ma; Marmont and Corfu 1989; Corfu et al. 1989), which suggests that some 106 copper-gold mineralization may be genetically related to hydrothermal activity generated by albitite dike emplacement (Melnik-Proud 1992;Brisbin 1997, 2000). A.5 Geology: Quartz-Feldspar Porphyries Quartz-feldspar porphyries within the Porcupine gold camp occur over a length of approximately 100 kilometers along the PDDZ from Bristol Township in the east to Carr Township in the west with numerous porphyries spatially associated with gold mineralization {Fig. A2). As part of this project 28 different quartz-feldspar porphyry intrusions were examined during 2003 and 2004. These 28 intrusions are geographically and geologically grouped into five suites as shown on Fig. A2 and Table Al. The five suites are the: Timmins porphyry intrusive suite - main camp (TIS-main), Timmins porphyry intrusive suite-other (TIS-other), Carr Township porphyry intrusive suite (CIS), Holmer intrusive suite (HIS) and granodiorite intrusive suite (GIS). Descriptions of each suite are presented below. A.5.1 Timmins Porphyry Intrusive Suite - Main Camp The Timmins porphyry intrusive suite - main camp (TIS-main) of quartz-feldspar porphyries includes intrusions in the Porcupine gold camp within the immediate vicinity of South Porcupine and Timmins. This includes 18 porphyry intrusions located directly along the PDDZ, its immediate splay faults (e.g. Dome Fault Fig. A3) or along/proximal to the Hollinger shear zone (Fig. A4), between the Burrows-Benedict Fault (eastern boundary) and the Mattagami River Fault (western boundary) within Tisdale and Deloro Townships. Specific intrusions that were examined include the Dome Fault Zone, Preston, Paymaster, West (West Preston), Northwest (Paymaster South and Paymaster 2- 3), Edwards (Vedron) and Buffalo Ankerite #5 porphyry intrusions located in the immediate vicinity of the PDDZ (Fig. A3) and the Crown, Pearl Lake, Gillies Lake and Coniaurium porphyry intrusions located in the Immediate vicinity of the Holllnger shear zone (Fig. A4). Some porphyry intrusions within TIS-main are not included within this study due to inaccessibility to drill core or outcrops as a result of unsafe ground conditions (e.g. sink holes). These inaccessible intrusions include the Buffalo Ankerite, Aunor, Delnite, Millerton, Miller Lake, Acme and Northern porphyry intrusions. A.5.1.1 Field Relationships The 18 intrusions of the TIS-main form two southwest-northeast linear belts that approximately range from 4 to 8 kilometers long and 1 to 2 kilometers wide (Fig. A3 and A4). The intrusions of both of these belts plunge eastwards and coalesce at depth (E. Barr, Porcupine Joint Venture-PJV, personal communication, 2003; P. Harvey, PJV, personal communication, 2003). Although many of the TIS-main porphyry intrusions join at depth, these porphyry bodies may simple be apophyses of a larger batholith-scale intrusion that has yet to be identified. The TIS-main porphyries intrude into three different stratigraphic levels of the Tisdale Assemblage: 1) along the northern margin of the PDDZ (Buffalo Ankerite, Aunor and Delnite porphyries: Fig. Al); 2) below or at the Hersey Lake Formation - Central Formation contact (West, Northwest, Vedron and Buffalo Ankerite #5 porphyries: Fig. Al); and 3) into the Central and Vipond Formations (Dome Fault Zone, Preston, Paymaster, Crown, Pearl Lake, Gillies Lake and Coniaurium porphyries: Fig. Al). The intrusions lie subparallel to the volcanic stratigraphy and form numerous elongated, irregularly shaped porphyry bodies that are generally semi-conformable with stratigraphy except for the Preston Porphyry which crosscuts stratigraphy at a high angle. As well, the TIS-main porphyry intrusions show a weak correlation with pillowed units of the Tisdale Assemblage (i.e., the porphyry bodies have dominantly intruded into pillowed flows) and alteration zones, known within the camp as 'carb rock.' Furthermore, zones of deformation are also proximal to areas where the porphyry intrusions have been emplaced. For example, intrusions are present in deformation zones such as the PDDZ (e.g., Buffalo Ankerite, Aunor, Delnite, Naybob and Porphyry Hill intrusions: Fig. A3), the Dome Fault Zone {e.g., Dome Fault Zone, Preston and Edwards intrusions: Fig. A3), and the Hollinger shear zone (e.g. Pearl Lake and Coniaurium intrusions: Fig. A4). TIS- main intrusions are also located within fold hinges such as that of the Northern Anticline (Gillies Lake porphyry: Fig. A4: Ferguson et al. 1968; Piroshco and Kettles 1991). The porphyry intrusions of the TIS-main can be separated into three groups with respect to size and shape. The most common form of the intrusions is as small dikes, sills and plugs up to 1 kilometer long and 0.5 kilometer wide, but typically only a few hundreds of meters long and tens of meters wide. This form of intrusions include the Northwest, Edwards, Buffalo Ankerite #5, Crown, Gillies Lake and Coniaurium porphyries (Figs. A3 and A4). The second most common form of intrusions are elongate porphyries. For example, the Dome Fault Zone, Preston and Paymaster porphyries range from 1-2 kilometers long and 100-300 meters wide (Fig. A3). The third grouping encompasses the largest porphyry of the TIS-main, the West and Pearl Lake porphyries, which occur as oval shaped intrusions up to 2 kilometers long by 600 meters wide (Figs. A3 and A4). The TIS-main porphyry intrusions typically are in sharp intrusive or tectonic contact with the host Tisdale Assemblage mafic volcanic rocks (Dome Fault Zone, Preston, Paymaster, Northwest, Vedron, Buffalo Ankerite #5, Pearl Lake and Gillies Lake porphyries: Fig. A5A). Meter scale apophyses are present at both the Northwest and Edwards porphyries (Fig. A5B). Contact breccias occur along the margins of three TIS- main porphyries, including: 1) the northern contact of the Edwards porphyry, where subrounded porphyry fragments are present in a fine-grained chloritic matrix and form a flank breccia (Fig. A5C); 2) the western nose of the Paymaster porphyry where large (up to 15 centimeters in size), subangular flow banded porphyry fragments and large {up to 15 centimeters in size) subrounded mafic volcanic fragments are hosted within a fine grained chloritic matrix forming a basal breccia (Fig. A5D); and 3) the northern tip of the Crown porphyry where subrounded, stretched clasts of porphyry and mafic volcanic rocks are hosted within a fine-grained chloritic matrix forming a 'roof breccia (Fig. A5E). Mapping around this marginal breccia unit illustrates that the Crown porphyry breccia extends northward, cross-cutting stratigraphy (Fig. A6). A.5.1.2 Petrography The porphyry intrusions of the TIS-main are porphyritic textured and consist of 5- 45% modal percent quartz and feldspar phenocrysts in a ratio of 1 to 3 surrounded by a very fine grained, nearly aphanitic quartzo-feldspathic matrix (Fig. A5F). Quartz phenocrysts are generally subhedral in shape and are moderately to highly strained, ranging from 1-5 millimeters in size. Feldspar phenocrysts are anhedral to euhedral in shape and range in size from 1-8 millimeters.. Feldspar phenocrysts are dominantly plagioclase, although black orthoclase phenocrysts are present in the Gillies Lake porphyry (Fig. A5G). Accessory minerals are present in minor amounts within all the intrusions and include: 0.5 millimeter crystals of colourless apatite; up to lmillimeter 110 long blades of tourmaline; and submillimeter, subhedral to euhedral disseminated sulphide minerals. The sulphide minerals, which consist of pyrite and lesser pyrrhotite, chalcopyrite, molybdenite and bornite, occur as disseminated submillimeter grains, millimeter thick stringers, and three to four centimeter thick clusters (Fig. ASH). Foreign material including xenoliths of ultramafic rock that has undergone green-mica alteration (loosely termed 'carb rock') are present in most of the intrusions (Fig. A5I). These fragments are most abundant near the margins of the intrusions and are elongate parallel to the dominant structural fabric in the porphyries and country rocks. Flow banding defined by dimensional mineral alignment of plagioclase is present in the western nose of the Paymaster porphyry {Fig. A5J) and internal, hydrothermal breccias occur in the Pearl Lake porphyry and are distinguished by centimeter to decimeter fragments of porphyry within a feldspathic- to tourmaline-rich matrix (Fig. A5K). Metamorphic minerals are rarefy observed within the porphyry intrusions of the TIS- main. Although metamorphic biotite is reported in porphyries in the vicinity of the Dome Mine (Thompson 2003), none was observed in samples collected from the same porphyries and only stilpnomelane, which occurs as long blades up to one millimeter in length, was found within the Edwards porphyry (Fig. A5L). A.5.0 Alteration, Veining,and Mineralization The porphyries of the TIS-main have undergone different intensities and styles of alteration. The most common type of alteration that affects all of the porphyries of the TIS-main is white mica (sericite) alteration of feldsparphenocrystsan d their feldspathic matrices. Depending on the degree of alteration, feldspar phenocrysts can be almost pristine (Fig. A5M), relicted (Fig. A5N) or completely replaced (Fig. A40). The most Ill intense white mica alteration is present in the immediate vicinity of the Dome (Dome Fault Zone, Preston and Paymaster porphyries) and Hollinger-Mclntyre mines (Pearl Lake porphyry: Fig. A7). These porphyry bodies have undergone the most intense white mica alteration and are best described as quartz-sericite schists, rather than true igneous porphyries, as has historically been the case (e.g. Davies and Luhta 1978a). Often coupled with the white mica alteration, but also locally occurring within separate alteration zones, is calcium-carbonate alteration, which bestow a cloudy grayish-brown appearance to feldspars (Fig. A5P). Rocks that are often described as "bleached" exhibit the most pervasive calcium-carbonate alteration (Fig. A5Q), and like sericite alteration, carbonate alteration is strongest in the vicinity of the Dome and HoHmger-McIntyre mines. Chlorite alteration occurs in minor abundance in all of the intrusions as euhedral to anhedral laths up to 1 millimeter (Fig. A5R). Iron-carbonate (ankerite) alteration is also locally common (Fig. ASS), with the TIS-main porphyries west of the Dome mine along the Dome Fault exhibiting the most intense ankerite alteration (West, Northwest and Buffalo Ankerite #5). The Pearl Lake porphyry also contains zones of pervasive hematite (pink) and tourmaline alteration (Fig. A5K). Four different types of veins cut across the porphyry intrusions of TIS-main, including; quartz-tourmaline, quartz-ankerite, monomineralic quartz and quartz-calcium carbonate veins. Quartz-tourmaline veins are the most common, generally occurring as subvertical, north-northwest trending veins that crosscut stratigraphy and structural fabrics. The quartz-tourmaline veins are typically 10-30 centimeters wide (Fig. A5T) and 5-15 meters long, although smaller veins are observed in the Northwest porphyry. No alteration envelopes are present around the quartz-tourmaline veins. The second most 112 common vein type is quartz-ankerite veins. These veins are generally subparallel to stratigraphy and are 10-20 centimeters thick, but only 1-5 meters long. Alteration associated with the quartz-ankerite veins includes 10 centimeter wide zones of green mica in host rocks outside of the porphyry intrusions, and meter-scale pervasive ankerite alteration within the porphyry intrusions. Pyrite enrichment is typically associated with the ankerite alteration envelopes. The least common vein types are chaotic clusters of white, monomineralic quartz veins and sporadic, narrow, white quartz-calcium carbonate veins. These two types of centimeter thick veins are present in randomly oriented localized zones, and are not associated with alteration envelopes. Timing relationships between the four types of veins are not known. Both gold and copper mineralizations are spatially associated with the porphyries of the TIS-main which are all reported within historic mine workings. For example, the most southeastern of the porphyries of the TIS-main (Dome Fault Zone, Preston and Paymaster) join in a triple point precisely where the Dome Super Pit is located, and plunge in the same general direction as the mineralization (E. Barr, PJV, personnel communication, 2003). Likewise, gold enrichment in the Hollinger-Mclntyre mine trend is focused around the Pearl Lake porphyry (Fig. A7). However, although this tight spatial association between gold mineralization and porphyry intrusions of the TIS-main exists, the majority of historical gold production was sourced from mafic volcanic flows of the Tisdale Assemblage along the contacts of the porphyry bodies (Melnik-Proud 1992). Gold enrichment within the TIS-main also shows a strong association with sericite-carbonate altered porphyries with grades and generally bulk tonnage of gold deposits decreasing with intensity of alteration (Mason and Melnik 1986; E. Barr, PJV, 113 personnel communication, 2003). In contrast to gold, copper mineralization and historical production was from a hematite (pink) alteration zone (Fig. A5) bearing chalcopyrite and bornite from the centre of the Pearl Lake porphyry (Memik-Proud 1992). Gold veins typically crosscut the hematite alteration, suggesting that copper mineralization predated gold enrichment (Burrows and Spooner 1986). A.5.1.4 Deformation The porphyry intrusions of the TIS-main show varying degrees of deformation ranging from non-existent (e.g. Gillies Lake porphyry) to extremely intense (e.g. Pearl Lake porphyry). Specifically, the TIS-main porphyries show at least four generations of structural fabrics with varying degrees of intensity depending on the location of the porphyries with respect to main deformation corridors and on the abundance of alteration minerals that can define structural fabrics. The dominant fabric observed within the intrusions of the TIS-main is an east striking, steeply dipping, millimeter- to centimeter-scale spaced cleavage (Figs. A5U and A5V). This spaced cleavage is roughly parallel to the axial plane of regional folding (e.g. South Tisdale Anticline) that formed during a D3 deformation event (Bateman et al. 2008). An older, more penetrative foliation is observed within microlithons bounded by the younger D3 spaced cleavage discussed above. This older foliation likely formed during a D2 folding and thrusting deformation event (Figs. A5U and A5V: Bateman et al. 2O05, 2008). An east plunging (-50°) lineation is locally observed along the D3 spaced cleavage. This lineation is best expressed as a strong stretching lineation of clasts within a 114 heterolithic breccia that surrounds the Crown porphyry (Fig. A6B)r and is also present as a mineral lineation within the Pearl Lake porphyry. A crenulation cleavage also overprints the D3 spaced cleavage locally (Fig. A5Q). This crenulation cleavage is related to a localized D4 deformation event in the vicinity of the PDDZ (Bateman et al. 2008) The youngest structural fabric is a shallowly dipping to flat lying foliation observed within the Pearl Lake porphyry; this foliationi s related to the D6 deformation event which is suspected to be a result of late orogenic collapse (Bateman et al. 2004). A.5.1.5 Geochronology Results of U-Pb age dating were previously reported for six of the TlS-main intrusions. The Paymaster, Preston, Crown, Millerton and Pearl Lake porphyries have U- Pb zircon crystallization ages of2690±2 Ma, ca. 2690 Ma, 2688 ±2 Ma, 2691 ±3 Ma, and 2689 ±1 Ma, respectively, (Corfu et ai. 1989) and the Dome Fault Zone porphyry has an U-Pb zircon crystallization age of2688±2 Ma (Gray and Hutchinson 2001). Collectively, these ages suggest that the TIS-main intrusions were emplaced between 2686-2692 Ma. A.5.2 Timmins Porphyry Intrusive Suite - Other The quartz-feldspar porphyries of the Timmins porphyry intrusive suite - other (TIS- other) includes three geographical groups of intrusions that are not located in the main Timmins town site portion of the Porcupine gold camp. These three geographical groups are: 1) any intrusions west of the Mattagami River Fault that are along the possible westward extension of the PDDZ in Bristol Township and western Ogden Township (Figs. A2 and A8); 2) intrusive bodies south of the PDDZ which form part of the swarm of porphyry intrusions that surround the Shaw Dome in Deloro and Shaw townships 115 (Figs. A2 and A9); and 3) porphyry intrusions along the PDDZ west of the Burrows- Benedict Fault, from roughly South Porcupine east to Whitney, Hoyle and MacKlem Townships (Figs. A2 and A1G). The porphyry intrusions are from east to west, the Bristol Lake, South Bristol Lake, Bristol Township, northern Deloro Township dike swarm, Mt. Logano, Hoyle Pond, Aquarius Mine, Aquarius (previously described as a diorite by Corfu et al. 1989), Homestead, Pominex and Crowley porphyries (Figs. A8, A9 and AlO). A.5.2.1 Field Relationships TIS-other intrusions occur as individual intrusions (Mt. Logano and Hoyle Pond porphyries) or as east-west linear belts ranging from 1 to 7 kilometers long (Bristol Lake- South Bristol Lake-Bristol Township, northern Deloro Township dike swarm and Aquarius Mine-Aquarius-Homestead-Pominex-Crowley porphyries). The plunge of most of the intrusions is unknown except for the porphyries west of the Mattagami River Fault which plunge westwards (C. Dupont, Tom Exploration, personal communication, 2004). The TIS-main porphyries were emplaced semi-conformable to stratigraphy at three stratigraphic levels, including: 1) into the upper unit of the Deloro Assemblage calc- alkaline metavolcanie rocks (northern Deloro Township dike swarm and Mt. Logano porphyries: Figs. Al and A9);2) into the Hersey Lake and Central Formations of the Tisdale Assemblage tholeiitic metavolcanie rocks (Hoyle Pond, Aquarius Mine, Aquarius, Homestead, Pominex and Crowley porphyries: Figs. Al and A10); and 3) near or at the basal contact of the siliciclastic Porcupine Assemblage metasedimentary rocks and a thin sliver of the Tisdale Assemblage mafic metavolcanie rocks, south of the Kamiskotia Intrusive Complex (Bristol Lake, South Bristol Lake and Bristol Township 116 porphyries; Figs. Al and A8)» Structurally all of the TIS-other intrusions are located in the immediate vicinity to the PDDZ and/or its smaller splays. Some intrusions are also located along the margins of the Shaw Dome (northern Deloro Township dike swarm and Mt. Logano porphyries: Fig. A9) Like the porphyry intrusions of the TIS-main, the TIS-other displays multiple groupings of intrusions with respect to size and shape. Volumetrically most significant are large, oval shaped intrusions 4 to 6 kilometers long and approximately 2 kilometers wide and include the Bristol Township and Mt. Logano porphyries (Figs A8 and A9). The most common size and shape of intrusion within the TIS-other are small dikes, sills and plugs up to 1 kilometer in size. These types of intrusions include the northern Deloro Township dike swarm, Hoyle Pond, Aquarius Mine, Aquarius and Homestead porphyries (Figs. A9 and A10). The two other types of intrusions within the TIS-other are elongate porphyries ranging from 2 to 5 kilometers long and approximately 0.5 kilometers wide (Bristol Lake and South Bristol Lake porphyries: Fig. A8) and thin, regional dikes that are over 5 kilometers long but only a few tens to hundreds of meters wide (Pominex and Crowley porphyries: Fig. A10). The contacts of the TIS-other intrusions with surrounding host country rocks are generally sharp and either primary or fault controlled (Fig. Al 1A). Alteration can blur contact relationships and produce gradational contacts. For example, the contact zone between the Aquarius porphyry and surrounding volcanic rocks is 15 centimeters wide and is characterized by gradual transition from porphyry with very little chlorite, to chlorite-rich porphyry, to quartz-feldspar-rich chloritic volcanic rock, to chloritic volcanic rock (Fig. Al IB). Marginal breccias to TIS-other intrusions, similar to those 117 observed in the TIS-main (Figs. A5C, A5D and A5E% also occur along the margins of the Bristol Township porphyry (C. Dupont, Tom Exploration, personnel communication, 2004). A.5.2.2Petrography The TIS-other intrusions are porphyritic, containing quartz and plagioclase phenocrysts within a very fine, nearly aphanitic quartzo-feldspathic matrix (Figs. All'C and Al ID). Plagioclase phenocrysts are subhedral, vary in size from 1-6 millimeters, and constitute 5-35% modal percent of the rock. Quartz phenocrysts are euhedral to anhedral, weakly to moderately strained, vary in size from 1-3 millimeters and constitute 5-20% modal percent of the rocks (Figs. Al 1C and AMD). Accessory minerals include apatite, pyrite and chalcopyrite. Pyrite is the dominant sulphide mineral and occurs as trace to 5% modal percent of the rocks as euhedral to anhedral disseminated grains up to 1.5 millimeter in size, millimeter-thick stringers and centimeter sized clusters. Chalcopyrite is found with pyrite within the large Bristol Township porphyry as both millimeter-thick stringers and clusters up to a few centimeters in length. The Mt. Logano porphyry also contains internal breccias that consist of multiple centimeter-sized, rounded porphyry fragments within a porphyry matrix (Fig. Al IE), suggesting the Mt. Logano porphyry may be a composite intrusive body. Metamorphic minerals, such as biotite, chlorite and muscovite are present in trace amounts except for in the Aquarius porphyry which contains 2-3% modal percent, prograde biotite-muscovite metamorphic mineral clusters up to 1-3 centimeter wide that display rotation and chlorite retrograde metamorphism (Fig. Al IF). 118 A.5.23 Alteration, Veining, and Mineralization The TIS-other porphyry intrusions show various types and degrees of alteration. White mica alteration of feldspar phenocrysts and feldspathic matrices is the most common type of alteration. It varies from strong (10-20% modal percent) along the margins of the intrusions to weak (-2% modal percent) within their center. This type of alteration is characterized by clusters (Fig. Al 1G) and trains (Fig. Al 1H) of ~0.3 millimeter sericite blades (Fig. A12E) and depending on the degree of alteration, corroded and/or relict feldspar phenocrysts may or may not be visible. Often coupled with the moderate to strong white mica alteration is weak calcium-carbonate alteration. The calcium-carbonate alteration is recognizable by a bleached appearance in hand sample and a clouded brownish-grey appearance of feldspar phenocrysts and matrices in thin section (Fig. A10D). Weak to moderate chlorite alteration is the next most common alteration mineral present within the TIS-other porphyry intrusions, occurring as 0.5 to 2 millimeter anhedra^ subhedral and euhedral laths ranging from 2-20 modal percent (Fig. Al II). Less common, locally present alteration facies observed within the TIS-other intrusions include weak pervasive hematite alteration distinguishable by a light pink colouration (Bristol Township and Aquarius porphyries), patchy ankerite (Aquarius Mine porphyry) and strongly pervasive quartz and moderate albite alteration (Crowley and Pominex porphyries: Fig. Al 1J). Three types of veins are present in the TIS-other intrusions. The most common veins are 1-2 millimeter thick white quartz veinlets that have no systematic orientation and lack alteration haloes. The second and more significant vein type is white quartz with minor calcium-carbonate. These veins are northwest trending, centimeter- to decimeter-thick 119 (1-20 centimeters) and up to tens of meters in length., They are more abundant within the volcanic rocks that surround the porphyries. They locally contain angular wall rock fragments and are surrounded by pyrite ± chalcopyrite alteration haloes. The least common vein type, only observed with the Aquarius Mine porphyry, is quartz-ankerite veins. These veins are similar to the quartz - calcium carbonate veins discussed above, but they contain ankerite instead of calcium-carbonate. Gold mineralization is only associated with a few of the TTS-other intrusions, although all of the porphyritic intrusions have been the focus of exploration in the past. Gold mineralization shows the strongest spatial association with the strongly deformed, serieite-earbonate altered Hoyle Pond porphyry and with the ankerite-altered Aquarius Mine porphyry (R. Norman, Kinross Gold Corp., personal communication, 2004). Significant jjold mineralization is associated with quartz-pyrite veins within the large Bristol Township porphyry (~l-3g/t Au over up to 2 meters within various drill holes; C. Dupont, Tom Exploration, personal communication, 2004). Copper mineralization is also associated with the Bristol Township porphyry and is related to the presence of copper sulphide minerals (chalcopyrite) spatially associated with hematite alteration. No other TIS-other intrusions are known to contain evidence of copper mineralization except for the northern Deloro Township porphyry dike swarm which displays late copper mineralization In the form of quartz veins with approximately 5% chalcopyrite. A.5.2.4 Deformation The porphyry intrusions are overprinted by two distinct structural fabrics that vary in intensity as a function of location and abundance of alteration minerals. Similar to the TIS-main intrusions, the dominant structural fabric is a penetrative 1-3 millimeter spaced 120 D3 cleavage that trends east and is subvertical (Fig. A.11H). The second fabric is an older, penetrative foliation observed with microlithons between the D3 spaced cleavage planes and is subparallel to the D3 spaced cleavage,, is steeply dipping and is related to D2 regional deformation (Bateman et al. 2005, 2008). A.5.2.5 Geochronology The Bristol Township, Mt. Logano, Aquarius and Hoyle Pond porphyries have U-Pb zircon crystallization ages of 2687.7 ± 1.4 Ma for the Bristol Township porphyry (Ayer et al. 2003,) 2689.0±1.4 Ma for the Mt. Logano porphyry (MacDonald et al. 2005), 2705 ± 10 Ma for the Aquarius porphyry (Corfu et al. 1989) and 2684.4 ± 1.9 and 2687.2 ± 2.2 Ma for the Hoyle Pond porphyries (Ayer etal. 2005; Bateman et al. 2005: Table Al). The large error on the age of the Aquarius porphyry is due in part to scarcity of zircons combined with complex Pb loss and inheritance problems. Using the most robust U-Pb ages, these intrusions crystallized between 2690 Ma to 2683 Ma similar to the age of emplacement for the TIS-main intrusions. A.5.3 Carr Township Porphyry Intrusive Suite (CIS) The Carr Township porphyry intrusive suite (CIS) includes one large stock north of Matheson in Carr Township (Figs. A2 and A12). A.53.1 Field Relationships The Carr township porphyry has intruded the Porcupine Assemblage along the contact between the siliciclastic metasedimentary rocks of the Porcupine Assemblage and a thin sliver of mafic metavolcanic rocks that are most likely part of the lower to middle units of the Tisdale Assemblage (Figs. Al & A12). The Carr Township porphyry is the largest of all intrusive bodies investigated within this study. It is oval in shape and is 12 121 kilometers in length along its east-west axis and over 5 kilometers in width along its north-south axis (Fig. A12). The contacts of the Carr Township porphyry intrusive with its surrounding country rocks are generally sharp (Fig. ADA), although one observed contact consists of a one meter thick breccia with porphyry fragments( < 8 centimeters size) surrounded by a very fine-grained chloritic matrix that is similar in appearance to the chloritized mafic volcanic country rocks (Fig. ADB). A.5.3.2 Petrography The Carr Township intrusion is porphyritic with phenocrysts of plagioclase (5-35% modal percent) and quartz (5-20% modal percent) varying in size from 1 to 15 millimeters (Fig. ADC). The phenocrysts are euhedral to subhedral, and the quartz phenocrysts exhibit weak to moderate strain. The matrix that surrounds the phenocrysts consists of fine to very fine-grained quartzo-feldspathic material. Trace to 5% euhedral to subhedral pyrite ranges from disseminated ~1 millimeter grains to millimeter-thick stringers and centimeter sized clusters (Fig. ADD). Trace chalcopyrite is also present and is associated with pyrite stringers and clusters. The Carr Township porphyry also contains internal breccias that consist of multiple centimeter-sized, rounded porphyry fragments within a porphyry matrix (Fig. ADE), suggesting the Carr Township porphyry is a composite intrusive body. Minor greenschist grade metamorphic mineral assemblages (e.g. chlorite and biotlte) are indicators of metamorphism within the CIS. A.5.3.3 Alteration, Veining and Mineralization The CIS porphyry intrusion has a range of alteration types with differing intensities. The most prominent alteration present is weak to moderate white mica alteration ranging from 1-10% modal percent and occurs as submillimeter clusters and trains within the matrix of the porphyries (Fig. A13F). Chlorite alteration is the second most common alteration facies, occurring as disseminated 0.5 millimeter euhedral to subhedral laths typically near the margins of the CIS intrusion. Weak to moderate pervasive hematite alteration and silicification are also present locally. Two types of veins are present in the CIS. The most common veins are white quartz "sweats" that are 1-2 millimeter wide and are not accompanied by alteration of the surrounding wall rock. The second and more significant vein type is white quartz with minor calcium-carbonate. These types of veins are centimeter- to decimeter-scale in width, often accompanied by narrow wall roek alteration envelopes and sulphide mineralization. Both anomalous gold (over 0.5g/t) and copper are spatially associated with the CIS porphyritic intrusions as is implied by previous exploration drilling carried out by Kinross (gold) and Falconbridge (copper) on the intrusion. Most notable are anomalous copper values up to 2187 ppm copper collected and analyzed during this study (sample # 03-PJM-142i). The copper enrichment is spatially associated with hematite alteration zones and the presence of chalcopyrite with pyrite in stringers and centimeter sized clusters (Fig. A13D). A.5.3.4 Deformation The CIS intrusion is generally undeformed with only a localized, weak foliation along the sericite altered margin of the intrusion (Fig. A13F). Based on regional structural knowledge this weak foliation is likely related to D3 regional deformation (Bateman et al. 2008). 123 A£3£ Geochronology No published ages on the CIS intrusion exist. With that said, based on the lack of D2 deformation along with geological similarities to the TIS-main and TIS-other intrusions, the age of the CIS is speculated to be slightly younger, presumably circa 2670-2685 Ma. A.5.4 Holmer Intrusive Suite (HIS) The Holmer intrusive suite (HIS) includes three intrusions west of the Mattagami River Fault along the PDDZ (Fig. A2). These three intrusions are near the Timmins west mine site of Lake Shore Gold Inc., in Bristol Township, and included the Holmer porphyry, the Thunder Creek syenite and the Southwest Bristol Township syenite (Fig. A14). A.5.4.1 Field Relationships The three intrusions of the HIS form a northeast trending, near vertical linear belt approximately three kilometers long and 1 kilometer wide. The intrusions are generally subparallel to stratigraphy and are located along or near to the boundary between the Tisdale Assemblage metavolcanic rocks and the Porcupine Assemblage clastic metasedimentary rocks south of the Kamiskotia Intrusive Complex and are subparallel to the host stratigraphy (Figs. Al & A14; Vaillancourt et al. 2001) The three HIS intrusions are all relatively small compared to the other intrusive suites. The southwest Bristol Township syenite, which is approximately one kilometer in diameter and is round and plug like, is the largest of the three intrusions (Fig. A14). The Holmer porphyry and Thunder Creek syenite are tabular in shape, up to 500 meters in length and a few tens to a hundred meters in width (Fig. A14). Contacts between the HIS intrusions and country rock are generally sharp. The Holmer porphyry locally has a heterolithlc breccia exposed in drill core, consisting of angular blocks of porphyry, mafic volcanic rocks and siliciclastic metasedimentary rocks up to a few meters in size (Fig. Al 5 A). A.5.4.2 Petrography The three intrusions of the HIS have porphyritic to equigranular textures. The Holmer porphyry contains 10-25% modal percent plagioclase phenocrysts, l-5mm in size, and 5-20% modal percent moderately strained, euhedral to subhedral quartz phenocrysts, 1-3 mm in size, within a fine grained quartzo-feldspathic matrix (Fig. A15B). The Thunder Creek syenite is similar, but contains slightly less quartz (1-5% modal percent) as well as clusters of intergrown, 1-2 millimeter equigranular feldspars (orthoclase and plagioclase) that are up to three centimeters in size (30-40% modal percent). The southwest Bristol Township syenite comprises, fine to medium grained, interlocking orthoclase (60-70% modal percent) and plagioclase (30-40% modal percent)* which are up to 3 millimeters in size (Fig. A15C). Pyrite is the dominant sulphide mineral and it occurs as euhedral to anhedral, up to 3 millimeter in size,, disseminated grains (trace to 5%). Arsenopyrite is present as submillimeter euhedral crystals within the Holmer porphyry. No metamorphic indicator minerals were identified within the HIS by this study. A.5.4.3 Alteration, Veining, and Mineralization The intrusions of the HIS show various types and degrees of alteration. The intrusions all display varying degrees of sericite alteration, ranging from weak to moderate (2-15% modal percent) and depending on the degree of sericite alteration, feldspar phenocrysts may appear corroded (Fig. A15C). Weak to moderate chlorite alteration is the second most common alteration fades, occurring as 0.5 millimeter anhedral to subhedral laths ranging from 2-10% modal percent. Similar to other intrusive suites, very weak calcium-carbonate alteration is associated with sericite alteration locally and is recognizable by a clouded brownish-grey appearance of feldspar phenocrysts and matrices in thin section (Fig. A15C). The three HIS intrusions also locally display ankerite and hematite alteration ranging from weak to moderate in intensity, and identified by orange-brown and pink colouration in hand samples, respectively. Minimal quartz venting is present within the three FES intrusions. The most common vein type is white quartz veins with minor calcium-carbonate ranging from one and ten centimeters wide with minor pyrite (±chalcopyrite) enrichment within their vein envelopes; the timing of these veins is uncertain. A second type of vein observed within the HIS is millimeter thick white quartz veinlets, best described as quartz sweats. Although no gold mine is directly associated with the intrusions of the HIS, a drill intercept across the Thunder Creek syenite yielded 11.20 grams/tonne gold over 10.4 meters (Lake Shore Gold December 16, 2008 press release). The other two intrusions are not enriched in gold. A.5.4.4 Deformation Where observed, the HIS intrusions generally show little to no deformation. One weakly developed 1-3 millimeter spaced cleavage was observed within the intrusions of the HIS. This structural fabric is steep dipping and generally strikes east-northeast/west- southwest and is interpreted as a D3 fabric following Bateman et at. (2008). 126 A.5.4-5 Geochronology An age of emplacement for the three HIS intrusions are unknown as there are no published U-Pb zircon dates. However, the HIS is hypothesized herein to be younger than the other suites due to a lack of D2 deformation fabrics with an emplacement age ranging between 2665-2675 Ma, presumably similar to the emplacement ages of other magmatic events throughout the Abitibi Subprovince (Corfu et al. 1989; Ayer et al. 2002a). A.5.5 Granodiorite Intrusive Suite (GIS) The granodiorite intrusive suite (GIS) consists of four intermediate to felsic intrusions located along the PDDZ, including two south and two east of the Timmins town site (Figs. A2, A17 and A17). Two of the four intrusions, the Naybob porphyry and porphyry hill intrusions, are located in Tisdale and Ogden townships, respectively, south of Timmins (Fig. A16); the other two, the Pamour porphyry and Bob's Lake granodiorite intrusions are located in Whitney Township, east of Timmins (Fig. A17). A.5.5.1 Field Relationships Each group of the GIS intrusions consists of one large plug-like intrusive body and one smaller dike-/sill-like intrusive body. In the ease of the south of Timmins GIS intrusions the porphyry hill intrusions is the large plug-like intrusive body, approximately 500 by 200 meters in size, and the Naybob porphyry is the dike-/sill-like intrusive body approximately 500 meters long, but only up to a few tens of meters wide (Fig. A16). The Bob's Lake granodiorite, east of Timmins, is the large, plug-like body and is elongate in shape, over 5 kilometers long and up to 2 kilometer wide (Fig. A17). The Pamour porphyry intrusion is the dike-/sill-like body is up to 1 kilometer long and 100 meters wide (Fig. A17). All of the GIS intrusions have intruded either the Tisdale or Deloro Assemblages (Fig. Al). The south of Timmins GIS intrusions were emplaced into the basal units of the Tisdale Assemblage roughly parallel, to the Hersey Lake Formation-Central Formation contact, in deformation zones immediately north of the PDDZ (Figs. Al and A16). The east of Timmins GIS intrusions were emplaced subparallel to but lower in the stratigraphy, approximately at the Tisdale-Deloro assemblages boundary (Figs. Al and A17). Where observed, all of the GIS intrusions have sharp intrusive or tectonic boundaries with the host lhhologies/stratigraphy. A.5.5.2 Petrography The intrusions of the GIS display both porphyritic (Figs. A18A and A18B: Naybob and Pamour porphyry intrusions) and equigranular textures (Figs. A18C and A18D: porphyry hill and Bob's Lake granodiorite intrusions). Phenocrysts of plagioclase (10- 30% modal percent) and quartz (10-20% modal percent) in the porphyritic intrusions range from 1-6 millimeter long (Figs. A18A and AI8B). Plagioclase phenocrysts occur as euhedral to subhedral grains, ranging from unaltered (Fig. A18A) to weakly altered, occurring as corroded phenocrysts (Fig. A18B). The quartz phenocrysts are euhedral to subhedral with weak to moderate strain extinction. The matrix that surrounds the phenocrysts consists of fine-grained quartzo-feldspathic material, typically coarser than the TIS intrusions. The equigranular Porphyry hill and Bob's Lake granodiorite intrusions (Figs. A18C and A18D) consists of 60% modal percent, 1-5 millimeter, subhedral to euhedral plagioclase; 30% modal percent, 1-2 millimeter, interstitial, weakly 128 strained quartz; and 10% modal percent fine grained quartzo-feldspathic matrix. Accessory minerals are present in minor amounts within all the intrusions include: 0.5-1 cm laths of biotite and muscovite; 0.5 millimeter crystals of colourless apatite; and submillimeter, subhedral to euhedral pyrite crystals that are disseminated throughout the intrusions. Metamorphic minerals are present in at least one of the GIS intrusions (Pamour porphyry). Biotite ranges from 10-20% modal percent of the Pamour porphyry and occurs as disseminated submillimeter, subhedral laths and 5-20 millimeter clusters (Fig. Al&E). Retrograde chlorite is also present in the Pamour porphyry and partially replaces biotite. Biotite and muscovite observed in the other intrusions maybe metamorphic in origin, but are interpreted to be primary and magmatic in origin because they are intergrown with quartz and feldspar crystals. A.5.5.3 Alteration, Veining, and Mineralization The GIS intrusions have a range of alteration types with differing intensity. The most prominent alteration present is white mica (sericite) alteration which ranges weak to moderate (from 1-10% modal percent) and occurs as corrosion of feldspar crystals (Fig. A18B)and as submillimeter clusters and trains within the matrices of the porphyries. One-centimeter wide clusters of muscovite in the Bob's Lake granodiorite are interpreted as primary magmatic mica, as discussed above. Coupled with the white mica alteration within the Naybob porphyry is calcium-carbonate alteration, typically resulting in the feldspathic mineralogy having a cloudy grayish-brown appearance, and in hand sample as a "bleached" appearance. Chlorite alteration is the second most common alteration facies being developed locally in most of the intrusions. The chlorite occurs as disseminated 1 millimeter subhedral laths, and is most prevalent within the Pamour porphyry but is interpreted as metamorphic in origin, not an alteration product, as it appears to be a result of retrograde metamorphism replacing biotite as discussed above. Iron-carbonate (ankerite) alteration was also observed weakly and locally within the Naybob porphyry intrusion. Two types of veins are present in the GIS intrusions. The most common veins are white quartz "sweats", 1-2 millimeter wide, not accompanied by alteration of the surrounding wall rock. The second vein type is white quartz with minor calcium- carbonate. These types of veins are typically centimeter-scale in width, and often are accompanied by wall rock alteration and minor sulphide mineralization. Three of the four intrusions of the GIS display a spatial association to gold mineralization, and none of the GIS are associated with copper mineralization. Both the Naybob and the Pamour porphyries are located in the vicinity to historical mine workings (Naybob and Pamour mines, respectively) with the Naybob displaying the tightest association with mineralization, being present within the historical mine working of the Naybob mine. The Porphyry hill intrusion is within the immediate vicinity of historical exploration work but not in the vicinity to a historical resource. The Bob's Lake granodiorite intrusion has no association to gold mineralization. A.5.5.4 Deformation Only the Pamour porphyry of the GIS displays significant structural fabrics. The other intrusions only display very weak indications of deformation. The structural fabric within the Pamour porphyry is a weak to moderately penetrative foliation developed near the margins of the intrusion. The exact orientation of the fabric is unknown as the intrusion was only examined in poorly oriented drill core, although it is suspected to be related to D3 regional deformation as this event was the most prevalent within the Porcupine camp. A.5.5.5 Geochronology Out of the four intrusions included in the GIS, only the Pamour porphyry has a U-Pb age. MacDonald et al. (2005) reported an age of 2677.5 ±1.0 Ma for the Pamour porphyry, but due to a diverse population of zircon grains that were not of high quality, this age was suggested as a minimum age; and is interpreted to represent the primary age of emplacement for the entire GIS (Table Al). Geological observation's including the degree of alteration and deformation in comparison to other intrusive suites substantiates this interpretation (Table Al). A.6 Geology: The Felsic Volcanic Suite (FVS) The Krist Formation at the base of the Porcupine Assemblage fills structural basins (Porcupine and Kayorum Syncline) to an approximate thickness of 200 meters (Fig. Al: Brisbin 2000). Two fundamental questions within the Timmins camp are: do the felsic volcanic rocks located south of the PDDZ have Krist Formation affinities?; and what is the relationship between the porphyries and the Krist Formation? In an attempt to test these relationships, the Krist Formation was briefly examined and sampled at three localities as to be compared with the porphyry intrusions. The three locations are shown on Fig. A19 and include outcrops within the Porcupine Syncline near a power line along the southern side of Highway 101 between Schumacher and South Porcupine; the Kayorum Syncline in a small outcrop within a trailer park between the Shania Twain Centre and Moneta Road; and a thin band of felsic volcanic rocks south of the PDDZ 131 (herein termed south of PDDZ) along the northern edge of the Shaw Dome, directly south. of the Aunor Gold Mine. Because it is unsure whether all of the felsic rocks are of Krist Formation affinity the sampled units are collectively termed the felsic volcanic suite (FVS). A.6.1 Field Relationships and Petrography The Porcupine and Kayorum Syncline exposures of the FVS are dominantly a volcaniclastic package that is composed of rounded pyroclastic felsic volcaniclastic rocks that consist of subroundedto rounded porphyry fragmentsu p to a few centimeters in size supported in a feldspar-phyric, intermediate to felsic, lapilli tuff matrix (Fig. A20A). Mafic volcanic fragments, similar in size and shape to the porphyry fragments, are locally observed near the base of the FVS unit within the Kayorum Syncline (Fig. A20B). Angular to subrounded sulphide (pyrite) fragments up to two centimeters in size are also common in both the Porcupine and Kayorum Synclines (Fig. A20C). The matrix contains minor quartz phenocrysts, with alteration minerals including white mica and chlorite. The south of PDDZ outcropping of FVS consists of a lapilli tuff with no porphyry or mafic clasts. A.6.2 Alteration, Deformation, Veining and Mineralization Alteration of the FSV includes weak to moderately developed sericite-carbonate alteration. This alteration assemblage affected the feldspathic portion of the matrix predominantly, resulting in a cloudy brownish-grey appearance of feldspars in thin section (Fig. A20D). Minor chlorite alteration is present within the FSV as well. A spaced D3 cleavage is present within all of the FSV localities (Bateman et al. 2008), and there is also a strong eastward plunging stretching lineation of clasts (Fig. 132 A20E). The generation of deformation that resulted in this stretching of clasts is unknown (Bateman et al. 2004). No significant veining or mineralization is associated with the FVS, although the sulphide fragmentspresen t within the Kayorum syncline exposure of the FVS do contain minor chalcopyrite. A.6.3 Geochronology Ayer et al. (2002b) presented crystallization ages of 2687.3 ±1.6 Ma for a felsic lapilli tuff within the Porcupine Syncline and 2687.5 ±1.3 Ma for a felsic tuff within the Kayorum Syncline (Table Al). The FVS south of the PDDZ is likely much older with an U-Pb age similar to another felsic unit at the top Deloro Assemblage surrounding the Shaw Dome that is dated at 2724.1 ±3.7 Ma (Ayer et al. 2005; Bateman et al. 2005, 2008). A.7 Comparison of Porphyry Trends The porphyry intrusions of the TIS-main and TIS-other are spatially associated with the majority of the gold deposits of the Porcupine gold camp (the Hollinger-Mclntyre, Dome and Hoyle Pond Mines) and because of this are the datum to which the CIS, HIS and GIS are compared. To begin, however, a comparison of the TIS-main and TIS-other is warranted. Many similarities exist between the TIS-main and TIS-other. Both trends exhibit similar field relationships, petrology, alteration, veining, deformation and geochronology as shown in Table A2 Gold mineralization is also similar in style within both of the trends, with the majority of enrichment spatially related to porphyry intrusions that have undergone sericite alteration. Copper mineralization is present only in the largest intrusions within both the TIS-main and TIS-other. The presence of hematite alteration accompanied by chalcopyrite and bornite is likely an important factor in copper enrichment (i.e., oxidized Cu-bearing fluids: Gorman et al. 1981). The CIS has some similarities in terms of their field relationships, petrology, alteration, veining, deformation, mineralization and deformation and to gold-bearing intrusions of the TIS-main and TIS-other (Table A2). Notable differences include the larger size of the CIS intrusion, the larger phenocrysts within the CIS, the lack of intense sericite alteration and suspected younger emplacement age (>5 Ma). Copper-bearing samples from the CIS have hematite alteration and copper sulphide minerals similar to copper-related intrusions of the TIS-main and TIS-other. The HIS suite intrusions are distinct from the gold-related intrusions of the TIS-main and TIS-other (Table A2), in that they are texturally distinct (e.g. equigranular), have little or no alteration and deformation, and a suspected emplacement age difference of >10 Ma. The GIS intrusions have many similarities to the TIS-main and TIS-other intrusions but also have distinctive differences (Table A2). The similarities include field relations, petrology/mineralogy, alteration and veining. Major differences that separate the suites are metamorphic assemblages, gold and copper mineralization, deformation and emplacement age (Tables Al and A2). A.8 Comparison of the Felsic Volcanic Suite and Porphyry Intrusions The relationship between the porphyries and the felsic volcanic suites, particularly the Krist Formation, has been a long-standing question in the Porcupine gold camp. The results of this study illustrates that the felsic volcanic suite (at least Krist Formation 134 members of the FVS) and the porphyries are similar in terms of their petrography and U- Pb ages. For example, the matrix of the volcaniclastic rocks and the lapilli tuffs of the felsic volcanic suite is identical to the mineralogy of the TIS-main and TIS-other intrusions. The felsic volcanic suite also contains similar secondary mineralogy and alteration as the porphyries. For example, they have secondary/alteration-related white mica, chlorite, calcium carbonate and pyrite, as do the porphyries in the TIS-main and TIS-other. Furthermore, the rounded porphyry and mafic volcanic fragments in the felsic volcanic suite are similar to the marginal breccias observed in many of the TIS-main and TIS-other porphyry trends. In addition to their field characteristics, U-Pb dating results from the Krist Formation within the Porcupine and Kayorum Synclines suggests the crystallization age (2687 Ma.; Ayer et al. 2002b) are coeval with the vast majority of dated porphyry magmas (2687- 2691 Ma.; Marmont and Corfu 1989; Corfu et al. 1989; Gray and Hutchinson 2001; Ayer et al. 2002b, 2003; MacDonald et al. 2005). In summary, the felsic volcanic suite in part represents field and temporal counterparts to the porphyry intrusions and suggests that it is the extrusive equivalent to the porphyries of the TIS-main and TIS-other intrusions. As such the TIS-main and TIS- other intrusions should be viewed as an intrusive part of the Porcupine Assemblage. It is notable that no parental vent, or vents, or, conduit systems that may have been the eruptive source for the felsic volcanic suite have been found; it is possible however, that the elongate porphyry trends may mark the subvolcanic roots of fissures that have had their surface expressions eroded off. 135 A.9 Summary The main results of the field-based and petrographic portion of this thesis include: • The porphyry intrusive suites of the Porcupine gold camp generally form east- west trending belts ranging that are composed of multiple bodies and that vary in length from 4 to 20 kilometers long. The intrusions vary in size and shape from small dikes that are a few hundred meters long to oval bodies that are up to 11 kilometers in length. The porphyry intrusive suites generally intrude into the Vipond Formation of the Tisdale Assemblage, but also at the Deloro-Tisdale and Tisdale-Porcupine Assemblages contacts. The porphyry intrusive suites are generally semi-conformable to stratigraphic contacts. The margins/contacts between the porphyry intrusive suites and host stratigraphy are generally sharp, although breccia zones do exist, and transition zones are rarer. • Petrographically, the intrusive suites are composed of dominantly porphyritic, but also include aphanitic and equigranular textural variations. Phenocrysts of plagioclase and quartz typically are 2-3 millimeter in size but range up to 15 millimeter in the CIS. Accessory and sulphide minerals include apatite, tourmaline, pyrite, chalcopyrite, pyrrhotite, bornite and arsenopyrite. Foreign clasts (xenoliths and wall rock fragments that are now mostly altered to green mica) are common in the TIS-main and TIS-other intrusions and range up to 10 centimeters in length. Metamorphic minerals include stilpnomelene in the TTS- main and prograde biotite (retrograded by chlorite) locally occurs in some of the TIS-other and GIS intrusions. 136 • The most common alteration minerals are sericite and associated calcium- carbonate. Chlorite, iron-carbonate, hematite, leucoxene, silica and albite are present in various intrusions. • Gold mineralization within the intrusive suites is most strongly associated with sericite ± calcium-carbonate alteration, and displays a weaker association to iron- carbonate. Copper mineralization is associated with hematite alteration and copper-sulphide minerals. • Many of the intrusive suites examined display structural fabrics associated with the D2 deformation event and most have a structural fabric associated with D3 deformation event described by Bateman et al. (2005, 2008). • Timing of emplacement of the porphyry intrusions is the strongest reason to split them into different suites. The TIS-main and TIS-other dominantly occurred between 2687 and 2691 Ma (Marmont and Corfu 1989; Corfu et al. 1989; Gray and Hutchinson 2001; Ayer et al. 2002b, 2003; MacDonald et al. 2005), although the Aquarius porphyry was emplaced at 2705 Ma (Corfu et al. 1989) and the Hoyle Pond porphyry at 2684.4 Ma (Bateman et al. 2005). The CIS and HIS are interpreted to be younger based on field observations and the Pamour porphyry, emplaced at 2677.5 Ma (MacDonald et al. 2005) is interpreted to represent the emplacement age of the GIS. • Petrology and geochronology suggest that the TIS-main and TIS-other porphyry intrusions are genetically related to the felsic volcanic suite (Krist Formation). The porphyry intrusions represent the subvolcanic equivalents of the Krist Formation and should be viewed as part of the Porcupine Assemblage. A.10 References Ayer, J.A., Berger, B.R. and Trowell, N.F. 1999a. 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Relationship of Gold Mineralization to Stratigraphy and Structure in Timmins and Surrounding Area; in Genesis of Archean, Volcanic Hosted Gold Deposits; edited by Pye, E.G. and Roberts, R.G.: Ontario Geological Survey, Miscellaneous Paper 97, p. 1-15. Pyke, D.R. 1982. Geology of the Timmins Area, District of Cochrane: Ontario Geological Survey, Geological Report 219, 14lp. Robert, F. 2001. Syenite-associated disseminated gold deposits in the Abitibi greenstone belt, Canada: Mineralium Deposita, v.36, p.503-516. Thompson, P.H. 2003. Discover Abitibi. Metamorphic Subproject. Metamorphism and its relationship to Gold Deposits in the Timmins-Kirkland Lake Area, Western Abitibi Greenstone Belt, Ontario: Report 1; in Summary of Field Work and Other Activities 2003: Ontario Geological Survey, Open File Report 6120, p.37-1 to 37-8. Thurston, P.C., Ayer, J.A., Goutier, J., and Hamilton, M.A. 2008. Depositional gaps in Abitibi greenstone belt stratigraphy: A key to exploration for syngenetic mineralization: Economic Geology, v. 103, p. 1097-1134. Vaillancourt, C, Pickett, C.L. and Dinel, E. 2001. Precambrian geology, Timmins West - Bristol and Ogden Townships: Ontario Geological Survey, Preliminary Map P.3436, scale 1:20 000. Wells, R.C. 2001. Petrographic, lithogeochemical and interpretative report on a porphyry sample suite, Dome mine area. Internal, unpublished report for Placer Dome Ltd., 32p. Wood, PC, Burrows, D.R., Thomas, A.V. and Spooner, E.T.C. 1986. The Hollinger- Mclntyre Au-Quartz Vein System, Timmins, Ontario, Canada; Geologic Characteristics, Fluid Properties and Light Stable Isotope Geochemistry; in Proceedings of Gold '86: An International Symposium on the Geology of Gold; edited by A.J. Macdonald. Toronto, p.56-80. 142 Timiskaming Assemblage: Dominantly composed of interbedded medium- to coarse-grained siliciclastic metasedimentary rocks. Unconformity Porcupine Assemblage: Beatty Formation Dominantly composed of turdibidic fine- to medium-grained siliciclastic metasedimentary rocks. Krist Formation Dominantly composed of intermediate to felsic conglomeritic volcaniclastic, lapilli tuff and lappillistone rocks. Unconformity Tisdale Assemblage: Gold Centre Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanie flows. Vipond Formation Dominantly composed of Fe-tholeiitic amygdaloidal, variolitic, and brecciated massive -•- and pillowed mafic metavolcanie flows. Central Formation Dominantly composed of Mg-tholeiitic amygdaloidal, variolitic, and brecciated massive and pillowed mafic metavolcanie flows. Hersey Lake Formation Dominantly composed of komatiitic to basaltic- komatiite metavolcanie flows. Porcupine-Destor Deformation Zone Deloro Assemblage: Dominantly composed of mafic, calc-alkaline metavolcanie flows interbedded with felsic volcaniclastic and banded iron formations at the top. Stratigraphic horizons at which +iPorphyr y Intrusions occur. Figure Al. Stratigraphic column of the Porcupine gold camp, Abitibi greenstone belt, displaying stratigraphic horizons of porphyry intrusions. Assemblages included are the Deloro, Tisdale, Porcupine and Timiskaming (modified from Pyke 1982; Ayer et al. 2002b). Maximum thicknesses of Assemblages is presented excluding the Deloro Assemblage. 143 Figure A2. Simplified regional geological map displaying the location of differing Assemblages within the Abitibi greenstone belt in the vicinity of the Porcupine gold camp, Timmins, Canada (modified from Ayer et al. 1999a, 1999b). Map also highlights the Porcupine intrusive suites examined for this study. 144 (£ Paymaster" frfft porphyry Dome Fault Zone Edwards porphyry porphyryH Northwest porphyry Ii^i Aunor W^ porphyry i ^^ Legend H Porphyry Suite I °"3 Krist Formation K=rH Timiskaming Assemblage \^\ Tisdale Assemblage t~~-—I r» ^ r —\"" Fold - Anticline Kilometers .••*\"'" Fold - Syncline 477000 484000 Figure A3. Simplified surface geological map showing the names and location of some of the intrusions of the Timmins porphyry intrusive suite - main camp (modified from Ferguson 1966; Brisbin 1997; Vaillancourt et al. 2001). 145 476000 477000 478000 479000 Legend Porphyry Suite Beatty Formation \„%°\ Krist Formation l^^~\ Tisdale Assemblage formation contacts *• Fold - Anticline v- Fold - Syncline 477000 479000 Figure A4. Simplified surface geological map showing the names and locations of some of the intrusions of the Tiinmins porphyry intrusive suite - main camp (modified from Ferguson 1966; Brisbin 1997). 146 (C) (D) ».:,r?5*!'_iv-— Porphyry; (E) Figure AS. Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - main camp: A) Sharpe contact of porphyry intrusions and host mafic volcanic rocks, Gillies Lake porphyry; B) 2 meter long transposed dike off of larger porphyry intrusions, north of Vedron; C) Porphyry fragments within chloritic matrix, Edwards porphyry; D) Basalt (white arrow) and porphyry (black arrow) fragments within chloritic matrix, Paymaster porphyry; E) Porphyry fragments within a chloritic matrix, Crown porphyry; and F) Porphyritic texture with feldspar and quartz phenocrysts within a quartzo-feldspathic matrix, Gillies Lake porphyry. 147 / • y- fmn-D •! _(H)_ o-o o-^7 5V»2navutTuftnaav? # (L) "Mgmir® AS, .„ Photographs and photomicrographs showing features of the Timoiins porphyrr y intrusive suite - main camp: G) Black orthoclase phenocrysts (white arrow) within Gillies Lake porphyry; H) Sulphide (pyrite and chalcopyrite) cluster within Pearl Lake porphy ry; I) Large foreign (green mica) fragment within porphyry intrusion, Edwards porphy ry; J) Flow banded lobe, Paymaster porphyry; K) Sericite and hematite-altered of porphyry within a tourmaline rich matrix, Pearl Lake porphyry; and L)Sti :ene blades within a aphanitic quartz-feldspathic matrix, Edwards porphyry, PPL, scale = 1.5cm: 1mm. 148 Figure A5, continued. Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - main camp: M) Cloudy grey feldspar phenocrysts within weakly altered porphyry, Gillies Lake porphyry, PPL, scale = lcm:2mm; N) Relict feldspar phenocrysts that has undergone partial (near complete) sericite replacement (alteration), Preston porphyry, XPL, scale = 1cm: Imm; O) Complete sericite replacement (alteration) of feldspar phenocrysts yielding quartz-sericite schist, Preston porphyry, XPL, scale = 1cm: lmm; P) Carbonate altered porphyry displaying clouded grey appearance, Paymaster porphyry, XPL, scale = 1cm: 1.5mm; Q)Strongly calcium-carbonate (bleached) altered porphyry, displaying late crenulation of dominant spaced cleavage, Pearl Lake porphyry; and R) Subhedral chlorite grain, Edwards porphyry, scale = lcm:lmm. 149 Figure AS, continued. Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - main camp: S) Iron-carbonate (ankerite) alteration of porphyry with a small ankerite veinlet (white arrow), Buffalo Ankerite #5 porphyry; T) Quartz-tourmaline vein, Edwards porphyry; U) Well developed D2 and D3 spaced cleavages, Buffalo Ankerite #5 porphyry; and V) Strongly sericite-calcium carbonate ("dirty") altered porphyry displaying D2 and D3 spaced cleavages, Pearl Lake porphyry, PPL, scale = lcm:1.5mm. 476450 476500 476550 476600 476650 -4- 476450 476500 476550 476600 476650 Figure A6. Surface geological map of the Crown porphyry breccia, Shania Twain Centre (modified from Ferguson 1966; Brisbin 1997), 151 476000 477000 478000 479000 • i i- i 476000 477000 478000 479000 Figure A7. Map showing location of Holliager-Mclntyre gold mineralization and sericite~caleium carbonate alteration relative to part of the Tirnmins porphyry intrusive suite -main camp (modified from Mason and Melnik, 1986). 152 464000 465000 466 458 000 45900 0 460,000 461,000 462000 463000 • • 000 467000 000 9 \ J ) 500 0 53 6 # 400 0 53 6 A ^ s 300 0 53 6 ^Sj* m m 0 53 6 £ ^AW^M o ^ Bristol Lake S to CM ^V H m to porphyry > m^ • 100 0 ^ i m':-y m to •a 1 i • W in E^*"' -". Bristol Township porphyry ooo o 5 : J to \ •-•.••ITS.-':- • [:• • •• -i 1 *• *• ' rn A *"•' mSouth Bristo l '•'•'••' '•'.'• m o Lake porphyry : o> ^ - * « .' • - • •-.-.•.. .i . m » ~ Legend * - •II Porphyry Suite •'.:'•••':'• • *•.".' 800 0 53 5 / lv (.-• •]„...... 1.- •] rorcupme Assemoiage r in in in * :.*." •. •,•" y o '•'.'•".•' Tisdale Assemblage n o - 1 I , » ' Fault tt in m .#1 • •- •*.'.- •'.'' «o in o .' '• '• ""•'."".' Kilometers — 0 1 2 3 4 to ^ in 356 0 -V ^ m 45800J0 45900 0 460000 461000 462000 463000 464000 465000 466000 467000 in Figure A8. Simplified surface geological map showing the names and locations of some of the Timmins porphyry intrusive suite - other (modified from Ayer et-ai 1999a, 1999b; Vaillancourt et al. 2001). 153 476000 478000 486000 488000 490000 492000 494000 476000 478000 480000 482000 484000 486000 488000 490000 492000 494000 Figure A9. Simplified surface geological map displaying the names and locations of some of the Timmins porphyry intrusive suite - other (modified from Ayer et al. 1999a, 1999b; Hall et al. 2003, 2004). 154 490000 500000 510000 520000 530000 490000 500000 510000 520000 530000 540000 488000 490000 492000 B 504000 506000 508000 510000 512000 -.' -. • •* -. •T^fet ' '." • Kilometers . ; - • ". b '•.•"-' Homestead Pominex '. I Hoyle Pond IDs m Aquarius porphyry porphyry - V^ porphyry r4oo o m i CO m Aquarius ^ Mine porphyry Crowley o porphyry 1 r ' 504000 506000 508000 510000 512000 _^ Legend ^^B Porphyry Suite I I Tisdale Assemblage h .'• "I Porcupine Assemblage Kidd-Munro Assemblage I Kinojevis Assemblage I//V1 Deloro Assemblage 488000 490000 492000 Major Fault Figure A10. Simplified surface geological map showing the names and locations of some of the Timmins porphyry intrusive suite - other (modified from Ayer et al. 1999a, 1999b; unpublished Kinross Gold Corp. - Echo Bay Mines Ltd. map, 2004). 155 Figure AH. Photographs and photomicrographs showing features of theTimmins porphyry intrusive suite - other: A) Sharp contact between porphyry dike and host mafic volcanic rocks, northern Deloro Township porphyry dike swarm, scale = lem:2m; B) Transitional (gradational) contact between porphyry intrusions and mafic volcanic rocks, Aquarius porphyry, scale = lem:5cm; C) Porphyritic texture with feldspar and quartz phenocrysts within a quartzo-feldspathic matrix, Bristol Township porphyry, scale — lcm:2mm; D) Porphyritic texture with feldspar and quartz phenocrysts within a quartzo-feldspathic matrix, northern Deloro Township porphyry dike swarm, XPL, scale = lcm:2mm; E) Subrounded porphyry fragments within a similar porphyry matrix, Mt. Logano porphyry; and F) Rotated large biotite-muscGvite cluster, Aquarius porphyry. Figure All, continued. Photographs and photomicrographs showing features of the Timmins porphyry intrusive suite - other: G) Moderately sericite altered and replaced feldspar phenocrysts within a very fine grained quartzo-feldspathic matrix, Mt. Logano porphyry, XPL, scale = 1.5cm: 1mm; H) Strongly sericite altered porphyry exhibiting a well developed crenulated D2 foliation, northern Deloro Township porphyry dike swarm, XPL, scale = lcm:2mm; I) Anhedral chlorite lath, northern Deloro Township porphyry dike swarm, PPL, scale = lcm:2mm; and J) Silicified feldspar porphyry, Pominex porphyry. 490000 500000 510000. 520000 530000 540000 Figure A12. Simplified surface geological map of the location of the Carr Township porphyry intrusive suite (modified from Ayer et al. 1999a, 1999b). 158 (E) (F) Fngmr® A13„ Photographs and photomicrographs showing features of the Can Township porphyry intrusive suite: A) Sharpe contact between porphyry intrusion and-host mafic volcanic rocks, Carr Township porphyry; B) Irregular, subrounded porphyry fragments within chloritic mafic volcanic matrix, Carr Township porphyry; C) Large feldspar phenocrysts, Carr Township porphyry, XPL, scale = lem:3mm;-B) Large sulphide (pyrite) fragment ("clot"), Carr Township porphyry; E) Subrounded porphyry fragmentswithi n a porphyry matrix, Can- Township porphyry; and F) Sfrongly sericite altered porphyry with feldspars and feldspathic matrix completely replaced by sericite, Carr Township porphyry, XPL, scale = lcm:2mm. 159 458000 459000 460000 461000 462000 463000 464000 465000 466000 467000 —, to co w\ ^•" '•' S CO CO in co ^F'- CD CO BBP^r WF.:- s to to co *• .* CO to .." >' *••..- Legend - - .'.'.« '.' • • - " - O) IO -A^' •> CO 3 ^^B Porphyry Suite CO -•j Holmer porphyrjr •: • •• .-' 1: -.' -1 Porcupine Assemblage « ' '.i.'-' : '•" • -1 •'•".' ".--• to : Thunder Creek ^^| Tisdale Assemblage rt in " porphyry/syenite - - " Fault ••'::1:';. ••.•:'••': "^T Timmins West/Holmer Mine Southwest Bristol Township syenite Kilometers 0 1 2 3 4 ^Cffffff^l • ••'.: -•'.v. .''.'I- 458000 459000 460000 461000 462000 463000 464000 465000 466000 467000 » Figure A14. Simplified surface geological map showing the names and locations of the Holmer intrusive suite (modified from Ayer et al 1999a, 1999b; Vaillancourt et al. 2001). 160 Figure A15. Photographs and photomicrographs showing features of the Holmer intrusive suite: A) Heterolithic breccia including angular shaped, centimeter sized fragments of quartz- feldspar porphyry, mafic volcanic and siliciclastic mudstone sediments, Holmer porphyry; B) Equigranular texture of interlocking feldspar crystals, Thunder Creek intrusion, scale = lcm:2mm; and C) Calcium-carbonate altered (clouded grey appearing) feldspar phenocrysts, Holmer porphyry, scale = lcm:2mm. 161 473000 474000 475000 476000 477000 478000 479000 480000 481000 482000 483000 484000 '3^ - '/?////, ^^ Legend ^^| Porphyry Suite IS :°^ Krist Formation r iS?l Timiskaming Assemblage L^***1! Tisdale Assemblage • n **. c .- formation contacts Beady Formation « Fault EZ2 Deloro Assemblage Kilometers •'•'\ Fold - Anticline ..*"\"'* Fold - Syncline 473000 475000 476000 478000 480000 Figure A16. Simplified surface geological map showing the names and locations of some of the intrusions of the granodiorite intrusive suite (modified from Ferguson 1966; Brisbin 1997; Vaillancourt et al. 2001). 490000 500000 510000 520000 540000 t- 490000 500000 510000 520000 530000 540000 488000 490000 492000 Legend —4— Porphyry Suite r J Tisdale Assemblage .' • J Porcupine Assemblage K""Vl Kidd-Munro Assemblage ^jj Kinojevis Assemblage Y//\ Deloro Assemblage « * ' Major Fault Pamour porphyry Bob's Lake granodiorite Kilometers 488000 490000 492000 Figure A17. Simplified surface geological map showing the names and locations of some of the intrusions of the granodiorite intrusive suite (modified from Ayer et al. 1999a, 1999b). 163 Figure A18. Photographs and photomicrographs showing features of the granodiorite intrusive suite: A) Porphyritic texture with quartz and feldspar phenocrysts within a quartzo-feldspathic matrix, Naybob porphyry, XPL, scale = lcm:2mm; B) Porphyritic texture with feldspar and quartz phenocrysts within a quartzo-feldspathic matrix, Pamour porphyry, XPL, scale = lcm:2mm; C) Equigranular texture of interlocking feldspars and quartz crystals, Porphyry Hill, XPL, scale = lcm:2mm; D) Equigranular texture of interlocking feldspar and quartz crystals, Bob's Lake granodiorite, XPL, scale = lcm:2mm; and E) Biotite cluster within the Pamour porphyry. 164 474000 475000 476000 477000 478000 479000 480000 481000 482000 474000 475000 476000 477000 478000 479000 480000 481000 482000 Figure A19. Simplified surface geological map of the felsic volcanic suite showing the names and locations where samples were collected (modified from Ferguson 1966; Brisbin 1997; Ayer et al. 1999a, 1999b; Hall et al. 2003). -J* m K^.\ I .>• (B) (D) (E) Figure A20. Photographs and photomicrographs showing features of the felsic volcanic suite: A) Quartz and feldspar phyric lapilli tuff matrix of Krist Formation, Kayorum Syncline, XPL, scale = lcm:2mm; B) Mafic clasts within conglomerate facies of Krist Formation, Kayorum Syncline; C) Large sulphide (pyrite) fragment within Krist Formation, Kayorum Syncline; D) Sericite and calcium-carbonate altered (cloudy grey appearance) Krist Formation matrix, Porcupine Syncline , XPL, scale = lcm:2mm; E) Elongate, stretched porphyry clasts along transposed S0/S2 fabric, Krist Formation, Kayorum Syncline. Name Suite Age (Ma) Source Crown porphyry TIS - main camp 2688 ± 2 Corfu et al. 1989 Millerton porphyry TIS - main camp 2691 ± 3 Corfu etal. 1989 Miller Lake porphyry TIS - main camp - - Northern porphyry TIS - main camp - - Acme porphyry TIS - main camp - - Gillies Lake porphyry TIS - main camp - - Pearl Lake porphyry TIS - main camp 2689 ± 1 Corfu etal. 1989 Coniaurium porphyry TIS - main camp - - Dome Fault Zone porphyry TIS - main camp 2688 ±2 Gray and Hutchinson 2001 Preston porphyry TIS - main camp ca. 2690 Corfu etal. 1989 Paymaster porphyry TIS - main camp 2690 ± 2 Corfu etal. 1989 West porphyry TIS - main camp - - Northwest porphyry TIS - main camp - - Edwards porphyry TIS - main camp - - Buffalo Ankerite #5 porphyry TIS - main camp - - Buffalo Ankerite porphyry TIS - main camp - - Bristol Twp. porphyry TIS - other 2687.7 ±1.4 Ayer et al. 2003 Bristol Lake porphyry TIS - other - - South Bristol Lake porphyry TIS - other - - northern Deloro Twp. porphyry dike swarm TIS - other - - Mt. Logano porphyry TIS - other 2689.0 ±1.4 MacDonald et al. 2005 Hoyle Pond porphyry TIS - other 2684.4 ±1.9 Bateman et al. 2005 Hoyle Pond porphyry sill TIS - other 2687.2 ± 2.2 Ayer et al. 2005 Aquarius porphyry TIS - other 2705 ±10 Corfu et al. 1989 Aquarius Mine porphyry TIS - other - - Homestead porphyry TIS - other - - Crowley porphyry TIS - other - - Pominex porphyry TIS - other - . Carr Two. porphyry CIS - . Holmer porphyry HIS - - Southwest Bristol syenite HIS - - Thunder Creek porphyry HIS - - Naybob porphyry GIS - - Porphyry Hill granodiorite GIS - - Pamour porphyry GIS 2677.5 ± 2.0 MacDonald et al. 2005 Bob's Lake granodiorite GIS - - Porcupine Syncline - Krist Formation FYS 2687.3 ±1.6 Ayer et al. 2002b Kayorum Syncline - Krist Formation FVS 2687.5 ±1.3 Ayer et al. 2002b South of PDDZ - Deloro Assemblage FYS - - Table Al. Table of porphyry intrusions and felsic volcanic rocks included in this study. Information includes the name, Porcupine intrusive suite designation, age of crystallization (if known) and published source of age date. Porcupine intrusive suites include: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS = granodiorite intrusive suite. FVS = felsic volcanic suite. 167 Category Subcategory TIS-main camp TIS-other CIS Field Tread east-northeast/west-southwest generally east-west east-west Relationships Size of trend? 2 trends: one is 8 x 2 km; and 3 groups total 50+ km along over 15 x 5 km one is 4 x 1.5 km PDDZ Join at depth? ves yes and ??? composite? Plunge east west and ??? ??? direction? Srratigraphic 1) northern margin of the PDDZ 1) upper Deloro l)Tisdale/Porcupine level Assemblage/ Deloro-Tisdale Assemblages contact Assemblages contact (lower/middle Tisdale -Vipond Formation) 2) Hersey Lake-Central 2) Hersey Lake-Central Formation contact Formation contact 3) Central and Vipond 3) base of the Porcupine Formations (Tisdale Assemblage/ Tisdale- Assemblage) Porpcupine Assemblages contact Stratigraphy generally semi-conformable semi-conformable semi-conformable? conformable? Other 1) pillowed mafic flows of the 1) Assemblage contacts N/A favonrable zones Tisdale Assemblage for intrusion? 2) 'carb rock' alteration zones 2) fault zones (PDDZ and related splays) 3) fault zones (e.g. Dome fault) 3) fold margins (Shaw Dome) 4) fold hinges (e.g. Northern anticline) Sizes & shapes 1) small dikes, sills and plugs 1) small dikes, sills and 1) one large composite plug (up to 500 x 300 m) plugs (up to 1 km x 200 m) (over 12x5 km) 2) dikes and sills (up to 2 x 0.5 2) large dikes and sills (up km) to 5 x 0,5 km) 3) large oval (~2 x 0.6 km) 3) large thin dikes and sills (up to 5 km x 50 m) 4) large oval (6x3 km) Margins -generally straight and sharp -generally straight and sharp -generally straight and sharp with small apophyses with small apophyses (primary or tectonic) -lesser marked by breccias -lesser marked by breccias -lesser marked by breccia (Edwards, Paymaster and (Bristol Township and Mt. Crown) Logano porphyries) -minor gradational contacts (Aquarius porphyry) Table A2. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al. 2005. Category Subcategory HIS GIS Field Trend northeast-southwest east-northeast/west-southwest Relationships Size of trend? 2 km 2 trends: one is 2 x 0.5 km; and one is 5 x 2.5 km Join at depth? ??? ??? Plunge ??? 77? direction? Stratigraphic 1) Tisdale/Porcupine 1) upper Deloro Assemblage/ level Assemblages contact Deloro-Tisdale Assemblages (lower/middle Tisdale contact -Vipond Formation) 2) Hersey Lake-Central Formation contact Stratigraphy semi-conformable semi-conformable conformable? Other 1) fault zones (PDDZ and 1) fault zones (Dome fault favourable zones related splays) extension and PDDZ) for intrusion? 2) fold margins (Shaw Dome?) Sizes & shapes 1) small plug (lxl km) 1) small dikes and sills (up to 1 kmx 1000 m) 2) small dikes and sills (up 2) plug (~500 x 200 m) to 500 x 100 m) 3) large elongate plug (-5 x 2 km) Margins -generally straight and sharp -generally straight and sharp (primary or tectonic) (primary or tectonic) -lesser marked by heterolithic breccia (Holmer porphyry) Table A2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. 169 Category Subcategory TlS-maia camp TIS-other CIS Petrology Texture aphamtic and norphvritic porDhvritic Dorohvritic Phenocrysts sub- to euhedral plagioclase sub- to euhedral plagioclase sub- to euhedral plagioclase and quartz up to 8mm and quartz up to 6mm and quartz up to 15mm Matrix aphanitic to very fine grained very fine grained fine grained Minor Minerals apatite and tourmaline apatite and tourmaline N/A Sulphides pyrite, chalcopyrite, pyrite, chalcopyrite, pyrite and chalcopyrite pyrrhotite, molybdenite and pyrrhotite and molybdenite bornite Foreign clasts green mica and porphyry green mica and porphyry rounded porphyry fragments fragments iro to 1 Ocm fraements up to 10cm Metamorphic stilpnomelene biotite, chlorite and trace chlorite and biotite muscovite Alteration, Alteration white mica (sericite), calcium sericite, calcium-carbonate, sericite, chlorite, hematite Veining and carbonate, hematite, iron- chlorite, hematite, iron- and silicification Mineralization carbonate (ankerite), chlorite carbonate (ankerite), and tourmaline silicification and albite Veining quartz-tourmaline, quartz- quartz sweats, quartz-calcite quartz sweats and quartz- ankerite, quartz-calcite and and quartz-ankerite calcite quartz Mineralization gold mineralization gold mineralization anomalous gold copper mineralization _anornalous_£ggDer_ jratmialous^jODDer_ Deformation Deformation D2 foliation, D3 spaced D2 foliation and D3 spaced D3 foliation cleavage, D? stretching cleavage lineation and D6 foliation Geochronology Geochronology -Paymaster = 2690 ±2 Ma (1) -Bristol Township = 2687.7 -unknown; suspected ~2685- ±1.4 Ma (3) 2670 Ma -Preston = ca. 2690 Ma (1) -Mt. Logano = 2689.0 ±1.4 Ma (4) -Dome Fault Zone = 2688 ±2 -Hoyle Pond = 2684.4 ±1.9 Ma (2) Ma (5) -Hoyle Pond sill = 2687.2 -Crown = 2688 ±2 Ma (1) ±2.2 Ma (6) -Aquarius = 2705 ±10 Ma -Millerton = 2691 ±3 Ma (1) (1) -Pearl Lake = 2689 ±1 Ma(l) Table A2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. Category Subcategory HIS GIS Petrology Texture porphvritic and equigranular porphyritic and eauigranular Phenocrysts sub- to euhedral feldspars sub- to euhedral plagioclase (orhoclase and plagioclase) ± and quartz up to 6mm auartz UD to 5mm Matrix finegrained fine grained Minor Minerals N/A biotite, muscovite and apatite Sulphides pyrite and trace arsenopyrite pyrite Foreign clasts N/A N/A Metamorpbic N/A biotite, chlorite and muscovite minerals Alteration, Alteration sericite, chlorite, calcium- sericite, calcium-carbonate, Veining and carbonate, hematite and iron- chlorite and iron-carbonate Mineralization carbonate (ankerite) (ankerite) Veining quartz sweats and quartz- quartz sweats and quartz- calcite calcite Mineralization gold mineralization gold mineralization no copper known no copper known Deformation Deformation D3 foliation D3 foliation Geochronology Geochronology -unknown; suspected -2675- -Pamour = 2677.5 ±1 Ma (4) 2665 Ma Table A2, continued. Table of field relationships, petrology, alteration, veining, mineralization, deformation and geochronology for the five Porcupine intrusive suites. (1) Corfu et al. 1989; (2) Gray and Hutchinson 2001; (3) Ayer et al. 2003; (4) MacDonald et al. 2005; (5) Bateman et al. 2005; (6) Ayer et al.2005. 171 Appendix B: An Assessment of the Immobility of Elements in Petrogenetic Interpretations of the Porcupine Intrusive Suites. B.l Introduction Petrogenetic interpretations of the Porcupine intrusive suites within this thesis utilized elements that are considered to represent primary magmatic abundances and/or ratios. The elements considered immobile include: AI2O3, TiC>2, Zr, Y, Nb, La, Yb, Ta, Sc and rare earth elements (REE). Due to observed alteration affecting most samples, it is important to illustrate that these elements remained immobile. This appendix presents the assessment of element immobility by comparisons of element abundances and element ratios commonly known to remain immobile during alteration versus: 1) other element abundances commonly known to remain immobile during alteration (Barrett and MacLean 1994); 2) alteration, using the Al203/Na20 alteration index as an alteration monitor (Spitz and Darling 1978; Piercey et al. 2002); and 3) Na20 mass change variations and associated immobile element mass changes (Barrett and MacLean 1994). B.2 Geochemical Tests of Element Immobility Three different tests are presented to test element mobility. The first test is the comparison of elements abundances commonly known to remain immobile. Bivariate plots of Th, Nb and Y versus Zr display linear trends that pass near the origin with only the Y plots displaying a minor amount of scatter (Figs. B1 .A, B1 .B and B1 .C). Bivariate plots of TKD2, Sc and Yb versus Zr display more scatter, although relatively well defined linear trends that pass near the origin are present (Figs. Bl.D, Bl.E and Bl.F). The second test is the comparison of alteration versus suspected immobile element abundances and element ratios. Figure B2 presents the Al20s/Na20 alteration index 172 verses some of the elements and element ratios used in Chapter 2. In all of figure B2 diagrams, few, if any, proportional linear trends can be observed. The third test is the comparison of Na20 mass change (and other element mass changes) versus abundances, ratios and mass change of elements assumed immobile (Barrett and MacLean 1994). Mass change calculations were undertaken using the Barrett and MacLean (1994) single precursor systems method for each of the Porcupine intrusive suites, with least altered precursors for each suite being selected using petrographic and geochemical observations. Mass change values for major and key trace elements are presented in Table Bl. Na20 mass change was selected for element immobility tests as it appeared the most consistently affected by alteration in the Porcupine intrusive suites. Plots of Na20 mass change versus Nb, La, Zr, Y, Yb, Sc, Zr/Ti02, Nb/Y, La/Yb, Zr/Y, La/Sm and Sc/Y, as well as Nb, La, Zr, Y, Yb and Sc mass change are presented in Figure B3. With the exception of the Holmer intrusive suite (HIS), the majority of the samples have element abundances that cluster near the precursor line for zero Na20 mass change in Figure B3. A few samples of the TIS-other display slight NaaO mass gain, with little to no affect on Nb, La, Zr, Y, Yb or Sc. As for the HIS, the samples display a negative correlation between Nb, La, Zr, Y, Yb and Sc abundances and Na20 mass gain. With respect to element ratios, none of the samples display a correlation with Na20 mass change. Mass changes of Nb, La, Zr, Y, Yb and Sc show little to no correlation with Na20 mass change, with the exception of the HIS samples which all show slight mass loss during Na20 mass gain. 173 B.3 Discussion of Element Immobility In the majority of samples, the elements used in Chapter 2 petrogenetic interpretations have remained immobile. Linear trends passing near the origin on bivariate plots of Zr versus Th, Nb, Y, T1O2, Sc and Yb (Fig. Bl) suggest that these elements have retained with primary ratios during alteration and are immobile (Barrett and MacLean 1994). Scatter in the Timmins porphyry intrusive suite (TIS) can be explained by minor regional geochemical inhomogeneities in the suites (e.g., Barrett and MacLean 1994). The absence of proportional linear trends in Figure B2 suggests that some process other than alteration controlled the distribution of these elements, i.e., these elements were immobile and primary petrogenetic processes controlled their distribution. As well, in the majority of samples Na20 mass change has had little effect on element abundances or element ratios, suggesting that the elements have retained primary abundances and ratios during alteration and mass change (Fig. B3). Based on the three tests presented above, it can be concluded that element abundances and element ratios used in Chapter 2 did remained immobile and reflect primary magmatic compositions. An exception to the conclusions above is the HIS. Elemental abundances in the HIS have to be used with caution because of the correlation between Na20 mass gain and Nb, La, Zr, Y, Yb or Sc abundances and mass loss. With that stated, the three samples with the highest trace and rare earth element abundances plot near the zero Na20 mass change line (Fig. B3) indicating their primary element abundances are intact and can be utilized for petrogenetic interpretations of the HIS. As well, none of the ratios display a correlation with Na20 mass gain indicating that ratios for all of the samples can be used for petrogenetic interpretations. 174 B.4 Summary of Element Immobility Element abundances of AI2O3, Ti02, Zr, Y, Nb, La, Yb, Ta, Sc and rare earth elements (REE) abundances and ratios reflect primary magmatic compositions for the majority of samples utilized in this thesis and can be used for petrogenetic interpretations. HIS element abundances are an exception, although HIS samples with the highest REE abundances do reflect primary magmatic concentrations and can be used for petrogenetic interpretations of the HIS. B.5 References Barrett, T.J. and MacLean, W.H. 1994. Chemostratigraphic and Hydrothermal Alteration in Exploration for VHMS Deposits in Greenstones and Younger Volcanic Rocks; in Alteration and Alteration Processes associated with Ore-forming Systems, edited by Lentz, D.R.: Geological Association of Canada, Short Course Notes, v.l 1, p.433-467. Piercey, S.J., Mortensen, J.K., Murphy, DC, Paradis, S. and Creaser, R.A. 2002. Geochemistry and tectonic significance of alkalic mafic magmatism in the Yukon- Tanana terrane, Finlayson Lake region, Yukon: Canadian Journal of Earth Sciences, v.39,p.l729-1744. Spitz, G. and Darling, R. 1978. Major and minor element lithogeochemical anomalies surrounding the Louvem copper deposit, Val d'Or, Quebec: Canadian Journal of Earth Science, v.15, p.l 161-1169. 175 40 30 1 A | Legend I ' I ' I ' I « Bj' I ' I ' I \ ' 1 ' A "A" TIS-main 30 •A- US-other — A 20 O CIS A A :ao A HIS A - o GIS A • FVS 10 - 10 O - JM" - +m^l III! I.I. T^JF . 1 . 1 1 1 1 1 1 100 200 300 400 500 600 100 200 300 400 500 800 Zr Zr 40 c]' i ' I 1 I 1 1 ' 1 ' A 30 — A . ><20 — A - 10 -a 1 - Y^^* . °i 1 1 1 1 1 1 1 100 200 300 400 500 600 Zr 20 IT -| 1 1 1 1 1 1 1 r- is r- v5«> **T«*. I 1 I i I I L 100 200 300 400 500 600 Zr Figure Bl. Immobile element versus immobile element immobility test plots, including: A) Zr versus Th; B) Zr versus Nb; C) Zr versus Y; D) Zr versus TiCh; E) Zr versus Sc; and F) Zr versus Yb. After Barrett and MacLean( 1994). Elemental abundances plotted in ppm, excluding Ti02 which is plotted in wt%. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and - other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 176 2000 1 1 1 1 | 40 Aj ' - Bl ' ' ' • Legend "A "AT TIS-main 1500 —- 30 " -A- TIS-other A g A O CIS - 2A - . C20H - A HIS SI O GIS 500 — 10 o * FVS • ar lr C • i i i i HIBLi 1—__i 1 1 * 0 10 20 30 40 50 60 70 10 20 30 40 50 60 70 Al203/Na20 Al203/Na20 30 C| ' " ' ' I 1 M • i i i i 1 A 20 - A - A 10 - $ -A- v i r fr ^ ********* * »** .... 1 > • i i i I l 10 20 30 40 50 60 70 10 20 30 40 50 60 70 Al203/Na20 Al203/Na20 10 20 30 40 50 60 70 20 X 40 50 Al203/Na20 Al203/Na20 Figure B2. Immobility test plots of the AhCh/NazO alteration index versus major, trace and rare- earth element abundances and ratios, including: A) AhOi/Na20 versus Zr/TiCh; B) AhOa/TSfeO versus Th; C) Ab03/Na20 versus Nb; D) AbOs/TS^O versus Nb/Y; E) Ab03/Na20 versus Zr/Y; and F) AhCh/Na^ versus La/Yb. After Piercey et al. (2002), alteration index from Spitz and Darling (1978). Major element abundances in wt%, and trace and REE element abundances in ppm. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 177 1 1 1 T eoo 9 Legend 0.6 4 1 1 1 1 500 ~& TIS-main 05 * * -A" TIS-other 400 04 "A D CIS • I* * 1 T N300 A ras Qo.3 A O GIS H 200 * FVS 02 — 100 f i$ Artft^*** * • 3 01 - 0 . • on i_ 1 1 1 1 1 10 20 30 40 50 60 70 10 20 30 40 50 60 70 Al203/Na20 Al203/Na20 "" • T • I] 40 Jj —i— A A X 2" A A > ><2D A £ • 1 ? 10 ™ i < 10 20 30 40 50 60 70 10 20 30 40 50 60 70 Al203/Na20 Al203/Na20 E-"" 1 3"S-' is h 15 h 9310 -A 4s« £ **#*** * * J-l as * *£ 0.0 10 20 30 40 50 60 70 20 30 40 50 60 70 Al203/Na20 Al203/Na20 Figure B2, continued. Immobility test plots of the AhCh/NasO alteration index versus major, trace and rare earth element abundances and ratios, including: G) Ab03/Na20 versus Zr; H) AbOa/NsbO versus TiGh; I) AbCb/NasO versus Yb; J) Ab03/Na20 versus Y; K) AhCb/NaaO versus Sc; and L) AbCh/N&O versus Sc/Y. After Piercey et al. (2002), alteration index from Spitz and Darling (1978). Major element abundances in wt%, and trace and REE element abundances in ppm. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 178 1 30 Aj 1 1 Legend —' 1 103 Bj j ' ' ' 1 A ir TIS-main 1 A 80 20 - i - •A- TIS-other I lA I 8,60 • CIS AA -I - « A HIS - I — 40 o GIS * FVS * A * A 1 1 0 I " 10 0 10 20 30 40 SO 60 10 0 10 20 30 40 50 60 NsuO (MC) Na20 (MC) 600 - 1 40 I 1 i 1 1 a j • ' ' 2l 1 500 _ i i — 4 30 i 400 A - i t>J300 - 20 - A < 200 I 10 A 100 £kr* A A i m r^fr , A 0 I i i i i 1 0 N *• • 1 10 0 10 20 30 40 50 60 10 i 10 20 30 40 50 60 Na20(MC) Na20 (MC) 3 Ej \ 1 J 20 • i i 1 1 P 1 15 2 - - • 1 ->->-- • l»10 — — > _ i „, 1 T* f* *h _ .A A A A A 0 *• • 1 0 ...A-J i i 1 -10 10 20 30 40 50 60 -10 10 20 30 40 50 60 Na20 (MC) Na20 (MC) Figure B3. Immobility test plots of the absolute mass change of N^O (NaaO (MC)) versus trace and rare earth element abundances, ratios and mass change, including: A) Na2<~) (MC) versus Nb; B) Na20 (MC) versus La; C) NaaO (MC) versus Zr; D) Na20 (MC) versus Y; E) NaaO (MC) versus Yb; and F) Na20 (MC) versus Sc. After Barrett and MacLean (1994). Absolute mass change of Na20 presented in g/lOOg, and trace and REE element abundances in ppm. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 179 nr Legend "A' TIS-main 3r" -A" TIS-other Q CIS ^ _ •02t— A HIS • • o GIS £# » FVS J_ J 10 20 30 40 S3 60 -10 10 20 30 40 50 60 Na20 (MC) Na20 (MC) T 10 t) 10 20 30 40 50 60 NsuO (MC) 60 K| I " • • " I 50 . * - g40 (« ,J30 : 20 - 6 10 A 0 i 10 20 30 40 50 10 20 30 40 Na20 (MC) Na20 (MC) Figure B3, continued. Immobility test plots of the absolute mass change of Na20 (Na20 (MC)) versus trace and rare earth element abundances, ratios and mass change, including: G) Na20 (MC) versus Zr/TiCh; H) NajO (MC) versus Nb/Y; I) Na20 (MC) versus La/Yb; J) Na20 (MC) versus Zr/Y; K) Na20 (MC) versus La/Sm; and L) NazO (MC) versus Sc/Y. After Barrett and MacLean (1994). Absolute mass change of Na20 presented in g/lOOg, and trace and REE element abundances in ppm. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 180 100 m ! Legend "A1 TIS-main X — •A- TIS-other • as tii&fcij.x J. o — A HIS A o GIS -50 — * FVS A ' A 1 A -100 1 1 1 1 i 1 10 20 X 40 -10 0 10 20 X 40 50 60 Na20 (MC) Na20 (MC) o] 1 —i 1 20 P I I I 1 A 10 - - ,lil i u So i £ra 3PWfr ft > m•9 1 . I • -10 A - BMMMN*-*- A A A - 1 * • • ' -20 i I • • • 1 10 0 10 20 30 40 50 60 -10 20 X 40 50 60 Na20 (MC) Na20 (MC) fil 1 1 20 R| I ' ' —i 1— 1 i i A — ** 10 - _ ! A 4 fc- A - 1 • • TO A u 1 cc o -&te~~- 1 • - i i -1- - 1 -10 • • " -10 10 20 X 40 x X -10 10 X X 40 X X Na20 (MC) Na20 (MC) Figure B3, continued. Immobility test plots of the absolute mass change of Na20 (Na20 (MC)) versus trace and rare earth element abundances, ratios and mass change, including: G) Na20 (MC) versus Zr/TiCh; H) Na20 (MC) versus Nb/Y; I) Na;*) (MC) versus La/Yb; J) Na20 (MC) versus Zr/Y; K) Na2Q (MC) versus La/Sm; and L) Na20 (MC) versus Sc/Y. After Barrett and MacLean (1994). Absolute mass change of Na20 presented in g/lOOg, and trace and REE element abundances in ppm. Legend note: TIS = Timmins porphyry intrusive suite (-main camp and -other); CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; GIS = granodiorite intrusive suite; and FVS = felsic volcanic suite. 181 Sample 93-i>JM-132e 03-PJM-132f 03-P.IM-132g 03-PJM-132D 03-PJM-139d 03-PJM-139* l)3-PJM-139h 03-NMAm Suite TlS-main^amo^ TIS-main camp TIS-main camp TIS-main canm TIS-main camp TIS-main camp TIS-main camp TIS-main camp ZrfEF) 0.898 0.906 0.585 0.917 0.952 0.853 0.892 0.763 SiG2 (LOI-free) 68.78 69.75 43.73 70.03 68.67 70.36 69.64 68.28 TiOl (LOI-free) 0.41 0.42 0.63 0.37 0.39 0.42 0.40 0.48 AW)3 (LOI-free) 17.96 17.15 29.59 16.61 17.31 18.48 17.89 18.57 FeOJ (LOI-free) 3.55 4.75 8.61 4.17 6.33 4.75 3.80 6.37 MnO (LOI-free) 0.03 0.03 0.07 0.06 0.02 0.00 0.07 0.07 MgO (LOI-flee) 1.47 2.73 3.39 2.07 1.17 0.39 1.37 2.80 CaO (LOI-free) 2.26 0.97 5.31 2.76 1.48 0.30 3.11 0.48 Na20(LOI-fiee) 0.59 1.03 0.57 1.11 0.77 0.78 1.24 0.69 K2O (LOI-free) 4.71 3.06 7.88 2.70 3.73 4.33 2.31 2.06 P2O5 (LOI-free) 0.22 0.11 0.23 0.13 0.14 0.20 0.16 0.19 SiOl(MC) -5.53 -t.16 ^tl.76 -3.07 -1.97 -7.28 -5J20 -15.23 TiO! (MC) 0.03 0.O4 0.03 0.00 0.03 0.02 0.01 0.03 AI2O3 (MC) -0.57 -1.17 0.60 -1.47 -0.23 -0.93 -0.74 -2.54 Fe203(MC) 0.04 1.15 1.88 0.67 2.87 0.90 0.24 1.71 MDO (MC) -0.03 -0.03 -0.02 0.00 ,0.04 -0.06 0.00 -0.01 MgO(MC) 0.07 1.22 0.73 0.65 -0.14 -0.91 -0.03 0,89 CaO(MQ -1.99 -3.15 -0.92 -1.50 -Z62 -3.77 -1.25 -3.66 Na20(MC) -4.34 -3.93 -4,53 -3.85 -4.14 -4.20 -3.76 -4.34 K20(MQ 2.10 0.64 2.47 0.35 1.42 1.56 -0.07 -0.56 P20S(MC) 0.05 -0.05 -0.01 -0.03 -0.01 0.03 -0.01 0.00 Sc(MC) -0.80 -0.90 1.40 0.10 0.40 0.80 0.30 -0.80 Zr(MC) 12.70 11.70 79.80 10:10 5.70 19.30 13.60 34.90 Nb(MC) 0.50 0.10 2.00 0.00 0.60 0.90 0.30 1.80 Y(MQ 1.78 0.83 3.42 2.79 0.97 3.39 1.35 2.78 La(MQ 4.16 5.54 16.01 -1.95 -1.09 9.31 1.42 2.76 Yb(MC) 0.08 0.07 0.50 0.12 0.10 0.27 0.05 0.21 Sample 03-PJM-139J 03-PJM-140a l)3-PJM-140b 03-PJM-140C 03-PJM-140h 03-PJM-14Oi 03-PJM-143C 03-PJM-143e Suite TIS-main camp TIS-main camo TIS-main camo TIS-main camp TIS-main camp TIS-main camp TIS-main camp TIS-main camp Zr(EF) 0.830 0.979 1.020 1.006 1.038 0.801 0.926 0.894 SiOz (LOI-ftee) 76.91 64.06 64.69 66.16 63.46 59.84 70.57 75.43 T1O2 (LOI-free) 0.44 0.40 0:42 0.40 039 0.50 037 0.41 AI2O3 (LOI-free) 19.23 16.93 16.95 16.69 15.16 21.01 18.41 19.11 F«03 (LOI-free) 0.59 7.57 8.07 6.24 10.64 7.96 4.66 0.73 MnO (LOI-free) 0.00 0.11 0.14 0.05 0.04 0.04 0.00 0.00 MgO (LOI-free) 0.04 2.09 2.80 2.05 2.07 1.71 0.56 0.07 CaO (LOI-free) 0.31 3.71 2.04 2.77 3.66 2.71 0.23 032 NalO (LOI-free) 0.78 0.42 0.49 0.28 0.48 0.46 0.64 131 K2O (LOI-free) 1.53 4.53 4.22 5.15 3.90 5.55 4.41 2.43 P2O5 (LOI-free) 0.17 0.18 0.18 0.20 0.20 0.21 0.15 0.19 SK)2(MC) -3.48 -4.60 -1.34 -0.75 -1.46 -19.39 -1.99 0.12 TK>2 (MC) 0.03 0.05 0.08 0.06 0.06 0.05 0.00 0.02 AI203(MQ -0.74 -0.13 0.58 0.09 -0.97 0.12 0.34 0.38 Fe203(MC) -2.66 4.26 5.08 3.13 7.89 323 1.17 -2.50 MBO(MC) -0.06 0.04 0.08 -0.01 -0.02 -0.03 -0.06 -0.06 MgO (MC) -1.21 0.80 1.61 0.82 0.90 0.12 -0.73 -1.18 CaO(MC) -3.77 -0.40 -1.95 -1.23 -0.23 -1.85 -3.81 J.74 Na20(MC) -t.22 -4.45 -4.36 ^(.59 -4.37 -4.50 -4.28 -3.70 K2O (MC) -0.86 2.30 2.18 3.05 1.91 2.32 1.95 0.04 P205(MC) -0.01 0.03 0.04 0.06 0.06 0.02 -0.01 0.02 Sc(MC) 0.80 0.80 1.20 1.20 0.50 0.60 0.60 -0.70 Zr(MQ 23.00 2.40 -2.20 -0.70 -4.10 27.90 9.00 13.30 Nb(MC) 1.00 0.30 0.10 0.40 0.50 1.10 0.10 0.30 Y(MC) 3.92 1.55 1.65 1.29 1.31 2.44 1.97 -0.94 La(MC) 10.36 2.15 3.11 -0.36 0.02 3.94 1.35 0.98 YbfMC) 0.31 0.09 0.09 0.06 0.10 0.21 0.12 -0.09 Table Bl. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite. Sample 03-PJM-143h 03-PJM-143i 03-PJM-l44b 03-PJM-144f 03-P]M-144g »3-PJM-144i 03-PJM-133a 03-PJM-»3f Suite TTS-main camp TIS-main camp TIS-main camp TIS-main camp TIS-main camp TIS-main camp TTS-main camp TIS-main camp ZrfEF) 0.935 0.879 0.794 0.864 0.932 0.920 1.000 0.985 Si02 (LOI-free) 76.78 76:49 68.49 65.22 66.29 64.93 67.32 66.64 TiO! (LOI-free) 0.41 0.40 0.41 0.38 0.39 0.40 0.34 0.37 AU03 (LOI-free) 16.90 17.76 18.02 17.41 16.75 17.05 16.70 15.85 fe203 (LOI-free) 0.78 0.14 3.84 6.96 3.41 6.04 3.15 4.11 MnO (LOI-free) 0.00 0.00 0.03 0.10 0.07 0.05 0.06 0.07 MgO (LOI-free) 0.10 0.12 1.65 2.53 2.81 2.65 1.25 1.68 CaO(LOI-free) 0.20 0.15 3.34 3.35 5.64 3.69 4.02 3.84 NalO (LOI-free) 0.66 1.06 2.02 0.82 1.10 0.45 4.87 5.99 K2O (LOI-free) 4.00 3.75 2.04 3.07 3.38 4.53 2.13 1.31 P2OS (LOI-freel 0.16 0.12 0.17 0.16 0.15 0.20 0.15 0.15 SiOi(MC) 4.47 -0.05 -12.93 -10.98 -5.55 -7.56 0.00 -1.68 TiOifMC) 0.04 0.01 -0.02 -0.01 0.02 0.02 0.00 0.03 AW)3(MQ -0.90 -1.09 -2.39 -1.66 -1.09 -1.01 O.00 -1.09 FeiOJ(MC) -2.42 -3.03 -0.10 2.86 0.03 2.41 0.00 0.89 MnO(MC) -0.06 -0.06 -0.04 0.02 0.00 -0.01 0.00 0.01 MgO(MQ -1.15 -1.14 0.06 0.94 1.37 1.19 0:00 0.41 CaO (MC) -3.84 -3.89 -1.38 -1.13 1.23 -0.62 0.00 -0.25 Na20(MC) -4,25 -3.94 -3,26 -4.16 -3.84 4.45 0.00 1.03 K20(MC) 1.61 1.17 -0.51 0.52 1.02 2.04 0.60 -0.84 P1O5 0MQ 0.01 -0.04 -0.01 -0:01 0.00 0.04 0.00 0.00 Sc(MC) -0.40 1.10 0.30 0.30 0.10 0.70 O.00 0.90 Zr(MC) 7.80 15.40 29.10 17.70 8.20 9.70 0.00 1.70 Nb (MC) 0.20 0.30 0.80 0.80 0.50 0.20 0.00 0.10 ¥(MC) 0.52 -0.98 2.62 1.76 1.76 1.70 OOO 3.04 La(MQ -3.79 -2.84 1.68 8.50 7.01 2.12 O.OO 1.52 YblMO 0.01 -0.06 0.20 0.11 0.12 0.11 . 0.00 . 0.32 Sample M*IM-134d »3-PJM-134e 03-PJM-150a 03-PJM-150D 04-PJM-2M 03-P.JM-148 03-PJM-OOS 03-PJM-006 Suite TIS-mainramp TIS-main camp TIS-main camp TIS-main camo TIS-main camp TIS-main camp TTS-main camp TIS-main camp Zr(EF) 0.770 1.046 0.973 0.958 0.956 1.085 1.004 1.115 SiOi (LOI-free) 61.54 65.91 68.93 68.94 69,21 66.20 65.29 68,17 Ti02 (LOI-free) 0.44 0.36 0.35 0.34 0.35 0.40 034 0.34 AI2O3 (LOI-free) 20.25 16.01 16.60 16.64 16:73 1775 17.16 17.17 Fe203 (LOI-free) 2.95 2.82 2.62 2.62 2.48 5.17 3.47 3.02 MnO (LOI-free) 0.05 0.08 0.03 0.03 0.05 0.03 0:06 0:04 MgO (LOI-free) 1.12 0.75 1.14 1.14 l.ll 157 1.77 1.78 CaO (LOI-free) 2.61 7.39 2.56 2.46 2.52 2.14 4.82 4.02 NajO (LOI-free) 10.28 3.92 6.10 6.15 5.79 1.11 3.30 0.54 K2O (LOI-free) 0.55 2.63 1.53 I.S4 1.58 4.50 3.62 4.75 P2OS (LOI-free) 0.22 0.15 0.14 0.14 0.17 0.13 0.16 0.16 Si02(MC) -19:92 1.59 -0.25 -1.26 -1.17 4.50 -1.74 8.70 Ti02(MC) 0.00 0.03 0.00 -0.02 0.00 0.09 0.00 0.04 AW)3(MC) -1.11 0.04 -0.54 -0,76 -0.71 2.56 0.53 2.45 Fe!03(MC) -0.88 -0.20 -0.60 -0.64 -0.78 2.46 0.33 0.21 MnO(MC) -O.02 0.02 -0.03 -0.03 -0.01 -0.03 0.00 -0.01 MgO(MC) -0.38 -0.46 -0.14 -0.16 -0.19 1.54 0.53 0.74 CaO(MC) -2:02 3.70 -1.53 -1.67 -1.62 -1.70 0.81 0.46 Na20 (MQ 3.05 -0.77 1.07 1.02 0.67 -3.66 -1.55 •421 KJO(MC) -1.71 0.61 -0.65 -0.65 -0.62 2.75 1.51 3.17 P20s(MC) 0.02 0.01 -0.01 -0.01 0:01 -0.01 0.02 0.03 Se(MC) 0.40 0.10 0.20 0.30 0.70 2.70 0.20 0.60 Zr(MC) 33.50 -4.90 3.10 4.90 5.20 -8.80 -0.50 -11.60 Nb(MC) 0.60 -0.10 0.10 0J0 0.70 -0.50 -0.10 -0.60 Y(MQ 0.37 4.98 0.61 0.85 1.34 1.78 0.07 -0.93 La(MQ 0.59 7.57 1.95 2.24 2.99 -1.20 1.88 1.60 YbfMC) 0.04 0.21 0.05 0.05 0.09 0.16 -0.04 -0.12 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/IOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Tixnmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite. Sample 03-PJM-007a 03-PJM-O07C 03-PJM-008 03-PJM-009 03-PJM-fllO 03-PJM-152a 03-PJM-152b 03-PJM-146 Suite TlS-maincamp^ US-main camp TlS-main camp TIS-main camD TIS-main camp TIS-main camp TIS-main camp TIS-maincamo Zr(EF) 1.223 1.020 0.961 1.154 1.253 1.263 1.259 1.050 SH>! (LOI-free) 66.32 68.66 66.33 67.59 64.30 68.12 68.65 65.30 TiCfc (LOI-free) 0.34 0.36 037 0.35 0.33 0.33 0.32 0.41 AI2O3 (LOI-free) 16.73 17.65 18.54 16.72 15.99 17.14 16.81 16.72 Fe203 (LOI-ftee) 2.90 3.89 3.54 4.98 6:49 2.54 2.42 5.35 MnO (LOI-free) 0.01 0.07 0.11 0.12 0.17 0.06 0.07 0.03 MgO (LOI-free) 1.65 Z06 1.82 232 2.07 135 121 1.73 CaO (LOI-free) 3.58 1.81 2.60 2.32 4.36 4.25 4.72 3.15 Na20 (LOI-free) 6.18 0.25 2.69 2.14 3.92 3.84 3.23 5.43 K20 (LOI-free) -2.18 5.11 3.87 334 126 228 2.41 1.72 P2O5 (LOI-ftee) 0.12 0.14 0.14 0.12 0.12 0.10 0.11 0.16 SiOJ (MC) 13.80 2.71 -3.55 10.68 13.27 18.73 19.10 1.21 Ti02(MC) 0.07 0.02 0.01 0.06 0.07 0.07 0.05 0.08 AI203(MC) 3.76 1.30 1.12 2.60 334 4.94 4.45 0.85 Fa03(MC) 0.40 0.81 0.25 2.60 4.98 0.05 -0.10 2.47 MnO (MC) -O.05 0.01 0.04 0.07 0.15 0.02 0.03 -0.03 MgO(MC) 0.77 0.86 0.50 1.43 1.35 0.46 0.34 0.57 CaO(MQ 0.36 -2.18 -1.53 -134 1.44 134 1.92 -0.72 NaJO(MC) 2.70 ^t.61 -2.28 -2.40 0.04 -0.02 -0.81 0.83 IOO(MC) 0.53 3.08 1.59 1.72 0.71 0.74 0.91 -0.33 P205 (MC) 0.00 -0:01 -0.01 -0.01 0.00 -0.01 -0.01 0.02 Sc(MC) -0.40 0.10 0.20 0.10 0.10 -0.70 -0.70 0.60 Zr(MC) -20.50 -2.20 4.50 -15.00 -22.70 -23.40 -23:10 -5.30 Nb(MQ -0.60 -0.40 -0.20 -0-50 -0.60 -120 -1.10 0.00 ¥(MC) -1.92 -0.27 -0.23 -0.16 -0.15 -1.98 -1.44 0.16 La(MC) -4.40 -0.47 0.80 1.67 -1:94 -4.17 -4.57 -0.24 YbfMCl -0.22 -0.05 -0.08 -0.11 -0.10 -0.24 -0.19 -0.04 Sample 03-PJM-149 03-PJM-001 03-PJM-602 03-P.IM-004 03-PJM-811 03-PJM-015 03-PJM-O22 03-PJM-028 Suite TlS-inaincamo TlS-main carno TIS-maincamo TIS-main camp TIS-main camp TIS-main camp TIS-main camp TIS-main camp. ZrffiF) 1.066 1.036 1.028 0.953 1.066 1.081 1.042 1.086 S1O2 (LOI-free) 65.39 66.50 63.32 68.11 72.24 71:28 73.11 73:87 TiOl (LOI-ftee) 0.46 0.36 0.39 0.37 0.23 0.21 0.21 0.24 AW>3 (LOI-ftee) 17.46 16.99 17.80 17.12 15.53 15.80 16.01 15.72 FeOJ (LOI-free) 2.21 3.12 2.94 3.61 1.39 1.58 1.76 1.29 MnO (LOI-free) 0.03 0.03 0.04 0.00 0.03 0.03 0.06 0:01 MgO (LOI-free) 2.07 1.39 1.29 1.18 0.64 0.63 0.71 0.54 CaO (LOI-free) 4.22 3.35 3.37 0.82 2:86 3.33 136 1.07 NalO (LOI-ftee) 5.33 6.95 10.35 7.69 3.92 4.49 3.09 4.44 K2O (LOI-free) 2.63 1.19 0.29 0.96 3.08 2.56 3.61 2.74 P2O5 (tOI-ircc) 0.19 0.15 0.21 0.15 0.07 0.08 0.08 0.08 SK>2(MC) 2.42 1.57 -2.21 -2.39 9.72 9.72 8.84 12.91 Ti02(MC) 0.15 003 0.06 O.01 -0.10 -0.12 -0.13 -0.09 AI2O3 (MC) 1.92 0.90 1.60 -0.38 -0.14 0.38 -0.03 0.37 Fe203(MQ -O.80 0.08 -0.13 0.29 -1.67 -1.44 -1.32 -1.75 MnO (MC) -0.03 -0.03 -0.02 -006 -0.03 -0.03 0.00 -0.05 MgO (MC) 0.96 0.19 0.08 -0.13 4)56 -0.56 -O.50 -0.66 CaO Suite TlS-main camp TlS-main camp TlS-main camp TlS-main camp TIS-main camp TlS-main camp Zr(EF) 1.044 1.416 1.075 1.564 1.420 1.101 S1O2 (LOi-free) 71.55 68.49 72.47 69.19 69.74 73.33 T1O2 (LOI-free) 0.24 0.29 0.22 0.25 0.28 0.22 AI2O3 (LOI-free) 15.23 16.52 14.98 15.88 16.54 15.44 FelQ) (LOI-free) 1.45 2.01 1.52 1.96 2.27 1.96 MnO (LOI-free) 0.03 0.05 0.03 0.09 0.03 0.06 MgO (LOI-free) 1.24 1.39 0.70 1.13 2.32 0.75 CaO (LOI-free) 0.37 1.71 3.48 5.19 0.17 2.19 Na20 (LOI-free) 9.69 9.38 4.83 3.79 8.47 3.13 K2O (LOI-free) 0.11 0.07 1.70 2.45 0.11 2.81 P2O5 (LOI-free) 0.08 0.08 0.07 0.07 0.09 0.10 S1O2 (MC) 7.35 29.67 10.56 40.89 31.68 13.42 TiOz (MC) -0.09 0.06 -0.11 0.05 0.05 -0.10 Ah03(MQ -0.81 6.70 -0.61 8.13 6.77 0.30 Fe203 (MC) -1.64 -0.30 -1.52 -0.08 0.07 -0.99 MnO (MC) -0.03 0.01 -0.03 0.09 -0.02 0.01 MgO(MQ 0.05 0.71 -0.50 0.52 2.05 -0.43 CaO(MC) -3.64 -1.60 -0.28 4.09 -3.79 -1.62 NalO(MC) 5.25 8.42 0.32 1.06 7.15 -1.42 K20(MC) -2.02 -2.03 -0.31 1.70 -1.98 0.96 P205(MC) -0.06 -0.03 -0.07 -0.03 -0.02 -0.04 Sc(MC) -1.11 0.52 -1.15 0.30 0.82 -0.66 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) -1.93 -0.81 -1.67 -0.84 -0.66 -1.74 ¥(MC) -3.10 -0.90 -2.72 -0.64 -0.89 -2.10 La(MC) -6.74 -5.63 -4.68 -7.25 -5.75 -3.87 Yb(MC) -0.31 -0.13 -036 -0.13 -0.16 -0.30 Saraple 04-PJM-300 04-PJM-299 04-PJM-234 04-PJM-235 04-PJM-238 04-PJM-239 04-PJM-241 04-PJM-243 Suite TIS-other TIS-other TlS-omei TIS-other TIS-other TIS-other TIS-other TIS-other ZrlEF) 1.497 1.238 1.270 1.097 1.300 1.279 0.925 1.125 S1O2 (LOI-free) 61.84 60.40 73.14 65.17 72.15 65.45 63.81 73.45 T1O2 (LOI-free) 0.51 0.60 0.13 0.23 0.13 0.17 0.49 0.19 AI2O3 (LOI-free) 12.93 15.17 15.79 19.38 16.08 18.97 16.54 14.65 Fe203 (LOI-free) 5.39 5.60 1.05 1.62 1.11 0.87 4.14 1.09 MnO (LOI-free) 0.12 0.10 0.02 0.02 0.01 0.05 0.07 0.02 MgO (LOI-free) 5.09 5.13 0.24 0.69 0.58 0.89 2.66 0.56 CaO (LOI-free) 9.29 6.24 2.02 2.30 1.49 2.66 3.43 1.07 Na20 (LOI-free) 2.98 5.51 6.00 10.39 6.58 10.09 7.26 8.68 K2O (LOI-free) 1.74 1.07 1.55 0.16 1.82 0.72 1.40 0.25 P2O5 (LOI-free) 0.11 0.17 0.06 0.06 0.04 0.13 0.19 0.04 SK)2(MQ 25.27 7.46 25.59 4.15 26.45 16.39 -8.29 15.32 T1O2 (MC) 0.42 0.40 -0.17 -0.10 -0.17 -0.13 0.11 -0.13 AI203 (MQ 2.66 2.08 3.36 4.55 4.19 7.56 -1.40 -0.22 FeOs(MC) 4.92 3.78 -1.82 -137 -1.71 -2.03 0.68 -1.92 MnO (MQ 0.11 0.06 -0.04 -0.04 -0.05 0.00 0.00 -0.04 MgO(MC) 6.37 5.11 -0.94 -0.49 -0.49 -0.12 1.21 -0.62 CaO(MC) 9.88 3.70 -1.46 -1.50 -2.09 -0.63 -0.85 -2.82 Na20 (MC) -0.40 1.96 2.76 6.52 3.69 8.04 1.85 4.90 faO(MC) 0.47 -0.80 -0.17 -1.96 0.24 -1.21 -0.83 -1.86 P20s(MC) 0.02 0.06 -0.08 -0.08 -0.09 0.03 0.03 -0.10 Sc(MC) 11.37 10.94 -1.27 -1.00 -1.48 -1J25 3.92 -1.61 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) 0.84 0.96 -1.98 -1.96 -1.81 -2.09 -1.O0 0.21 Y(MC) 3.62 1.86 -2.10 -3.13 -3.69 -3.49 2.21 -2.95 La(MQ -2.07 -3.11 -3.09 -6.09 -5.54 -5.31 17.60 0.03 YbfMC) 0.28 0.17 -0.33 -0.38 -0.46 -0.46 0.16 -0.36 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite. 185 Sample 04-P.IM-244 04-P.IM-245 IH-PJM-248 04-PJM-249 04-PJM-2S1 04-PJM-252 04-PJM-275 04-PJM-276 Suite TlS-olher TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other ZrfEFI 1.522 1.553 2.315 2.260 2.260 1.404 1.406 1.434 Si02 (LOI-free) - 74 21 74.61 73.78 73.72 70.43 61.52 66.54 65.64 TK)2 (LOI-free) 0.12 0.12 0.06 0.07 0.07 0.24 0.29 0.29 AW)3 (LOI-free) 14.75 14.45 15.97 15.69 16.82 17.71 17.73 18.05 Te203 (LOI-free) 1.15 1.01 1.46 1.07 1.12 1.75 3.74 3.32 MnO (LOI-free) 0.02 0.02 0.00 0.01 0.02 0.03 0.05 0.05 MgO (LOI-free) 0.21 0.22 0.32 0.16 0.47 3.73 1.25 1.38 CaO (LOI-free) 0.66 0.80 0.13 0.56 1.21 4.37 3.81 4.31 Na20 (LOI-free) 8.73 8.60 6.72 7.71 9.74 10.48 4.98 4.30 K2O (LOI-free) 0.11 0.10 1.51 0.96 0.08 0.13 1.49 2.56 P2Q5 (LOI-free) 0.03 0.07 0.06 0.07 0.06 0.06 0.11 0.11 SK>2(MQ 45.59 48.57 103.51 99.24 91.81 19.03 26.20 26.82 Ttt>2 (MC) -0.16 -0.15 -0.21 -0.19 -0.19 -0.01 0.07 0.08 Al203(MC) 5.74 5.74 20.26 18.75 21.30 8.15 8.22 9.19 Fe203 (MC) -1.39 -1.58 0.23 -0.74 -0.63 -0.70 2.11 1.60 MnO (MC) -0.03 -0.03 -0.05 -0.04 -0.03 -0.02 0.00 0.01 MgO (MC) -0.92 -0.90 -0.50 -0.90 -0.18 3.98 0.52 0.72 CaO(MC) -3.02 -2.78 -3.71 -2.77 -1J28 2.10 1.33 2.15 Na20 (MC) 8.42 8.49 10.68 12.56 17.14 9.84 2.14 1.29 K20(MC) -1.96 -1.98 1.36 0.03 -1.96 -1.94 -0.04 1.54 P205(MO -0.09 -0.04 -0.02 0.01 -0.02 -0.07 0.01 0.02 Sc(MC) -1.63 -1.28 -1.91 -1.94 -1.94 2.03 1.06 1.29 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) 2.89 2.40 0.67 0.57 0.57 -1.11 -0.41 -0.49 Y(MC) -1.66 -0.91 -1.15 -1.38 -1.06 -1.37 -1.33 -1.31 La(MC) -5.69 All -9.95 -3.73 -4.05 AM -4.72 -4.21 Yb(MC) -0.30 -0.29 -0.35 -0.34 -0.34 -0.22 -0.21 -0.20 Sample 04-PJM-277 04-PJM-278 04-PJM-283 04-PJM-286 04-PJM-287 04-PJM-288 04-PJM-292 04-PJM-293 Suite TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other ZrffiF) 1.551 1.511 1.021 1.402 1.366 1.425 1.318 1.564 Si02 (LOI-free) 67.61 67.81 61.34 65.43 66.16 67.67 65.71 65.60 TKU (LOI-free) 0.24 0.25 0.46 0.30 0.28 0.26 0.28 0.32 AI203 (LOI-free) 17.53 17.81 17.53 17.49 17.68 17.60 18.53 17.68 Fe203 (LOI-free) 3.35 2.70 5.82 3.57 1.92 1.62 2.61 3.51 MnO (LOI-free) 0.04 0.04 0.13 0.10 0.08 0.07 0.06 0.10 MgO (LOI-free) 1.06 1.02 3.86 2.09 1.26 1.05 1.41 1.70 CaO (LOI-free) 2.74 2.56 6.13 4.98 4.92 4.00 2.98 4.78 Na20 (LOI-free) 5.52 6.42 2.18 2.54 4.80 5.17 7.43 4.14 K20 (LOI-free) 1.83 1.31 2.33 3.38 2.78 2.44 0.86 2.06 PlOJ (LOI-free) 0.09 0.09 0.22 0.12 0.11 0.12 0.12 0.10 SI02 (MC) 37.54 35.17 -4.70 24.42 23.07 29.11 19.29 35.28 Ti02(MC) 0.03 0.03 0.13 0.08 0.04 0.02 0.03 0.16 A1203 (MC) 10.48 1021 1.19 7.81 7.45 8.38 7.72 10.95 Fe203(MQ 2.04 0.93 2.79 1.85 -0.53 -0.84 0.29 2.33 MnO(MC) 0.00 -O.01 0.07 0.08 0.05 0.03 0.02 0.10 MgO (MC) 0.40 0.30 2.69 1.68 0.48 0.25 0.61 1.41 CaO(MC) 0.22 -0.16 223 2.95 2.69 1.67 -0.10 3.45 Na20(MC) 3.69 4.84 -2.64 -1.30 1.70 2.50 4.93 1.61 K20(MQ 0.70 -0.16 0.25 2.61 1.67 1.35 -1.00 1.08 PlOsfMC) -0.01 -0.01 0.08 0.03 0.01 0.03 0.02 0.01 Sc(MQ 0.11 0.18 3.13 1.61 -0.29 -0.59 0.92 2.80 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) -0.09 -0.17 0.58 0.00 -0.36 -0.36 -0.47 0.25 YfMC) -1.89 -2.01 0.58 -1.54 -2.73 -2.95 -1.80 -0.72 La(MC) -4.52 -3.85 6.66 -3.43 ^t.83 -5.93 -4.35 -5.33 YbflvfO -0.29 -0.28 -0.11 -0.22 -0.36 -0.37 -0.26 -0.13 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite. 186 Sample 04-PJM-294 04-PJM-2W, 04-PJM-297 04-PJM-2S6 04-PJM-2S7 04-PJM-221 04-PJM-222 04-PJM-223 Suite TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other TIS-other Zr(EF) 1.483 1.497 1.429 1.579 2.185 0.842 0.838 0.842 S1O2 (LOI-free) 66.36 66.33 65.28 68.38 69.27 73.99 69.82 66.66 T1O2 (LOI-free) 0.29 0.32 0.34 0.23 0.17 0.23 0.36 0.42 AI2O3 (LOI-free) 17.77 17.57 18.51 17.41 16.40 15.46 16.49 17.43 Te203 (LOI-free) Z26 3J8 3.10 1.87 1.82 0.77 2J7 3.42 MnO (LOI-free) 0.11 0.08 0.08 0.03 0.03 0.01 0.04 0.06 MgO (LOI-free) 1.57 1.73 1.53 0.98 0.90 0.07 1.02 1.97 CaO (LOI-free) 4.93 3.53 4.57 2.44 3.09 0.18 3.76 2.10 Na20 (LOI-free) 4.69 6.00 5.30 7.55 7.37 9.10 3.64 6.75 K2O (LOI-free) 1.90 0.96 1.18 1.03 0.90 0.09 2.36 1.07 P2OS (LOI-free) 0.11 0.09 0.10 0.09 0.06 0.10 0.12 0.12 SK)2(MC) 31.13 32.00 25.95 40.67 84.02 -5.04 -8.81 -11.21 Ti02(MQ 0.09 0.14 0.15 0.02 0.02 -0.15 -0.04 0.01 AtrOJ(MC) 9.65 9.61 9.74 10.79 19.13 -3.68 -2.88 -2.03 Fe203 (MC) 0.20 1.91 128 -0.20 0.84 -2.51 -1.16 -0.27 MnO(MC) 0.10 0.05 0.05 -0.02 -0.01 -0.05 -0.03 -0.01 MgO (MQ 1.08 1.35 0.94 0.3! 0.72 -1.19 -0.39 0.41 CaO(MC) 3.29 1.27 2.51 -0.17 2.73 -3.88 -0.87 -2.25 Na20(MQ 2.10 4.12 2.71 7.05 11.22 2.80 -1.82 0.82 KiO(MC) 0.68 -0.70 -0.45 -0.51 -0.16 -2.06 -0.15 -1.23 P!05(MO 0.02 -0.01 0.00 -0.01 -0.02 -0.06 -0.04 -0.04 Sc(MC) 0.71 3.14 3.13 0.17 1.73 -2.46 -0.95 1.16 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.0O Nb(MC) -0.53 0.39 0.36 -0.66 0.00 -0.81 1.11 0.37 Y(MC) -1.90 -0.62 -0.89 -2.70 -0.78 -2.77 -1.15 0.42 La(MC) ^1.57 -6.50 -6.61 -6.41 -6.66 8.32 0.11 0.35 Yb(MQ -0.27 -0.12 -0.16 -0.33 -0.21 -0.43 -0.21 -0.01 Sample 04-PJM-224 04-PJM-225 03-PJM-153 04-PJM-227 04-PJM-228 Suite TIS-other TIS-other TIS-other TIS-other TIS-other Zr (EF) 1.023 0.929 1.229 1.039 1.182 Si02 (LOI-free) 67.53 68.70 71.80 74.85 71.81 T1O2 (LOI-free) 0.40 0.42 0.20 0.26 0.20 Ah03 (LOI-free) 16.31 16.40 15.60 15.93 16.11 Fe203 (LOI-free) 3.18 3.25 1.82 0.43 1.82 MnO (LOI-free) 0.05 0.09 0.04 0.02 0.02 MgO (LOI-free) 2.07 1.69 0.73 0.40 0.83 CaO (LOI-free) 3.40 2.89 3.62 1.79 2.40 Na20 (LOI-free) 5.06 4.03 5.22 3J8 4.86 K2O (LOI-free) 1.86 2.40 0.91 2.88 1.89 P2O5 (LOI-free) 0.12 0.13 0.07 0.08 0.07 S1O2 (MC) 1.75 -3.51 20.90 10.43 17.56 Ti02 (MC) 0.07 0.04 -0.10 -0.08 -0.10 AI2O3 (MC) -0.02 -1.47 2.46 -0.16 2.34 Fe203(MQ 0.10 -0.14 -0.92 -2.71 -1.00 MnO(MC) -0.01 0.02 -0.01 -0.05 -0.03 MgO(MC) 0.87 0.32 -0.35 -0.83 -0.27 CaO(MC) -0.55 -1.34 0.42 -2.16 -1.19 Na20(MQ 0.31 -1.12 1.54 -1.36 0.88 K20(MQ -0.23 0.10 -1.02 0.86 0.10 P205(MQ -0.02 -0.02 -0.06 -0.06 -0.07 Sc(MQ 2.02 1.16 -1J3 -039 -0.94 Zr(MC) 0.00 0.00 0.00 0.00 0.00 Nb(MQ 0.59 0.31 0.19 -0.59 0.16 Y(MC) 0.86 -0.51 -1.35 -1.83 -1.41 La(MC) 1.82 0.87 9.40 -0.17 0.28 YblMO 0.00 -0.11 -0.24 -0.24 -0.24 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite. 187 Sample 03-PJM-142a 03-PJM-142f 03-PJM-142h 03-PJM-142i 03-PJM-142J 03-PJM-142* Suite CIS CIS as CIS CIS CIS Zr(EF) 0.981 1.000 0.963 0.984 Q.958 0.994 S1O2 (LOI-free) 71.84 69.17 69.90 70.58 71.96 70.47 TiOl (LOI-free) 0.26 0.28 0.29 0.27 0.28 0.27 Ah03 (LOI-free) 15.14 15.36 15.67 15.05 15.86 15.24 Fe203 (LOI-free) 1.91 2.87 3.00 2.11 2.01 2.39 MnO (LOl-ftee) 0.00 0.00 0.01 0.00 0.00 0.00 MgO (LOI-free) 0.95 0.99 0.93 0.84 1.06 0.67 CaO (LOI-free) 1.97 0.97 1.70 1.09 1.41 1.91 NazO (LOI-free) 5.78 4.63 5.89 5.06 3.67 8.46 K20 (LOI-free) 2.07 5.64 2.53 4.92 3.65 0.52 P2O5(L0I-free) 0.07 0.09 0.08 0.08 0.08 0.08 S102(MC) 1.31 0.00 -1.89 0.25 -0.21 0.91 TiOa (MC) -0.02 0.00 0.00 -0.01 0.00 -0.01 A1203 (MC) -0.51 0.00 -0.28 -0.56 -0.16 -0.20 FeOl(MC) -1.00 0.00 0.01 -0.79 -0.94 -0.50 MnO(MC) 0.00 0.00 0.01 0.00 0.00 0.00 MgO(MC) -0.06 0.00 -0.10 -0.16 0.03 -0.32 CaO (MC) 0.96 0.00 0.67 0.10 0.38 0.93 NaJO(MQ 1.04 0.00 1.04 0.35 -1.11 3.78 K20(MC) -3.60 0.00 -3.20 -0.79 -2.14 -5.12 P20s(MQ -0.02 0.00 -0.01 -0.01 -0.01 -0.01 Sc(MC) -036 0.00 0.26 -0.15 -0.14 -0.52 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) -0.15 0.00 -0.10 0.05 -0.40 0.18 Y(MQ -0.08 0.00 1.01 0.36 -3.85 0.74 La(MC) 3.60 0.00 0.18 -2.63 -1.36 5.80 Yb(MC) 0.04 0.00 0.07 0.05 -0.24 0.08 Sample 04-PJM-2S8 04-PJM-259 04-P.IM-262 04-PJM-263 04-PJM-265 D4-PJM-261a Suite HIS HIS HIS HIS HIS HIS Zr(EF) 0.716 1.000 4.383 6.043 1.533 3.033 SiO! (LOI-free) 58.66 62.79 63.18 66.02 67.60 70.71 T1O2 (LOI-free) 0.63 0.50 0.35 0.32 0.31 0.09 AI1O3 (LOI-free) 18.06 14.51 20.93 19.01 19.05 15.72 FeiOJ (LOI-free) 5.85 4.91 2.69 1.63 2.89 0.66 MnO (LOI-free) 0.10 0.13 0.04 0.02 0.06 0.02 MgO (LOI-free) 3.56 3.19 1.26 0.77 0.62 0.07 CaO (LOI-free) 4.42 7.27 0.84 1.56 3.45 1.50 Na:0 (LOI-free) 7.81 5.95 9.77 9.99 4.98 5.76 KlO (LOI-free) 0.13 0.14 0.78 0.55 0.90 5.44 P2O5 (LOI-free) 0.77 0.60 0.16 0.13 0.14 0.03 Si02 (MC) -20.81 0.00 214.09 336.13 40.85 151.70 Ti02 (MQ -0.05 0.00 1.02 1.45 -0.03 -0.23 Al:OJ(MQ -1.59 0.00 77 22 100.38 14.69 33.17 Fe203 (MC) -0.73 0.00 6.90 4.91 -0.47 -2.90 MnO(MC) -0.06 0.00 0.04 0.02 -0.04 -0.08 MgO(MQ -0.64 0.00 2.35 1.46 -2.24 -2.98 CaO(MC) -4.11 0.00 -3.60 2.15 -1.99 -2.71 Na20(MQ -0.36 0.00 36.88 54.43 1.69 11.51 K20(MC) -0.05 0.00 3.29 3.15 1.23 16.36 PiOS(MQ -0.05 0.00 0.08 0.21 -0.38 -0.50 Sc(MC) -1.79 0.00 3.91 8.72 -1.13 -6.68 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) 0.36 0.00 -1.89 -1.31 2.42 -2.47 V(MC) -3.33 0.00 -13.75 19.65 -1.61 -10.98 La(MC) -19.86 0.00 -65.05 -59.40 9.41 -82.78 Yb(MCD -0.29 0.00 -0.61 0.87 0.13 -0.52 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Hornier intrusive suite; and GIS= granodiorite intrusive suite. 188 Sample 04-PJM-2S3 04-PJM-233 04-PJM-229 03-PJM-131g 03-P4M-l41b 03-PJM-141f Suite GIS GIS GIS GIS GIS GIS ZrffiFI 0.795 1.032 1.000 0.936 1.097 0.872 Si02 (LOI-free) 75.31 73.96 71.23 69.51 66.81 67.09 T1O2 (LOI-free) 0.27 0.25 0.28 0.32 0.31 0.32 AI2O3 (LOI-free) 14.41 15.26 15.59 15.60 15.60 16.88 Fe203 (LOI-free) 0.98 1.49 1.45 1.73 1.98 1.63 MnO (LOI-free) 0.01 0.01 0.03 0.02 0.03 0.02 MgO (LOI-free) 0.14 0.46 0.50 0.79 1.18 0.87 CaO (LOI-free) 0.26 0.22 1.67 2.02 4.14 2.12 Na20 (LOI-free) 6.53 6.20 5.42 6.41 7.88 8.37 IQO (LOI-free) 1.92 2.02 3.68 3.48 1.95 2.60 P2O5 (LOI-free) 0.17 0.13 0.17 0.13 0.11 0.12 S102(MC) -11.35 5.09 0.00 -6.14 2.06 -12.72 TiOJ(MC) -0.06 -0.01 0.00 0.02 0.07 0.00 Al203(MC) ^.14 0.15 0.00 -0.98 1.52 -0.88 Fe!03 (MC) -6.67 0.09 0.00 0.17 0.73 -0.03 MDO (MC) -0.02 -0.02 0.00 -0.01 0.01 -0.01 MgO (MC) -0.39 -0.02 0.00 0.24 0.80 0.26 CaO (MC) -1.46 -1.44 0.00 0.22 2.87 0.18 Na20 (MC) -0.23 0.97 0.00 0.58 3.22 1.87 K20(MC) -2.15 -1.60 0.00 -0.42 -1.54 -1.41 P20S(MC) -0.03 -0.03 0.00 -0.04 -0.04 -0.06 Sc(MC) -0.39 0.36 0.00 0.19 0.69 0.07 Zr(MC) 0.00 0.00 0.00 0.00 0.00 0.00 Nb(MC) -1.84 -1.20 0.00 -1.58 -1.56 -1.68 Y(MC) -0.79 0.86 0.00 0.21 -0.34 -0.41 La(MC) 4.06 -7.53 0.00 -».33 -6.72 -8.11 Yb(MC) -0.06 0.08 0.00 0.00 -0.01 -0.04 Sample 04-PJM-217 04-PJM-2J8 (P4-PJM-255 Suite FVS FVS FVS ZrffiFI 1.000 1.197 0.980 Si02 (LOI-free) 67.15 73.81 66.85 T1O2 (LOI-free) 0.43 0.25 0.47 AbOJ (LOI-free) 17.60 15.81 17.60 Fe203 (LOI-free) 3.64 1.15 3.58 MnO (LOI-free) 0.07 0.02 0.07 MgO (LOI-free) 0.88 0.42 1.66 CaO (LOI-free) 3.31 0.90 3.81 Na20 (LOI-ftee) 4.94 6.12 4.08 K20 (LOI-free) 1.79 1.46 1.69 P2OS (LOI-free) 0.19 0.06 0.20 Si02 (MC) 0.00 21.20 -1.64 T1O2 (MC) 0.00 -0.14 0.03 AI2O3 (MC) 0.00 1.32 -0.36 Fe203 (MC) 0.Q0 -2.26 -0.12 MaO(MC) 0.00 -0.05 -0.01 MgO(MC) 0.00 -0.38 0.75 CaO(MQ 0.00 -2.22 0.43 NalO (MC) 0.00 2.38 -0.95 K20(MQ 0.00 -0.04 -0.14 P2O5 (MC) 0.00 -0.12 0.01 Sc(MC) 0.00 -7.24 -3.40 Zr(MC) 0.00 0.00 0.00 Nb(MC) 0.00 1.96 -0.19 Y(MC) 0.00 -8.30 -1.98 La(MC) 0.00 -9.44 -2.05 YhfMO 0.00 -0.98 -0.45 Table Bl, continued. Table of Zr enrichment factors (EF), LOI-free major element abundances and relevant absolute mass change values (MC) expressed in g/lOOg with precursors indicated by shading. MC calculations via single precursor systems method (Barrett and MacLean 1994). TIS = Timmins porphyry intrusive suite; CIS = Carr Township porphyry intrusive suite; HIS = Holmer intrusive suite; and GIS= granodiorite intrusive suite.