Geology and Mineralization of the Island Copper Property, Sault Ste. Marie, Ontario
A. Hamid Mumin, Ph.D., P.Eng And John Camier, B.Sc. (Specialist)
February, 2002
GEOLOGY AND MINERALIZATION
of the
ISLAND LAKE PROPERTY,
SAULT STE. MARIE, ONTARIO
February, 2002
Prepared by
A. Hamid Mumin, Ph.D., P. Eng. and John Camier, B.Sc. (Specialist)
Department of Geology, Brandon University, Brandon, Manitoba, Canada, R7A 6A9
Table of Contents
Title Page…………………………………………………….…………………………….i
Table of Contents…………………………………………………………..…...…………ii
List of Tables……………………………………………………………………………..iv
List of Figures…………………………………………………………………………….iv
Summary..…………………………………………………………………………………1
Introduction and Terms of Reference……………………………………………………..3
Disclaimer…………………………………………………………….…………………...3
Property Description and Location………………………….………….…………………4
Accessibility, Infrastructure, Local Resources, Climate and Physiography………………4
History and Previous Work on the Island Copper Property……...……………………….9
Geological Setting………………………………………………………………………..17
Geology and Mineralization of the Island Copper Property ..…………..………27
Deposit Types……………………………………………………………………..……..31
Mineralization……………………………………………………………………………33
Exploration of the Island Copper Property...…………………………………………….34
Geophysics……………………………………………………………………….35
Drilling on the Island Copper Property……..…………………………………………...36
Sampling Method and Approach………………………………………………………...38
Sample Preparation, Analyses and Security……………………………………………..38
Data Verification…………………………………………………………………………38
iii Mineral Resource and Reserve Estimates…..……………………………………………39
Other Relevant Data ……………………………………………………………………39
Interpretation and Conclusions…………………………………………………………..39
Recommendations……………………………………...………………………………...42
References………………………………………………………………………………..43
Certificates……………………………………………………………………………….45
Appendix 1: Petrographic Reports………….……………………………………………47
Appendix 2: Whole Rock Geochemistry...………………………………………………57
iv List of Tables
Table 1: Claim Standing………………………………………………………………….7
Table 2: Summary of Exploration..…………………………………………………..….10
Table 3: Significant Drill Hole Assays...…………………………………………..…….11
Table 4: Summary of Historical Drilling…………………………………….…………..37
List of Figures
Figure 1: Location Map………………………………………….……………….….……5
Figure 2: Property Claims and Patents.…………………………….………….………….6
Figure 3: Historical Drill Hole Locations….………………………………..……….…..12
Figure 4: Historical Drill Hole Locations.…………………………………….…………13
Figure 5: Historical Drill Hole Locations.…………………………………….…………14
Figure 6: Historical Drill Hole Locations.…………………………………………….…15
Figure 7: Geology of the Island Copper Property………………………………….……18
Figure 8: Residual Gravity…………………………………………………………….…19
Figure 9: IP - Fraser Filtered Chargeability…...……………………………...…………20
Figure 10: Residual Aeromagnetic Data - Regional…………………..…………………21
Figure 11: Aeromagnetic Data and Mineral Occurrences.………………………………22
Figure 12: Regional Geology….…………………………………………………………24
Figure 13: Trench at the Main Copper Showing – Photograph….………………………26
Figure 14: Geological Contact Between the Gros Cap Gneiss Breccia and Mineralized Albite Granite Breccia - Photographs…….……….………………………..30
Figure 15: Schematic Geological Model for Island Copper Mineralization…..…………41
v Summary
This report on the Geology and Mineralization of the Island Copper Property was prepared at the request of the Directors of Golden Temple Mining Corporation (hereafter referred to as the Company). The report describes the geology and mineral potential of the property, and presents a summary of the relevant geological work that has been carried out to date.
The Island Copper property is located approximately 19 kilometres northeast of Sault Ste. Marie, Ontario, north of the cottage community of Island Lake (Figure 1). The property is situated northwest of the junction between Highways 556 and 552, and straddles Highway 552. The Island Copper property is comprised of four Falconbridge claims, three YMCA patents and the Nystedt leasehold patents (Figure 2, Table 1).
The property hosts significant copper mineralization in altered, hematite-rich albite granite breccias at and near the contact with Gros Cap granite and granodiorite gneiss. The mineralized breccias occur near the intersection of major structures, and are accompanied by alkali metasomatism (Na +/- K enrichments), and chlorite, amphibole and Fe-oxide alteration. The copper occurs as chalcopyrite associated with pyrite and Fe-oxides.
At least 37 diamond drill holes were previously drilled on the southeastern portion of the property to a maximum vertical depth of ~ 137 meters. Copper values are reported for most of the drill holes, but cannot be independently verified due to improper storage of the core. Recent work includes detailed geology, surface sampling, and magnetic, gravity and chargeability geophysical surveys. Coincident chargeability and gravity anomalies remain largely untested.
It is recommended that this property be further explored in the light of recent advances in the understanding of Fe-oxide copper-gold type deposits. The historical diamond drilling and surface data needs to be replotted and evaluated for: 1) any trends in copper grades, 2) variations in intensity and type of alteration mineralogy, 3) variations in the style and intensity of brecciation, and 4) the association of major and subordinate structures with brecciation, hydrothermal alteration and mineralization. These evaluations combined with a general and thorough overall property evaluation, including the current geology and
1 geophysics should be carried out prior to any decision regarding how much and where further diamond drilling is conducted.
It is also recommended that the assay procedures be tested using several independent methods (including NAA) on splits of the same sample, in order to determine the best method to assay for copper and gold in this particular deposit.
2 Introduction and Terms of Reference
This report on the Geology and Mineralization of the Island Copper Property was prepared at the request of the Directors of Golden Temple Mining Corporation (hereafter referred to as the Company), in order to fulfill certain regulatory reporting requirements following the signing of an Option and Joint Venture Agreement between Falconbridge Limited and Golden Temple Mining Corp. The report describes the geology and mineral potential of the property, and presents a summary of the relevant geological work that has been carried out to date. This report is an independent geological assessment of the property as of the date of writing.
Both writers have previously investigated this property. A petrographic report was prepared by Camier and Mumin (1999) for Falconbridge, describing the petrography of selected samples from the Island Copper property (Appendix 1). Mr. Camier visited the property briefly in the summer of 1999, and carried out detailed mapping and sampling of the property for 6 weeks in July-August, 2000, and a further 2 weeks in July, 2001. Mr. Camier researched the historical work on this property in 2000 and 2001, and prepared two further reports with maps and diagrams for Falconbridge Limited, based on both historical and current geological information (Camier and Mclellan, 2000; Camier and Oosterman, 2001). The present evaluation is based largely on these reports, current and historical data, and the writers experience on the property. Both writers are knowledgeable about, and active in, the investigation of Proterozoic Fe-oxide Copper-Gold deposits in Canada.
Disclaimer
All statements regarding historical diamond drilling and associated assays cannot be independently verified, since the drill core has not been maintained in a useable condition. Also, historical surface assays have not been independently verified. However, drill logs with assay data are available for review.
3 Property Description and Location
The Island Copper property is located approximately 19 kilometres northeast of Sault Ste. Marie, Ontario, north of the cottage community of Island Lake (Figure 1). The property is situated northwest of the junction between Highway's 556 and 552, and straddles Highway 552. The Island Copper property is comprised of four Falconbridge claims, three YMCA patents and the Nystedt leasehold patents (Figure 2, Table 1). All claims were in good standing at the time of writing as indicated in Table 1.
The Falconbridge claims bound the patents held by the YMCA of Sault Ste. Marie on the north, west and southwest. The YMCA patents contain the main copper showings. Falconbridge currently has an option to earn a 100% interest in the YMCA patents as defined in the Falconbridge-YMCA option agreement (February 21, 2000). Falconbridge also has options on the Nystedt patents, which consist of two surface and mining leasehold patents owned by the Nystedt family of Sault Ste. Marie, Ontario. The Nystedt patents were optioned to Falconbridge Limited in August 2000. These claims are immediately south of the YMCA patents.
Accessibility, Infrastructure, Local Resources, Climate and Physiography
The Island Copper property is easily accessed by paved highway from Sault Ste. Marie (Figure 1). The property can be accessed by traveling north along the Trans-Canada Highway (#17) for ~ 15 kilometers to highway 556 at Heyden. Proceed northeast on 556 for ~ 5 kilometers to the junction of Highways 552 and 556, which is in the southeast corner of the property. The property straddles Highway 552 for approximately 3.5 kilometers NNW of the junction with Highway 556 (Figure 1). The cottage community of Island Lake is situated near the property at the junction of Highways 552 and 556, and along the northwest shore of Island Lake. Algoma Central Railway (ACR)
4
Figure 1: Location of the Island Copper Property north of Sault Ste. Marie, Ontario. Map orientation is north-south/east-west.
5
Figure 2: Island Copper property claim and patent map. Map orientation is north south/east-west.
6 Table 1: Claim status for the Island Copper property
Owner Claim Recording Date Due Date Claim Unit Standing Number Size Falconbridge Limited 1239731 September 1, 1999 September 1, 2002 8 Good Falconbridge Limited 1239732 September 1, 1999 September 1, 2002 3 Good Falconbridge Limited 1239733 September 1, 1999 December 9, 2002 8 Good Falconbridge Limited 1239734 September 1, 1999 September 1, 2002 4 Good Nystedt Family, Sault Leasehold N/A N/A 2 blocks Current St Marie Patent surface and mining rights
YMCA, Sault Freehold N/A N/A 3 blocks Current Ste Marie Patent surface and mining rights
7 passes on the southeast boundary of the property. A 5-car spur line is located off the gravel quarry on the eastern side of the property, and is leased from the YMCA by DCI Investments of Sault Ste. Marie. This quarry is located on the eastside of Highway 552 across from the main Cu-showing of the Island Copper property. The property is within easy access to major infrastructure, including air, rail, highways, power and port facilities at the city of Sault Ste Marie. Sault Ste. Marie is a major commercial and industrial city of ~ 100,000 inhabitants, located on the St. Marys River which connects Lake Superior and Lake Huron. Sault Ste. Marie serves a large portion of north-central Ontario, and is connected by international bridge directly to Sault Ste. Marie, U.S.
The climate and physiography of the property is typical of the Canadian Shield east of Lake Superior. The climate is northern temperate with warm summers and cold, snow-covered winters from approximately November through to Early April. Steep hilly terrain occupies the southern and central portions of the property, while the northern area drops steeply at first, then gently towards the Goulais River valley. The region is covered with a mixture of outcrop and overburden consisting of glacial sand and gravel in varying thickness that is covered by humus. Outcrop exposure averages <10% and occurs predominantly along rocky ridges, hilltops and cliff faces. Thin coverings of glacial overburden and humus occur along the flanks of rocky ridges and covers the small valleys between the ridges in the southern areas of the property. This increases to a relatively thick covering of glacial lacustrine-derived tills in the north towards the Goulais River valley where outcrop exposure is very minimal to non-existent. The area is overgrown with thick stands of maple alternating with cedar and spruce. Drainage along the northern portion of the property is towards the Goulais River and forms deep ravines with fast-flowing creeks. However, drainage is relatively poor in the central highland area of the property, and forms occasional swamps and beaver ponds between the hills with surface water available for diamond drilling.
8 History and Previous Work on the Island Copper Property
Copper mineralization was first discovered in the area over 90 years ago. Very little information about the early exploration history can be found, the exception being an historic adit on the property. The adit has since been backfilled and the length of the drift is unknown with only the top of the adit visible below a horizontal drill hole. The ground was reportedly explored during the 1950's with some diamond drilling. However, detailed assessment research conducted by Highland-Crow Resources Ltd., Falconbridge Limited and the authors could not find any records of this drilling. The Geological Survey of Canada and the Ontario Geological Survey carried out reconnaissance mapping in the region during 1964 and 1965, respectively. This work generated some interest in the potential of the area. A detailed summary of exploration of the area and property is listed in Table 2.
Prospecting in 1965 by Kennco Explorations (Canada) Ltd. near the adit led to the discovery of the hilltop showing. Kennco defined an area of chalcopyrite and hematite mineralization occurring in outcrop over an area of 650 metres by 400 metres. Geochemical analysis coupled with petrographic examinations revealed that host rock for the chalcopyrite and hematite was an albite-rich syenite (also referred to as albite granite in this report). They determined the syenite consisted of 65% albite, 15% orthoclase, and 15% quartz, with minor amounts of chlorite, apatite, pyrite and chalcopyrite. Kennco conducted geophysical surveys over the exposed mineralized zones, which included ground EM (induced electromagnetic chargeability), resistivity, and IP (induced polarization). Their geophysical survey delineated a horseshoe-shaped anomaly, which was coincident with the surface mineralization. Further work carried out by Kennco included geochemical assays for copper, geological mapping on a grid cut over the property, and digging and blasting of numerous trenches within mineralized zones. They culminated their exploration of the property with 2751.4 feet (838.6 meters) of diamond drilling in 18 drill holes (Figures 3, 4, 5 and 6). Significant results from the diamond drilling are listed in Table 3.
9 Year of Work Name of Company Work Carried Out Early prospecting led to the Pre 1960 Unknown, no records were drifting of an historic adit. found of the companies who Diamond drilling was reported previously worked the area. to have occurred one in the 1950’s., although no records have been recovered. Geological Survey of Canada; Regional reconnaissance and 1964 to 1965 Ontario Geological Survey mapping. Prospecting, Geological 1965 - 1966 Kennco Explorations (Canada) mapping, Geophysics, Ltd. Geological sampling and Geochemical assaying, Diamond Drilling (18 diamond drill holes; 2700 feet {822.96 m}) Prospecting and Diamond 1970 H. Nystedt Drilling (2 diamond drill holes; 503 feet {153.31 m}) Diamond Drilling 970 - 1971 Copperville Mining Corp. (10 diamond drill holes; 3,558.6 feet {1084.66 m}) Geological mapping, 981 – 1982 Highland-Crow Resources Geochemical sampling, line Ltd. cutting, Geophysical airborne survey, 2000 – 2001 Falconbridge Limited I.P. survey (Fraser Filtered Chargeability), and Residual Gravity survey, Geological mapping, Geochemical sampling, line cutting
Table 2. Summary of historical work carried out on the Island Copper property and area.
10 Table 3. Kennco Exploration and Copperville Mining Corporation significant assay results returned from diamond drill intersections.
Company Diamond From: To: Intersection: Cu (%) Au Name Drill Hole metres metres metres (g/tonne)
Kennco KO-65-01 2.135 13.25 11.59 3.4 0.9 Exploration
KO-65-02 1.52 6.40 4.88 0.85 trace
KO-65-04 2.44 15.86 13.42 0.48
H. Nystedt 2 diamond N/A Total N/A N/A N/A drill holes 153.31
Copperville No Au Mining Cpp-70-01 14.00 18.30 4.30 3.01 assays were Corporation recorded
Cpp-70-03 42.70 46.79 4.09 1.14
Cpp-70-04 19.83 21.35 1.53 0.63
36.60 42.70 6.10 1.70
Cpp-70-05 22.72 24.16 1.43 0.88
Cpp-70-06 6.10 6.86 0.76 1.14
15.25 31.23 15.98 0.83 35.84 36.60 0.76 0.75 86.93 88.02 1.10 0.75 96.69 102.79 6.10 1.04
Cpp-71-09 38.13 42.70 4.58 1.08
54.29 54.90 0.61 1.71
Cpp-71-10 44.23 48.80 4.58 0.70
57.95 61.00 3.05 0.95
11
Figure 3: Historical drill hole location map. Map orientation is north-south/east-west.
12
Figure 4: Historical drill hole location map.
13
Figure 5: Historical drill hole location map.
14
Figure 6: Historical drill hole location map.
15
No further interest in the property occurred until 1970, when prospector H. Nystedt drilled two holes totaling 503 feet (153.3 meters) southwest of the hilltop showings. This sparked some interest by Copperville Mining Corp. who optioned the property in 1970 and 1971. They carried out a ten-hole drilling program in 1971 totaling 3,558.6 feet (1084.7 metres). Their drill program tested the property to greater depths than Kennco, with the deepest hole extending to 167 metres in length and ending in brecciated granite and chloritized mafic rock. The significant results of the diamond drilling are listed in Table 3.
Highland-Crow Resources conducting a regional reconnaissance program during the 1980 to 1981 field seasons, and concluded that the area warranted further investigation. They optioned the property from the YMCA of Sault Ste Marie and Mr. Nystedt in 1981. Their first phase of exploration included field mapping over the property to establish geological limits to the alteration, mineralization and extents of brecciation. Their results determined that the target area lay entirely within the YMCA and Nystedt optioned-property and a detailed program of geological mapping and geochemical sampling was undertaken. A proposal for their 1983 exploration program of the property included at least three diamond drill holes, trenching and further geochemical sampling (Highland-Crow, 1983). However, no further information was found in the assessment files and it is doubtful as to whether this work was completed.
As part of a regional prospecting project, prospector F. Racicot collected four grab samples from the main mineralized zone of the property. His samples averaged greater than 1% Cu and contained between 24 and 373 ppb Au. Other companies that have worked in the region include Tri-Bridge (663.7 meters of drilling on or near the property), Delta Minerals, and Colleen Copper. At least 39 holes have been drilled to date on or adjacent to the property, for an approximate total of 2740.3 meters (Figures 3, 4, 5 and 6).
The most recent work on the property has been carried out by Falconbridge Limited (Timmins, Ontario regional exploration office). During a regional exploration program undertaken by Falconbridge the property was visited with the Ontario Geological Survey regional field geologist from Sault Ste. Marie. They determined the area required investigation and optioned the property from the YMCA in February of 2000. Falconbridge staked additional ground around the patent claims, and conducted a detailed airborne Heli-mag
16 survey in early 2000. A grid line was cut over the property in the spring of 2000, followed by geological mapping (Figure 7) and rock geochemical sampling during the 2000 summer field season. Falconbridge then optioned the Nystedt surface and mining leasehold patents in August of 2000 from the Nystedt family of Sault Ste Marie. A ground gravity survey was conducted over the properties in late fall of 2000 (Figure 8). During the 2001 field season a grid line extension was cut over the Nystedt property followed by geological mapping, rock sampling for geochemistry and assay, and a Fraser Filtered IP chargeability survey (Figure 9). Falconbridge subsequently decided to joint venture the properties to any parties interested in advancing the exploration.
In addition to work by private companies, regional aeromagnetic survey maps are available from the Geological Survey of Canada (Figure 10) and the Ontario Geological Survey (Figure 11).
Geological Setting
The Island Copper property lies immediately northwest of the Archean-Proterozoic boundary, in moderately to strongly foliated Archean granitoid gneisses of the Gros Cap Batholith (Figure 12). The Archean- Proterozoic boundary is delineated by the Proterozoic Highway Fault Zone (Figure 7) that parallels Highway 556 and the ACR railway line. This boundary separates Proterozoic aged clastic rocks of the Aweres
17
Figure 7: Geology of the Island Copper Property.
18
Figure 8: Residual Gravity Map. Data from Falconbridge Limited.
19
Figure 9: Fraser Filtered Chargeability Map. Data from Falconbridge Limited.
20
Figure 10: Residual Total Field Regional Aeromagnetic Data. Geological Survey of Canada data. 21
Figure 11: Aeromagnetic Data and Mineral Occurrences. Ontario Department of Mines and the Ontario Geological Survey data
22 Formation to the southeast from the Archean gneiss. To the north and northwest of the property, Huronian sedimentary and volcanic rocks overlie the Archean.
The Gros Cap Batholith forms the majority of the outcrop exposures on the property. These rocks are comprised of gneissic granite, granodiorite and amphibolite that have been strongly to moderately foliated, and contain localized migmatitic units. The rocks are typically buff to white- brown in colour on weathered surfaces with localized zones of white migmatite visible in outcrop along cliff faces in the northern part of the property. On fresh surface, the gneiss is light gray to pink with black blebs or occasional banding of mafic minerals. The gneiss is typically comprised of plagioclase, potassium feldspar, quartz, and biotite ± hornblende. At several locations, the gneiss appears intensely altered and contains units of east-west trending chloritized-amphibole schist. This schist may reflect intense shear zones related to faulting within the gneiss.
The gneiss has been intruded by numerous gabbroic to fine-grained diabase dikes of at least three different ages, all of which exhibit variably strong to weak magnetism. The larger dikes trend in a west-northwest direction and exhibit gabbroic textures with moderate magnetism and are occasionally weakly chloritized. The finer grained diabase dikes trend in a northwest direction and are generally strongly magnetic. Several, strongly magnetic, southeast trending and north-south trending possible biotite-lamprophyre dikes, comprised almost wholly of biotite and other mafic minerals were also observed. They are the youngest mafic intrusive units identified.
The Gros Cap gneiss is locally brecciated in the eastern area of the property adjacent to the north-northwest trending Island Lake fault, and extensively brecciated in the southeastern portion of the property. The breccia is characterized by subangular to rounded, occasionally stretched fragments, which exhibit trains of comminuted material. The fragments are set in a matrix of occasionally silicified, chloritized-amphibole that contains small-comminuted fragments of gneiss. The fragments are easily identified due
23
Figure 12: Regional Geology of the Sault Ste. Marie area. Map orientation is north-south/east- west. 24 to preferential weathering of mafic minerals within the matrix, and occasionally by a mineral foliation. Apparently, secondary tectonic overprinting of the original foliation did not occur. Quartz veins of varying widths occasionally form anastomosing stockworks that crosscut and silicify the breccia. On occasion, associated with the quartz veins are parallel trending veins (<1cm width) of specular hematite that crosscut the quartz veins or occur as a selvage along fracture walls.
Within brecciated zones of Gros Cap gneiss, are localized albite-rich granite breccia bodies that appear intrusive in nature and have sharp contacts. The pink coloured, albite-rich granite is comprised of 80-85% albite crystals intermixed with potassium feldspar and quartz. This unit contains the bulk of the Fe-oxide and copper mineralization. The unit displays a crackle or shatter brecciation with disseminated and anastomosing veins and veinlets of specular hematite, chlorite, chalcopyrite and pyrite forming the matrix. Several outcrops display a sharp visible irregular contact between the Gros Cap breccia and the albite-rich granite breccias indicating they are separate distinct units (Figure 13). Within the Island Copper property the Gros Cap Gneiss appears to form a cap-rock over the albite granite, although the copper mineral veining within the albite granite was not observed to continue into the Gros Cap breccia. Occasional veins and veinlets of specular hematite intrude into the Gros Cap breccia, and are accompanied by quartz veining.
Although the Gros Cap Gneiss is Archean, the albite granite intrusions have not been radiometrically dated. Some investigators believe that the albite granite (and mineralization) may be Proterozoic (possibly Keewanawan), however, their age remains undetermined.
Structurally the area is quite complex with intense faulting. The Highway Fault Zone (southern boundary of the property) has been interpreted to represent the Archean-Proterozoic boundary thrust fault along the northern margin of the Lake Huron Graben
25
Figure 13: Photograph of the trench at the main copper showing.
26 Structure. The north-northwest trending Island Lake Fault crosscuts the gneiss on the eastern side of the property and is visible in outcrop along Highway 552. The Island Lake fault appears to be truncated and offset by the Highway Fault. A further series of faults running sub-parallel to the Island Lake fault cut across the property northwest of the Highway Fault. The brecciated gneiss and albite-granite breccia appear to be closely associated with these faults, and display cataclastic brecciation in this zone of structural weakness at the intersections of NE and NNW trending faults .
Geology and Mineralization of the Island Copper Property
Massive Gros Cap gneiss underlies the western portion of the property (Figure 7). It consists of light gray to pink granite and granodiorite, comprised of plagioclase, quartz, and biotite ± hornblende and displays a strong to moderate mineral foliation. Localized zones of migmatite occur in the Gros Cap gneiss, which consists of alternating wispy bands of mafic minerals set in quartz-feldspar matrix. In one location northwest of the brecciated gneiss, the gneiss is distinctly albitized. The gneiss outcrops in the western part of the grid in Falconbridge claims #1239733 and #1239734, and is the predominant rock type in claim #1239731. The Gros Cap gneiss covers an extensive area on both sides of Highway 552, and appears to be locally brecciated adjacent to the north- northwest trending Island Lake fault. The breccia is characterized by subangular to rounded and occasionally stretched fragments. They are associated with trains of comminuted material in a matrix of chloritized-amphibole that is occasionally silicified and contains small comminuted fragments of gneiss. The fragments appear to have undergone some transport or movement as evidenced by the degree of mixing of the fragments and faint imbrications or flow fabric within the matrix. Fragments are easily identified due to preferential weathering of mafic minerals within the matrix, and occasionally by a preserved mineral foliation. This is particularly evident for fragments in strongly chloritized-amphibole schist that is often found in conjunction with the breccia. Silicification is apparent and often overprints the matrix or forms anastomosing to fragmental quartz veinlets within the matrix and between the fragments. The fragments are
27 occasionally hematized. Late fractures within the breccia exhibit weathering comprised of limonite-goethite occasionally mixed with calcite and siderite.
The Gros Cap Gneiss is crosscut by numerous variably magnetic, mafic intrusions that generally trend in a northwest direction. They consist of are comprised of narrow, generally less than 5 metres wide, highly magnetic diabase dykes, and >40 meter wide weakly magnetic, gabbroic-textured mafic dykes.
Outcrops on the eastern side of the property are comprised of brecciated Gros Cap gneiss alternating with unbrecciated gneiss. The outcrops often contain numerous crosscutting quartz veins from 1 to 15 centimeters wide, which occasionally contain hematite and/or sulphide mineralization. Some of these outcrops have veins up to several meters wide of siliceous mafic material, which appears to be silicified chlorite-amphibole. These veins trend in a northeast direction parallel to the Highway Fault, and locally brecciate the gneiss. This is best observed on fresh exposures within the gravel pit quarry located south of L90+00N.
Brecciated gneiss fragments occur within intensely altered chlorite-amphibole schist as rounded to angular clasts that occasionally exhibit rotational textures. Within the schist, comminuted material is observable with the unaided eye. Hand lens examination shows that clasts are intensely comminuted, fractured, altered and supported in the chlorite-amphibole matrix. It is apparent that the schist is the result of intense brecciation and alteration of the gneiss. Angular fragments of unaltered to partially altered gneiss also occur within the schist, as observed in outcrop and on cliff faces. In several locations, specular hematite veins cut into the brecciated gneiss along quartz-filled fractures. However, no sulfide mineralization could be found within the brecciated Gros Cap gneiss.
28 Sediments of the Aweres Formation finger into and overlie the brecciated gneiss along fault contacts in the southeast portion of the property, and are visible in outcrop along the rail line. The sediments are comprised of arenite, siltstone, sandstone and occasional conglomerate in a rusty brown fine- to medium-grained matrix.
The Island Lake Fault zone cuts the gneiss breccia at high angle dipping steeply to the northeast, and is best observed in outcrop along both sides of Highway 552, between L88+00N and L90+00N. These outcrops are predominantly comprised of chlorite- amphibole schist containing numerous angular fragments of Gros Cap gneiss. The schist contains a strong lineation that generally strikes northwest. However, slickensides have been observed with variable orientations. The Island Lake Fault appears to have been active over a long period of time, but is truncated by the Highway Fault Zone. Numerous additional parallel to sub-parallel faults also strike NW from the Highway Fault Zone on both sides of the Island Lake Fault.
Large quartz veins crosscut the gneiss, forming anastomosing veins and stockworks. Some of these quartz veins are not continuous, but appear to have been fractured and dislocated. Occasional specular hematite veins up to 2 centimeters in width are often observed parallel to, invading, or occasionally cross-cut quartz veins. On the eastern side of Highway 552, the quartz veins appear sub-parallel the Island Lake Fault and trend in a north-northeast direction. These veins are larger than on the western side, and carry specular hematite with occasional chalcopyrite mineralization.
Pink albite-rich granite intrudes the brecciated gneiss in several locations. In surface hand-samples it is comprised of 80-85% pink to pinkish white albite crystals intermixed with K-feldspar and minor quartz. The unit has undergone crackle or shatter brecciation with specular hematite +/- sulfides forming the matrix. The contact between the albite granite and brecciated gneiss is sharp with a narrow chill margin grading into the albite granite (Figures 13 and 14).
29
Figure 14a and 14b: Photographs of the geological contact between the Gros Cap gneiss breccia and mineralized albite granite breccia.
30 The albite granite comprises a large portion of the cliff face where an historical adit is located, and contains very good exposures of chalcopyrite veining and malachite stains. Above the adit, the brecciated gneiss appears to be draped over and down the flanks of the cliff, limiting further exposures of albite granite to small windows at several locations. Towards the top of the hill on L89+00N, several historical trenches expose mineralized albite granite and its contact with the Gros Cap Gneiss. The main chalcopyrite showing is located at the top of the hill on L89+00N at 100+00E (Figure 13).
The predominant mineralization observed on the property consists of hematite, chalcopyrite and pyrite within the albite granite breccia between L88+00N and L91+00N on L100+00E. However, another outcrop east of the highway along L92+00N was trenched along a cliff face and exposes further chalcopyrite veining within the albite granite. This exposure shows albite granite interfingered with brecciated gneiss and is the only mineralized zone found on the eastern side of the property to date. This mineralization may have been faulted and juxtaposed against un-brecciated gneiss.
Detailed petrographic analysis of three samples of the mineralized albite granite breccia were carried out by Camier and Mumin (2000), and are included in Appendix 1, along with photos and photomicrographs of the samples.
Deposit Types
The Island Copper mineralization occurs in an albite-rich granite breccia that intrudes and is capped by the Gros Cap Gneiss. The mineralized intrusion is situated at the intersection of major crustal faults, the Highway Fault Zone and the Island Lake Fault. The mineralized intrusion is at the terrain boundary between Archean and Proterozoic rocks, along the margins of a major paleo-rift setting. Copper and gold enrichments occur in chalcopyrite and pyrite within a hydrothermal Fe-oxide (hematite) chlorite and
31 amphibole matrix that cements fragmented and altered granite breccia. The mineralized breccias are regionally associated with barren to weakly mineralized quartz-vein stockworks and chlorite-amphibole schists. These characteristics of the Island Copper mineralization are presently thought to most closely resemble hydrothermal Fe-oxide copper-gold deposits (IOCG). Consequently, this deposit type should be carefully considered when exploring the Island Copper property.
The best current reference for hydrothermal Fe-oxide copper-gold deposits is the Australian Minerals Foundation publication “Hydrothermal Iron Oxide Copper-Gold and Related Deposits: A Global Perspective”, 2000, edited by T. M. Porter (ISBN 0-908039- 76-X). This volume contains 25 papers with numerous authors, covering all aspects of this deposit type, including several overviews and numerous studies of specific deposits from around the globe. We refer interested readers to this volume for detailed information on this deposit type.
The location of the Island Copper property adjacent to the 1.1 Ga mid-continent rift, which runs through Lake Superior and along the eastern shoreline of the lake, is a very good setting for the exploration of IOCG deposits. The rift formed an extensional environment that thinned the crust and allowed the generation and eruption of mafic volcanic and intrusive rocks. Thinning of the crust also facilitated the generation of intermediate to felsic melts derived from basement continental rocks. These potentially volatile-rich melts could have ascended along deep structural fractures initiated by the extensional tectonics. Emplacement at higher structural levels, and exsolution of volatiles could have generated IOCG type deposits and the mineralization at Island Copper.
32 Mineralization
Near surface mineralization on the Island Copper property consists of Fe-oxide (hematite ± magnetite), pyrite and chalcopyrite occurring between trace (£0.1%) and 6 wt % chalcopyrite, with surface weathering to malachite and azurite. The hematite and sulphides occur as intergranular fillings, disseminations and anastomosing veins and veinlets of chalcopyrite and pyrite along with hematite ± magnetite (Camier and Mumin, 2000; Appendix 1). The mineralization plus chlorite and amphibole form the matrix of a crackle and/or shatter breccia in the albite-rich granite. Copper mineralization does not extend into the overlying Gros Cap gneiss, except for the presence of occasional vein-type specular hematite associated with crosscutting quartz veins in the brecciated zones.
Recently collected surface grab samples taken by Falconbridge for whole rock geochemistry and metal assays indicate Cu at up to 0.5 wt%, with occasional gold values up to a maximum of 2 g/tonne, and silver up to 4.2 g/tonne (Appendix 2, geochemistry only). Falconbridge did not resample the known historical trenches from the main copper showings. Historical grab samples collected by prospector F. Racicot from the main mineralized zone of the property reportedly averaged greater than 1 wt% Cu, and contained between 24 and 373 ppb Au. The report by W. H. Thompson for Kennco Explorations (Canada) Limited, December 1966, indicates surface trench assays of up to 2.93 wt% Cu over significant widths (widths not indicated in the material provided to the writers). Assay results from historical drilling also indicate some good values, with copper grades of up to 4.02 Wt% Cu over 9.45 meters reported for hole KO-65-01. Assaying for gold in the historical drilling was apparently not carried out for most of the drill holes. Additional significant assay results from the historical drilling are listed in Table 3. Historical surface and drill hole assays have not been independently verfied (re-sampled) by the writers.
Other mineralization historically reported from the Island Copper property comes from Highland-Crow. Their sampling indicated several quartz veins on the eastern side of the property with elevated Zn and Pb values. Surface samples taken by Falconbridge were
33 not able to reproduce these results, however, it is unlikely that Falconbridge sampled the same material. Several other copper showings have been reported in the vicinity of the Island Copper, and one radioactive occurrence is reported about 1 km south of the property (Figure 11).
Exploration of the Island Copper Property
Falconbridge Limited has been the latest company to work on the Island Copper property. During a regional exploration program undertaken by Falconbridge in 1999, the Island Copper property was visited with the regional field geologist from the Sault Ste. Marie office of the Ministry of Northern Development and Mines, Ontario. Falconbridge determined the area required further investigation and optioned the property from the YMCA in February of 2000. Falconbridge then staked additional ground around the patents. This work was followed by a detailed airborne Heli-mag survey, flown in the spring of 2000. A 42 line-kilometer grid line was cut over the property in the late spring of 2000, followed by geological mapping and rock geochemical sampling during the 2000 summer field season. The grid lines were cut at a 100 meter spacing over the mineralized showings in the central portion of the claims, and 200 or 400 meter spacing elsewhere. Falconbridge then optioned the Nystedt surface and mining leasehold patents located south of the YMCA patents in August of 2000 from the Nystedt family of Sault Ste Marie. A ground gravity survey was conducted over the Falconbridge and YMCA properties in the fall of 2000. During the 2001 field season a 3.8 line-kilometer grid extension was cut over the Nystedt patents followed by geological mapping, rock sampling for geochemistry and assays, a Fraser Filtered IP chargeability survey and a gravity survey. Falconbridge subsequently decided to joint venture the properties to any parties interested in advancing the exploration of the ground. At the time of writing, no further work had been carried out on the property.
34 Geophysics
Regional aeromagnetic data are available from both the Geological Survey of Canada (GSC) and the Ontario Geological Survey (OGS) (Figures 10 and 11, respectively). The Island Copper Property occurs within the intersection of broad, relatively low and poorly defined regional trends of magnetic highs. A NNW trend of moderated magnetic highs stretches from Echo Bay, east of Sault Ste. Marie to west of Mamainse Point on Lake Superior. A second broad ENE trend of moderate magnetic highs intersects the NNW trend in the region of the Island Copper property (Figure 10). An ovoid point-source magnetic anomaly of ~ 500 gammas is centered ~ 3 km NE of the property (Figure 11). A minor ovoid 50 gamma anomaly is located in the SW portion of the property.
Several geophysical surveys were carried out over the property on behalf of Falconbridge, including detailed heli-mag, ground gravity and induced polarization. The gravity and induced polarization surveys resulted in a significant coincident anomaly. A linear gravity high anomaly of up to ~ 1 mGal extends east-west across the property and is coincident with the mineralized showing on the east side of the property (Figure 8). The induced polarization survey indicates a broad zone of high chargeability (up to ~ 10mV/V) that is partly coincident with the gravity high (Figure 9).
These anomalies are coincident with a weak regional gravity high that occurs to the WSW of the property and extends as far as Whitefish Bay, Lake Superior. This regional gravity high also appears coincident with a weak aeromagnetic anomaly that also extends WSW from the property.
The east-west gravity and chargeability highs within the Island Copper property indicate the possibility buried mineralization along this trend.
35 Drilling on the Island Copper Property
The only diamond drilling information available for examination (drill logs only) was conducted approximately 30 to 37 years ago. Falconbridge Limited reviewed the historic assessment files and determined that at least 39 diamond drill holes have been drilled on or adjacent to the property for an approximate total of 2,740.3.meters. A list of known drill holes is given in Table 4. The diamond drill core is not available for viewing because it was not stored satisfactorily. It can be found scattered under the leaf litter near old drill sites. Other debris from diamond drilling activity is occasionally found, such as old drill rods, rotted pieces of core boxes and rusted oil cans. A number of the old drill hole collars are still visible at surface (e.g. Figure 13). Historical drill logs for 18 Kennco, 10 Copperville and 2 Nystedt holes were reviewed by the authors at the time of writing. They are in acceptable condition with assay results reported for all but the two Nystedt holes.
Kennco Explorations (Canada) Limited conducted the most aggressive drill program on the property, drilling 18 diamond drill holes for a total of approximately 838.6 meters (Table 4). Their activity focused primarily around the showing, however, they did not test the anomaly to any great depth. Copperville Mining Corporation conducted a 10- hole diamond drill program for an approximate total of 1084.7 meters testing the ground to a maximum vertical depth of ~137 meters in drill hole CPP-70-7. Tri-Bridge Mines Ltd. drilled 9 diamond drill holes for an approximate total of 663.7 meters on and adjacent to the property. Not listed in Table 4 is the historic drilling conducted prior to 1965, and the 2 diamond drill holes which H. Nystedt completed (~153.3 meters).
36 Table 4: Summary of Historical Drilling. Hole No. Easting Northing Elevation (M) Date Azimith Dip Depth Drilled by KO-65-01 708494.5 5172445.68 121.0 05/12/1965 0 90 61.89 Kennco Explorations (Canada) Limited KO-65-02 708494.43 5172467.68 122.0 08/12/1965 37 45 93.6 Kennco Explorations (Canada) Limited KO-65-03 708515.11 5172517.28 120.0 10/12/1965 127 45 63.41 Kennco Explorations (Canada) Limited KO-65-04 708475.11 5172463.06 122.0 13/12/1965 37 45 46.34 Kennco Explorations (Canada) Limited KO-65-05 708402.16 5172479.88 118.0 14/12/1965 92 45 55.79 Kennco Explorations (Canada) Limited KO-66-06A 708521.59 5172422.94 120.0 09/10/1966 0 90 23.57 Kennco Explorations (Canada) Limited KO-66-06B 708526.59 5172422.9 120.0 10/10/1966 0 90 23.17 Kennco Explorations (Canada) Limited KO-66-06C 708524.17 5172421.69 120.0 11/10/1966 0 90 44.82 Kennco Explorations (Canada) Limited KO-66-07 708582.61 5172529.61 113.0 13/10/1966 0 90 38.87 Kennco Explorations (Canada) Limited KO-66-08 708543.16 5172612.02 108.0 14/10/1966 0 90 45.73 Kennco Explorations (Canada) Limited KO-66-09 708509.84 5172709.76 103.0 16/10/1966 0 45 53.66 Kennco Explorations (Canada) Limited KO-66-10 708613.01 5172452.25 113.0 19/10/1966 0 90 50.3 Kennco Explorations (Canada) Limited KO-66-11 708722.8 5172446.15 96.0 22/10/1966 0 90 41.77 Kennco Explorations (Canada) Limited KO-66-12 708732.84 5172459.07 96.0 23/10/1966 228 45 69.39 Kennco Explorations (Canada) Limited KO-66-13 708674.51 5172722.69 96.0 25/10/1966 0 90 28.05 Kennco Explorations (Canada) Limited KO-66-14 708745.46 5172756.85 107.0 27/10/1966 75 45 18.29 Kennco Explorations (Canada) Limited KO-66-15 708691.92 5172754.88 98.0 75 45 22.26 Kennco Explorations (Canada) Limited KO-66-16 708660.28 5172737.77 94.0 70 45 62.5 Kennco Explorations (Canada) Limited CPP-70-1 708488.71 5172402 123.0 25/09/1970 0 45 76.22 Copperville Mining Corporation CPP-70-2 708487.4 5172399.96 123.0 03/10/1970 0 65 77.13 Copperville Mining Corporation CPP-70-3 708574.59 5172551.26 112.0 07/10/1970 280 45 121.95 Copperville Mining Corporation CPP-70-4 708573.7 5172437.65 118.0 14/10/1970 280 45 92.07 Copperville Mining Corporation CPP-70-5 708655.37 5172436.24 106.0 19/10/1970 260 45 91.46 Copperville Mining Corporation CPP-70-6 708775.98 5172473.68 96.0 02/11/1970 280 90 152.44 Copperville Mining Corporation CPP-70-7 708777.58 5172471.85 96.0 14/12/1970 280 55 167.26 Copperville Mining Corporation CPP-71-8 708774.82 5172472.08 96.0 06/01/1971 280 65 152.44 Copperville Mining Corporation CPP-71-9 708617.58 5172581.23 101.0 20/01/1971 255 45 92.99 Copperville Mining Corporation CPP-71-10 708633.64 5172526.59 104.0 28/01/1971 255 45 60.98 Copperville Mining Corporation TBG-71-1 707402.97 5171360.41 114.0 270 45 91.46 Tri-Bridge Mines Ltd. TBG-71-3 707658.04 5171277.3 103.0 270 45 69.21 Tri-Bridge Mines Ltd. TBG-71-4 707779.23 5171365.8 101.0 270 45 77.44 Tri-Bridge Mines Ltd. TBG-71-5 707708.82 5171919.7 106.0 270 0 60.98 Tri-Bridge Mines Ltd. TBG-71-5A 707753.53 5171917.79 106.0 270 45 90.85 Tri-Bridge Mines Ltd. TBG-71-6 707765.28 5171808.17 108.0 270 45 60.98 Tri-Bridge Mines Ltd. TBG-71-7 708046.24 5171606.84 114.0 270 45 91.46 Tri-Bridge Mines Ltd. TBG-71-8 707765.48 5171702.28 106.0 270 45 60.06 Tri-Bridge Mines Ltd. TBG-71-9 707880.09 5171450.15 104.0 270 45 61.28 Tri-Bridge Mines Ltd.
37 Sampling Method and Approach
Falconbridge Limited collected approximately 45 surface grab samples during geological mapping of the property. Twenty-two samples were submitted for whole rock analysis. The results of the whole-rock geochemistry are discussed in the chapter on geology. All samples were acquired from outcrop so that only unweathered material was collected.
Surface grab samples that were collected for metal assay were unweathered material selected to represent a visually fair distribution of sulphides within the rock. These samples were collected from surface exposures of the albite-rich granite at various locations along the gridlines. The results are discussed in the section on mineralization.
Sample Preparation, Analyses and Security
To the knowledge of the writers, the whole rock geochemistry and assaying conducted by Falconbridge was carried out according to normal industry standards and are acceptable for the opinions presented in this report. The samples were analyzed at Swastika Laboratory, Timmins, Ontario, under the directions set by Falconbridge Limited.
Data Verification
The assay results discussed in this report are based primarily on historical drilling and assaying records. The quality of this work cannot be independently verified because the drill core is not in useable condition, and exact locations of surface samples is not clear. Only the drill logs and reports along with reported assays are available for inspection. J. Camier (co-author), was contract geologist for Falconbridge Limited, and was an active member of the team that collected and researched the historical data on the Island Copper
38 property. Mr. Camier was also the senior field geologist in charge of mapping and sampling the Island Copper property for Falconbridge in both the 2000 and 2001 field seasons. He was co-author of two reports for Falconbridge, which are used in the present report. Mr. Camier verifies that he collected, packed and shipped the recent surface samples collected for Falconbridge, to Falconbridge, and that Falconbridge subsequently forwarded them to Swastika Laboratories for analysis.
Mineral Resource and Reserve Estimates
It is not possible to carry out a verifiable resource estimate using the historical data. Additional and verifiable diamond drilling and surface trench assaying is required before any reliable estimates can be calculated.
Other Relevant Data
No other relevant data was available to the authors at the time of writing. However, supplementary information is believed to be available from Falconbridge, the historical records and academic literature.
Interpretation and Conclusions
It is apparent from the historical and current work that a significant amount of felsic-intrusion-hosted Fe-oxide, copper +/- gold mineralization is present on the Island Copper property. Most of the mineralization occurs in an albite-rich granite breccia that intrudes the Gros Cap Gneiss, as illustrated in the schematic model shown in Figure 15. The mineralization is concentrated at and near the contact with the gneiss, in a region of extensive faulting and brecciation. The copper mineralization does not appear to extend into the gneiss.
39 It is the opinion of the authors that this mineralization is most similar to the class of deposits referred to as Proterozoic Fe-oxide Copper-Gold deposits, for reasons already discussed in the section Deposit Models. Consequently, this deposit type should be carefully researched and considered in any further exploration of the property.
Exploration carried out to date has located pods and zones of copper mineralization ranging from low to significant grades, however, this work has not conclusively determined the mineral potential of the property. Diamond drilling is relatively shallow, reaching a maximum vertical depth of about 137 meters, and is concentrated in the east- central and south-east portions of the property. The coincident gravity and chargeability anomalies that extend in an east-west direction across the property have not been tested west of the main showing.
40
Figure 15: Schematic geological model for the Island Lake copper mineralization.
41 Recommendations
It is recommended that this property be further explored in the light of recent advances in the understanding of Fe-oxide copper-gold type deposits. The historical diamond drilling and surface data should be replotted and evaluated for: 1) any trends in copper grades, 2) variations in intensity and type of alteration mineralogy, 3) variations in the style and intensity of brecciation, and 4) the association of major and subordinate structures with brecciation, hydrothermal alteration and mineralization. These evaluations combined with a general and thorough overall property evaluation, including the current geology and geophysics should be carried out prior to any decision regarding how much and where further diamond drilling is conducted.
It is also recommended that the assay techniques be tested by several methods on splits of the same sample, to determine if the historical information has accurately reported the metals presence. This should include aqua regia digestion versus multi acid (near total digestion), and the comparison of these results with neutron activation analysis. In some Fe-rich deposits, it has been demonstrated that a significant portion of the gold may not be reported due to analytical interference.
42 References
Camier, J. and Mclellan, D., 2000. Island Copper Project Report, Island Copper PN 297. Technical report for Falconbridge Limited.
Camier, J. and Mumin, A.H., 2000. Petrographic Report of Selected Rock Samples from Riley Township, Island Copper Property, and Copper Corp. Minesite. Petrographic report for Falconbridge Limited.
Camier, J. and Oosterman, D., 2001. Island Copper Project – Nystedt Extension Report, August, 2001, Addendum to Island Copper Project 2000 Report, Island Copper PN 297. Technical report for Falconbridge Limited.
Douglas, J.H., 1971. Colleen Option, Aweres Township, Sault Ste. Marie Mining Division, District of Algoma. Supplementary report to the Directors, Copperville Mining Corporation.
Geological Survey of Canada, Regional Aeromagnetic Data – Sault Ste. Marie Area, Residual Total Field – Source: GSC Map NL-16-17-M.
Innes, D.G. and Associates Ltd., 1983. Island Lake Property Geological Report. Technical report for Highland Crow Resources Ltd.
Ontario Department of Mines, Aeromagnetic Data, ODM Map 2200G.
Ontario Geological Survey, Occurrences, OGS Aweres GDIF 28.
Ontario Geological Survey, Map 2419: Sault Ste. Marie- Elliot Lake, Ontario.
McDonald, D.A., 1970. Report on Colleen Copper Property, Township of Aweres, Sault Ste. Marie Mining Division, District of Algoma.
43
Porter, T.M., 2000, (editor). Hydrothermal Iron Oxide Copper-Gold and Related Deposits: A Global Perspective. Australian Minerals Foundation, 349 p.
Sutcliffe, R.H., 1991. Proterozoic geology of the Lake Superior area. In Geology of Ontario, Ontario Geological Survey, Special Volume 4, Part 1, pp.627-658.
Thompson, Jas. E., 1954. Geology of the Mamainse Point Copper Area. 62 Annual Report, Ontario Department of Mines, Vol. LXII, Part 4.
Thompson, W.H., 1966. Report on Diamond Drilling, Nystedt Property. Technical report for Kennco Explorations (Canada) Limited.
44 45 46 APPENDIX 1
Petrographic Report for Selected Samples from the Island Copper Property
47 Petrographic Report of selected samples from the Island Copper property.
The following petrographic report describes hand samples IC-1, IC-2, and IC-3. The samples were collected by Mike Collison during the 1999 summer field season from the Island Copper property, owned by the Young Men's Christian Association of Sault Saint Marie, and optioned to Falconbridge Exploration, Timmins. The Island Copper property is located in Aweres Township, Sault Saint Marie Mining District. Polished thin sections were made from the hand samples and examined using a Nikon Labphot-2, in both transmitted and reflected light. Detailed petrographic reports are included in the attached appendix.
The hand samples consist of pale orangey-pink, hematite-stained, fractured and brecciated quartz-feldspar porphyry. Breccia matrix consists of medium gray, non- magnetic specular hematite in IC-2 and IC-3, and chalcopyrite ± hematite in IC-1. The specular hematite and chalcopyrite form intergrowths of anastomosing veins that infill fractures in the porphyry (Photo-plates 1, 2, and 3). Chalcopyrite forms anhedral grains and aggregates within the hematite of IC-2 and IC-3, and often rims breccia fragments. Chalcopyrite also occurs as abundant anastomosing veins and veinlets within the porphyry independent of hematite (IC-1). Epidote alteration in the porphyry is evident as pale-pistachio green colouration interstitial to the groundmass. Minor secondary weathering occurs as an earthy-red colouration on old and fresh fracture surfaces, and as anhedral tan coloured minerals adjacent to fracture walls within the porphyry.
Microscopic examination of the polished thin sections revealed the host rock to be quartz- feldspar porphyry in various stages of cataclastic brecciation and alteration. The dominant matrix mineral is specular hematite, formed in part from the alteration of magnetite, which occurs as irregular shaped inclusions within hematite blades (IC-2 and IC-3). Chalcopyrite also occurs in the matrix forming anhedral to irregular shaped grains interstitial to the gangue minerals and the Fe-oxides, and is the dominant matrix mineral in IC-1. Goethite- limonite alteration rims some hematite and chalcopyrite, and is interstitial to the gangue minerals. It is occasionally observed crosscutting chalcopyrite and forms anastomosing veins. There are minor inclusions of anhedral hematite in some chalcopyrite grains. No secondary Cu-alteration minerals where observed in any of the sections. A brief summary of each polished thin section follows.
48 Examination of IC-1 revealed inequigranular, corroded, cataclastic textured, anhedral to subhedral, sericite-altered plagioclase exhibiting strong albite twins. The plagioclase is intermixed with anhedral sericitized K-feldspar, quartz, apatite, and minor sericite, goethite, and epidote. Quartz forms anhedral, inequigranular, interstitial grains and intergranular aggregates between the feldspars. Apatite is unusually abundant and occurs as subhedral to euhedral prismatic or columnar grains that are predominantly inclusions associated with quartz. Goethite-limonite occurs along fractures from late secondary weathering, and rims chalcopyrite and Fe-oxides. Epidote alteration occurs as interstitial alteration of the gangue minerals. Chalcopyrite is the dominant matrix material within this section and forms anhedral irregular shaped anastomosing veins and fracture fillings. There are numerous inclusions of unknown microcrystalline minerals (probably sericite), with one and two phase fluid inclusions were observed in both feldspars and quartz.
Examination of IC-2 reveals anastomosing veins of specular hematite and minor chalcopyrite infilling fractures of a brecciated feldspar porphyry. The porphyry consists of plagioclase, K-spar, quartz, apatite, and secondary alteration minerals and goethite- limonite, sericite and chlorite. The porphyry is characterized by cataclastic textured, embayed, corroded, fractured and sericitized plagioclase and K-spar. These are set in an interstitial, granular matrix of anhedral quartz and subhedral to euhedral apatite (Photomicrograph 1), with very minor chlorite and late goethite-limonite alteration. An anastomosing reddish-brown Fe-oxide alteration mineral forms veins and veinlets interstitial to cataclastic textured minerals that are crosscut by late hematite. The hematite is comprised of subhedral bladed laths, which exhibit occasional primary or stress induced lamellae, and are intergrown with anhedral grains. Rutile forms interstitial granular aggregates often rimming and intergrown with, and occasionally crosscutting the hematite (Photomicrograph 2). Interstitial anhedral blebs of chalcopyrite occur throughout the gangue, often rimmed with an overgrowth of goethite (Photomicrograph 3). An occasional bright green vitreous mineral (malachite) is observed associated with the chalcopyrite.
Examination of IC-3 revealed a cataclastic-textured rock comprised of plagioclase, K-spar, quartz, and apatite, with minor alteration minerals sericite and chlorite, which are set in a matrix of hematite, goethite-limonite and trace chalcopyrite. The brecciated porphyry consists of sericitized, anhedral, corroded, embayed and fractured, plagioclase and K-spar grains, intermixed with anhedral quartz and interstitial subhedral to euhedral apatite, and
49 comminuted quartz and feldspar fragments. The cataclastic-textured fragments contain interstitial and occasional internal chlorite-alteration, evident in severely sericitized feldspars. The gangue has been crosscut by hematite, rutile, and Cpy veining, which has undergone late-alteration to goethite-limonite, chlorite, and clays. Anhedral irregular shaped magnetite inclusions (Photomicrograph 4) are visible as minute aggregates within the cores of the hematite. Hematite is usually rimed by granular aggregates of subhedral rutile. However, several rutile veins also crosscut the hematite (Photomicrograph 5 and 6). Hematite also contains numerous interstitial inclusions of silicate gangue minerals. Cpy occurs as anhedral blebs within gangue minerals, and as large angular grains which have been fractured and crosscut by goethite veins (Photomicrograph 7).
50 51
52 53 Sample # Island Copper sample IC-1 Microprobe: Location: Island Copper Property EMP Notes: Not requested. Rock Name: Equigranular Quartz-Feldspar Porphyry Photograph: Geochemistry: Not available Photo Notes: None, the polished thin section is too thick.
Hand Sample Pink coloured, brecciated, equigranular quartz-feldspar porphyry (QFP). The fragments appear suspended in anastomosing veins of chalcopyrite, and are variable in size and shape. In outcrop, the QFP is Description: massive with chalcopyrite forming anastomosing veins and veinlets throughout the rock with only local brecciation of the QFP.
Microscopic Examination reveals an inequigranular feldspar population of altered albitic plagioclase intermixed with sericitic K-feldspar (possibly orthoclase). Quartz forms anhedral, inequigranular, interstitial grains Description and intergranular aggregates between the feldspars. Apatite occurs as subhedral to euhedral grains predominantly as inclusions associated with quartz, along with subhedral to euhedral microcrystal inclusions of tourmaline. There are numerous inclusions of unknown microcrystalline mineral (probably sericite), with 1- and 2-phase fluid inclusions observed in both feldspars and quartz. Chalcopyrite forms veins of anhedral irregular shaped grains interstitial to the gangue minerals and along fractures. Goethite ( and limonite) occurring along fractures suggests secondary weathering. The thin section was thick, yielding anomalous higher order colouration in the feldspars and quartz. Mineral Modal % Size-mm Texture Alteration To: Altered From: Intergrown With: Notes: Cpy 10.00% irregular shaped, interstitial, fracture and goethite / gangue Chalcopyrite occurs as anhedral irregular shaped blebs interstitial to gangue minerals and vein filling, goethite/limonite rims, no limonite as vein and fracture fillings. No inclusions were noted within the Cpy. Grains display a inclusions observed very weak anisotropism. Goethite/limonite appears to rim occasional grains in fractures, suggesting weathering, however, no alteration Cu-minerals were observed. rutile 1.00% ± 0.05 subhedral to euhedral granular sphene goethite/limonite, Rutile forms granular aggregates of subhedral to euhedral crystals, and occasional euhedral aggregates and individual grains, high chalcopyrite, gangue individual grains, predominantly associated as rims about chalcopyrite, however some internal brown to reddish-brown grains were observed interstitial to the gangue. High internal reflections give a yellow- reflections brown to reddish-brown colouration with some grains exhibiting bright-white colouration, which occasionally show a relic sphene shape. plagioclase 35.00% ± 4 subhedral to anhedral grains with albite sericite K-spar, quartz, sericite, Plagioclase occurs as altered anhedral to subhedral grains exhibiting very strong albite twinning and occasional Carlsbad twins Cpy twinning and occasional Carlsbad twins. Edges of the grains are often embayed and rimmed by quartz and granular quartz aggregates. Sericite alteration is apparent in the larger grains evidenced by dusty interiors. Smaller anhedral grains do not show sericite alteration, and exhibit strong twinning. K-feldspar 30.00% ± 2 anhedral, cloudy and dusty grains with sericite primary K-spar? plag, quartz, Cpy, K-spar forms altered anhedral grains intergrown with plag and quartz, twinning is not occasional inclusions of Cpy, some sericite readily apparent, however several clear grains appear to have weak tartan twins. Grains are grains are rimmed with quartz and plag mostly cloudy with sericite alteration, with rims of quartz and plag. Occasional inclusions of Cpy were observed within the K-spar, occurring along fractures. There is no observable evidence to indicate if K-spar was primary. quartz 15.00% ± 1 anhedral, dusty grains with numerous plag, K-spar, Cpy, Quartz occurs as anhedral grains and granular aggregates interstitial to feldspars and as inclusions and observable fluid apatite, tourmaline overgrowths around the feldspars. Numerous 1- and 2-phase fluid inclusions where inclusions, commonly forms interstitial observed within the quartz, along with numerous unknown microcrystalline minerals aggregates giving a cloudy or dusty appearance to some quartz grains. Inclusions of subhedral to euhedral apatite and tourmaline occur within the quartz. sericite 6.00% <<0.1 microcrystalline aggregates on unknown feldspars tourmaline, apatite, Sericite forms inclusions of fine-grained aggregates of microcrystalline minerals and clays, minerals and clays, gives the fsp and microcrystalline giving a cloudy or dusty appearance to the feldspars. The minerals are too fine-grained for occasional quartz grains cloudy-dusty minerals positive identification and are intermixed with tourmaline and apatite microcrystals and interiors fluid inclusions within the gangue minerals. goethite 2.00% reddish-brown, earthy lustered to vitric, clays and Fe-rich minerals Cpy Goethite forms reddish-brown, earthy to vitric or glassy luster, fractures within the goethite fractured concentric radial to colloform unknown form concentric radial to colloform textures and overgrowths around Cpy grains. Goethite textured overgrowths about Cpy minerals also occurs within occasional crosscutting fractures that also contain Cpy.
epidote 0.50% <0.1 anhedral, radial, granular aggregates of sericite feldspars interstitial to gangue Epidote forms very fine-grained, anhedral, granular aggregates of acicular and prismatic acicular and prismatic crystals green to yellowish-green vitreous crystals, that occur interstitial to occasional feldspar grains. There appears to be an association between epidote and goethite, as both are occasionally intergrown, or the goethite is altering from the epidote. apatite 0.50% ± 0.1 anhedral to subhedral grains and gangue Apatite forms clear glassy, anhedral to subhedral, prismatic or columnar grains either in occasional aggregates of columnar granular aggregates or individual grains interstitial to quartz and feldspars. The grains are crystals often observed with hexagonal cross-sections, are high relief, and exhibit first-order gray colours in crossed polars in areas were the thin section is close to 30 microns thick. Tourmaline 0.1% <0.1 Subhedral to euhedral acicular crystals gangue Tourmaline forms acicular clear glassy, subhedral to euhedral microcrystals interstitial to forming individually or in aggregates. the feldspars and quartz, as individual crystals or aggregates. Total Modal % 100.00% Note: Due to the thickness of the thin section, identification of some of the minerals was difficult.
54 Sample # Island Copper sample IC-2 Microprobe: Location: Island Copper Property EMP Notes: Not requested. Rock Name: Equigranular Quartz-Feldspar Porphyry Photograph: XX Geochemistry: Not available Photo Notes: 1) Hem veins crosscutting cataclastic textured QFP
Hand Sample Pinkish-red, hematite-stained, matrix- to clast-supported, brecciated feldspar porphyry, set in a non-magnetic matrix of specular hematite. Chalcopyrite appears associated with the Fe-oxide matrix and Description: forms irregular shaped blebs and minor veinlets. Epidote-alteration occurs within the porphyry and is crosscut by the Fe-oxides, suggesting epidote-alteration was early. Secondary weathering minerals are visible occurring as anhedral tan coloured minerals alongside fractures. Microscopic Examination reveals hydrothermal veins of specular hematite brecciating the feldspar porphyry. However, the porphyry appears to have been previously brecciated evidenced by ratty, embayed, fractured Description feldspars in an interstitial, granular matrix of anhedral quartz and subhedral to euhedral apatite, with very minor chlorite and late goethite-limonite alteration. There appears to be an anastomosing, reddish- brown alteration product forming veins and veinlets interstitial to all the minerals (probably Fe-oxides such as goethite). Hematite veins consist of anhedral grains interstitial to subhedral bladed laths, which exhibit occasional primary or stress induced lamellae, and form anastomosing veins that crosscut the gangue. Rutile is often intergrown with, and occasionally crosscuts the hematite. Interstitial anhedral, irregular shaped blebs of chalcopyrite occur throughout the gangue, often rimmed with an Fe-oxide or sphalerite (?). Mineral Modal % Size-mm Texture Alteration To: Altered From: Intergrown With: Notes: hematite 15.00% ± 0.5 anhedral interstitial blebs and goethite / gangue Hematite forms massive, randomly oriented subhedral blades intergrown with interstitial anhedral blebs. unoriented subhedral blades vein limonite which form veins that crosscut the rock. Occasional blades exhibit twinning and stress lamellae. material and individual blades, Interstitial gangue material is often intergrown with the hematite. Rutile often rims blades and occurs as exhibiting twins and stress lamellae overgrowths on occasional blades. Alteration to goethite-limonite is visible along rims. chalcopyrite 1.00% ± 0.02 irregular shaped grains intergrown Fe-oxide mineral Chalcopyrite forms irregular shaped blebs either rimmed or included in Fe-oxide minerals scattered with or included in Fe-oxide material throughout the gangue. However, the material surrounding the cpy appears to be microcrystalline aggregates of goethite (or sphalerite?) with a reddish-brown colouration and occasional deep-red internal reflections. There does not appear to be a clear relationship with the hematite veining, however there are occasional Cpy grains that appear to be in the same fracture system as hematite. rutile 2.00% << 0.01 subhedral granular aggregates of ilmenite? hem Rutile occurs as interstitial granular aggregates with a strong association to hematite. The grains display yellowish and reddish-brown grains massive internal reflections of yellow to reddish brown. There are occasional veins of rutile that crosscut interstitial to hem, numerous internal the hematite, suggesting syn- and late-alteration formation of rutile. Occasional bright green vitreous reflections minerals occur with the rutile and appears to be Malachite. plagioclase 30.00% < 1.3 subhedral, irregular shaped, skeletal, sericite, clays k-spar, quartz Plagioclase exhibits skeletal, embayed, irregular shaped cataclastic textures, with rims of interstitial embayed, cataclastic textured, apatite granular aggregates of feldspar and quartz. Occasional fractures within the phenocrysts show quartz sericitized grains, albite twinning replacement. Albite twinning is visible with variably thick lamellae. The majority of the phenocrysts display moderate to severe sericite alteration depending on fracturing within the crystals. K-spar 25.00% < 1.0 subhedral, irregular shaped, skeletal, sericite, clays plag, quartz, K-spar exhibits a subhedral, embayed, cataclastic texture, with interstitial granular aggregates of feldspar embayed, cataclastic textured, apatite and quartz. Occasional fractures within the phenocrysts show quartz replacement. Perthitic and sericitized grains, perthitic to occasional tartan twinning is occasionally visible, however, the majority of crystals have no twinning. occasional tartan twinning The majority of the phenocrysts display moderate to severe sericite alteration. quartz 15.00% < 0.8 anhedral irregular shaped grains with k-spar, plag, Quartz exhibits anhedral, interstitial, irregular shaped grains, and intergrown granular aggregates that numerous fluid inclusions and apatite, unknown surround and occur along fractures within feldspars. The quartz displays undulose extinction and contains microcrystal inclusions crystals numerous 1-, 2- and occasional 3-phase fluid inclusions, and unknown microcrystals. There are rounded to subangular feldspar inclusions trapped within the qtz. apatite 8.00% < 0.2 anhedral, subhedral and euhedral gangue Apatite forms anhedral, subhedral to occasional euhedral crystals, forming granular aggregates interstitial crystals at various orientations to the gangue minerals with an affinity to interstitial anhedral quartz. Occasional grains contain numerous occurring as aggregates interstitial to 2-phase fluid inclusions. Occasional larger grains of apatite appear to have inclusions of smaller euhedral the gangue minerals apatite crystals, suggesting several stages of growth. goethite / 2.00% < 0.1 anhedral, vitreous reddish-brown to clays feldspars, gangue and Goethite/iddingsite occurs as interstitial vitreous material displaying yellow-brown to reddish-brown limonite yellow-brown interstitial material hematite hematite veining colouration within the gangue minerals and the hematite veining. The interstitial material within the gangue helps to delineate crystal rims, and appears to form veins or veinlets with an observable association to chlorite alteration. Goethite also forms overgrowths around Cpy grains. sericite 1.00% < 0.01 microcrystalline inclusions within the clays feldspars Sericite forms microcrystalline inclusions to the feldspar grains giving them a dusty or cloudy feldspar grains giving them a cloudy appearance. The sericite alteration is variable within the feldspars, with occasional feldspars exhibiting or dusty appearance very little to moderate alteration, and some feldspars are completely clouded over. There is an increase in chlorite alteration surrounding and intruding the severely sericitized feldspars. chlorite 0.50% < 0.1 anhedral, feathery to radial masses clays feldspars gangue and Chlorite appears interstitial to and occasionally intruding severely sericitized feldspar crystals, following interstitial to gangue and hematite hematite veining fractures and veins. Chlorite is strongly associated with the goethite/iddingsite alteration veining and minerals helps to delineate feldspar crystals within the gangue. Chlorite also occurs rimming and interstitial to the hematite veining intergrown with quartz. Total Modal % 99.50%
55 Sample # Island Copper sample IC-3 Microprobe: Location: Island Copper Property EMP Notes: Not requested. Rock Name: Equigranular Quartz-Feldspar Porphyry Photograph: XX Geochemistry: Not available Photo Notes: 1) Photo of the rims of sph or goethite around Qtz. 2) Photo of magnetite inclusions in hematite 3) goethite veins in Qtz. 4) Rutile cross- cutting hematite Hand Sample Pinkish-red, hematite-stained, brecciated feldspar porphyry in matrix- to clast-support, set in a non-magnetic specular hematite matrix. Chalcopyrite appears associated with the Fe-oxide matrix and forms irregular Description: shaped blebs and minor veinlets. Greenish epidote-alteration occurs in porphyry minerals that are crosscut by Fe-oxide veins. Secondary weathering minerals are visible occurring as anhedral tan coloured minerals alongside fractures, and goethite-limonite. Microscopic Cataclastic textured rock comprised of anhedral, embayed and fractured feldspars intermixed with anhedral quartz grains, interstitial subhedral to euhedral apatite, granular quartz and feldspar fragments. The gangue Description has been crosscut by hematite, rutile and Cpy veining, which has undergone late-alteration to goethite, chlorite and clays. Cpy occurs as blebs in the gangue and as large grains fractured and crosscut by goethite veins. Twinned and stressed hematite blades contain occasional irregular shaped to rounded inclusions of magnetite. Hematite is usually rimed by rutile, however there are several rutile veins crosscutting the hematite. Mineral Modal % Size-mm Texture Alteration To: Altered From: Intergrown With: Notes: hematite 30.00% ± 0.6 anhedral interstitial blebs and goethite, magnetite gangue, Hematite forms massive, randomly oriented subhedral blades intergrown with interstitial anhedral unoriented subhedral blades vein limonite, magnetite, rutile blebs, and contains anhedral inclusions of magnetite. Blades exhibit twinning and stress lamellae. material and individual blades, chlorite Gangue material occurs interstitial and intergrown with the hematite. Rutile occurs rimming blades exhibiting twins and stress lamellae and occasionally crosscuts the hematite, alteration to goethite/limonite is visible along edges. rutile 3.00% ± 0.05 subhedral granular aggregates of ilmenite? hem Rutile occurs as interstitial granular aggregates, as overgrowth rims and crosscutting veins in hematite, yellow to reddish-brown grains with individual crystals or clusters in the gangue. The grains display massive internal reflections of interstitial to hem, numerous internal blue-white, yellow-white to reddish brown in the overgrowths and veins. Occasional small fractures reflections within the gangue contain veins filled with rutile. chalcopyrite 1.00% one grain rounded to irregular shaped anhedral goethite sphalerite, Chalcopyrite occurs as rounded to irregular shaped anhedral grains often rimmed by goethite. In large at 5, the grains occasionally rimmed by goethite grains the goethite is present in crosscutting veins, and surround occasional inclusions of hematite. rest < 0.1 sphalerite or veined by goethite The goethite veins often extend out of the Cpy into the surrounding gangue. magnetite 0.10% << 0.01 inclusions of anhedral, irregular hematite Magnetite occurs as inclusions of anhedral, irregular shaped to rounded grains or clusters of inclusions shaped to rounded grains in in occasional hematite blades. Texture suggests the hematite formed at the expense of magnetite, occasional hematite blades which implies original Fe-rich fluids formed magnetite then oxidized to hematite. sphalerite 0.01% < 0.02 anhedral, massive rims on Cpy blebs Cpy Possible sphalerite may rim occasional Cpy grains found within the cataclastic textured gangue. that exhibit reddish-brown to deep- Petrographically the mineral resembles sphalerite, especially the internal reflections occasionally red internal reflections observed on some overgrowths. However, the mineral also resembles goethite overgrowths, which is observed in large Cpy grains as crosscutting vein material and in smaller grains near hematite. goethite / 3.00% ± 0.01 anhedral radiating masses, clays Fe-oxides, gangue, hematite Goethite/iddingsite occurs as interstitial vitreous material displaying yellow-brown to reddish-brown limonite overgrowths and crosscutting vein feldspars colouration within the gangue minerals and as rims surrounding hematite. It also forms crosscutting material, reddish-brown interstitial veins through some of the Cpy grains. It appears to be associated with chlorite within the cataclastic vitreous material textured gangue minerals. However, the strongest associations are with hematite. plagioclase 25.00% ± 1 subhedral, irregular shaped, skeletal, sericite, clays k-spar, quartz Plagioclase exhibits a skeletal, embayed, irregular shaped cataclastic texture, with rims of interstitial embayed, cataclastic textured, apatite granular aggregates of feldspar and quartz. Occasional fractures within the phenocrysts show quartz sericitized grains, albite twinning replacement. Albite twinning is visible with variably thick lamellae. The majority of the phenocrysts display moderate to severe sericite alteration and appears to be dependant on fracturing within the crystals. K-feldspar 15.00% ± 1 subhedral, irregular shaped, skeletal, sericite, clays plag, quartz, K-spar exhibits a subhedral, embayed, cataclastic texture, with interstitial granular aggregates of embayed, cataclastic textured, apatite feldspar and quartz. Occasional fractures within the phenocrysts show quartz replacement. Perthitic sericitized grains, perthitic to and occasional tartan twinning is occasionally visible, however, the majority of crystals have no occasional tartan twinning twinning. The majority of the phenocrysts display moderate to severe sericite alteration. quartz 15.00% ± 1 anhedral irregular shaped grains with k-spar, plag, Quartz exhibits anhedral, interstitial, irregular shaped grains, and intergrown granular aggregates that numerous fluid inclusions and apatite, unknown surround and occur along fractures within feldspars. The quartz displays undulose extinction, and microcrystal inclusions crystals contains numerous microcrystals, and 1-, 2- and occasional 3-phase fluid inclusions. There are rounded to subangular feldspar inclusions trapped within some qtz. apatite 5.00% ± 0.07 anhedral, subhedral and euhedral gangue Apatite forms anhedral, subhedral and occasional euhedral crystals, forming granular aggregates crystals at various orientations interstitial to the gangue minerals with an affinity to interstitial anhedral quartz. Occasional grains occurring as aggregates interstitial to contain numerous 2-phase fluid inclusions. Occasional larger grains of apatite appear to have the gangue minerals inclusions of smaller euhedral apatite crystals, suggesting several stages of growth. sericite 2.00% < 0.01 microcrystalline inclusions within the clays feldspars Sericite forms microcrystalline inclusions in the feldspar grains giving them a dusty or cloudy feldspar grains giving them a cloudy appearance. The sericite alteration is variable within the feldspars, with occasional feldspars exhibiting or dusty appearance very little to moderate alteration, and some feldspars are completely clouded over. There is an increase in chlorite alteration surrounding and intruding the severely sericitized feldspars. chlorite 0.50% < 0.02 anhedral, feathery to radial masses clays feldspars gangue and Chlorite appears interstitial to and occasionally intruding severely sericitized feldspar crystals, interstitial to gangue and hematite hematite veining following fractures and veins. Chlorite is strongly associated with the goethite/iddingsite alteration minerals veining and helps to delineate feldspar crystals within the gangue. Chlorite also occurs rimming and Total Modal % 99.61% interstitial to, the hematite veining and is often intergrown with quartz. 56 APPENDIX 2
Whole Rock Geochemistry of Selected Samples from the Island Copper Property
57 SAMPLE Grid_E Grid_N FIELD_ SIO2 AL2O3 CAO MGO NA2O K2O FE2O3 TIO2 P2O5 NAME AT08775 100+98 88+20 9 70.38 14.82 0.19 1.71 7.17 0.28 3.78 0.28 0.08 AT08778 96+85 89+00 9 77.93 11.55 0.35 1.04 5.77 0.33 1.62 0.49 0.19 AT08779 100+00 90+85 9 71.52 13.67 0.37 1.82 5.55 1.09 3.61 0.46 0.15 AT08780 100+00 89+60 9 74.01 14.1 0.18 0.87 6.89 0.82 1.77 0.25 0.04 AT08784 100+98 88+00 9 78.35 10.54 0.12 0.51 5.72 0.09 3.59 0.1 0.04 AT08786 98+03 88+30 9 72.46 13.89 0.17 2.23 4.98 1.37 3.17 0.16 0.015 AT08787 100+65 89+00 9 70.43 9.61 0.12 0.47 4.79 0.34 9.42 0.26 0.15 AT08791 90+18 90+02 9 81.64 8.63 0.27 1.76 2.23 1.34 2.43 0.29 0.09 AU02162 101+15 89+00 9 69.32 15.05 0.07 0.3 8.64 0.21 5.21 0.26 0.07 AU02163 100+00 89+00 9 70.32 14.6 0.25 0.35 8.56 0.1 4.1 0.74 0.25 AU08795 101+25 89+00 9 46.8 13.82 <0.01 0.24 7.79 0.1 30.64 0.14 0.1 AT08776 92+00 80+45 12 69.85 15.98 0.62 1.44 5.42 2.88 2.04 0.33 0.09 AT08781 89+95 90+00 12 76.11 12.64 0.38 0.44 3.77 3.09 1.96 0.2 0.015 AT08782 102+33 89+00 12,bx 67.86 12.85 0.14 4.3 4.48 0.19 7.01 0.19 0.06 AT08783 102+40 87+85 12,bx 65.91 12.27 0.23 6.25 3.35 0.09 7.65 0.27 0.13 AT08785 100+45 88+00 12,bx 61.38 18.69 0.32 3.58 8.48 0.16 4.73 0.31 0.15 AT08790 101+80 90+00 12,bx 73.14 13.95 0.16 1.5 5.53 1.48 2.38 0.23 0.05 AT08792 101+50 91+00 12,bx 62.98 14.61 0.73 4.14 3.65 1.64 7.38 0.78 0.54 AT08794 101+10 88+90 12,bx 61.8 15.03 0.005 6.09 4.47 0.24 8.79 0.37 0.04 AU02164 101+01 89+00 12,bx 66.74 15.54 0.27 2.86 6.84 0.42 4.64 0.47 0.13 AU02165 99+50 93+00 12,bx 66.25 18.47 0.28 0.2 10.89 0.11 3 0.51 0.16 AT08777 90+55 87+95 7,
58 MNO LOI _COL16 Y ZR BA SR CU ZN NI CR CHEM_ID ALUM 0.03 1.54 100.26 3 181 45 79 11 62 20 193 9jA 194 0.03 0.94 100.24 17 354 76 83 9 39 8 233 4,9jA 179 0.08 1.56 99.88 5 317 307 143 3 111 13 242 4,9jA 195 0.03 1.06 100.02 3 149 86 106 9 25 11 209 4,9jA 179 0.03 1.06 100.15 1 68 33 28 11 18 8 255 4,9jA 178 0.05 1.89 100.39 3 87 215 83 3 70 15 247 4,9jA 213 0.02 4.75 100.36 3 110 45 44 4168 41 47 294 4,9jA 183 0.01 1.54 100.23 4 182 98 70 5 9 6 326 4,9jA 225 0.005 0.91 100.05 2 141 17 37 765 21 9 179 4,9jA 169 0.005 0.73 100.01 2 91 30 50 5113 18 8 216 3,8j 164 0.01 0.58 100.23 1 5 9 9 580 43 3 88 4,9i 175 0.02 1.41 100.08 3 115 906 239 0.5 33 7 164 9jA 179 0.02 1.33 99.96 4 289 1974 152 5 18 6 279 4,9jA 175 0.03 2.63 99.74 1 82 28 47 8 30 22 198 4,9jA 267 0.07 3.6 99.82 3 132 18 48 6 121 45 217 4,9jA 334 0.03 2.54 100.37 5 482 50 119 3 62 24 71 4,9i 209 0.02 1.4 99.84 3 96 239 128 12 23 10 224 4,9jA 195 0.05 3.31 99.81 7 264 258 72 8 50 32 212 3,8jy 243 0.06 3.61 100.51 3 63 36 53 46 149 41 145 4,9jA 319 0.05 1.91 99.87 2 141 56 99 30 73 24 146 4,9jA 206 0.01 0.55 100.43 20 201 25 81 104 18 5 111 3,8i 164 0.16 1.85 99.84 31 290 449 496 38 154 26 113 2,7jyz 125
59 AG CO PB S V AS SN CD SB BI TA W MO 0.25 72 1 0.253 40 14 10 0.5 2.5 2.5 2.5 10 0.5 0.25 4 1 0.019 24 11 10 0.5 2.5 2.5 2.5 10 1 0.25 10 21 0.06 35 6 10 0.5 2.5 2.5 2.5 10 0.5 0.25 11 1 0.028 20 21 10 0.5 2.5 2.5 2.5 10 1 0.25 36 1 0.346 14 10 10 0.5 2.5 2.5 2.5 10 0.5 0.25 8 16 0.006 33 10 10 0.5 2.5 2.5 2.5 10 0.5 4.6 138 3 7.079 12 23 10 1 2.5 2.5 2.5 10 5 0.25 3 1 0.004 36 2.5 10 0.5 2.5 2.5 2.5 10 0.5 0.25 4 7 0.106 28 6 10 0.5 2.5 2.5 2.5 10 2 0.25 7 1 0.489 25 8 10 0.5 2.5 2.5 2.5 10 0.5 <0.2 3 6 300 88 <5 <20 <0.2 <5 <5 <10 <20 <1 0.25 5 3 0.009 27 12 10 0.5 2.5 2.5 2.5 10 0.5 0.25 2 1 0.045 12 31 10 0.5 2.5 2.5 2.5 10 0.5 0.25 17 3 0.04 44 9 10 1.5 2.5 2.5 2.5 10 1 0.25 17 6 0.004 88 10 10 0.5 2.5 2.5 2.5 10 0.5 0.25 9 1 0.006 42 15 10 0.5 2.5 2.5 2.5 10 0.5 0.25 6 1 0.014 39 8 10 0.5 2.5 2.5 2.5 10 0.5 0.25 16 9 0.011 74 13 10 0.5 2.5 2.5 2.5 10 0.5 0.1 16 52 0.02 53 2.5 10 0.3 2.5 2.5 5 10 0.5 0.25 21 1 0.06 53 5 10 0.5 2.5 2.5 2.5 10 0.5 0.25 0.5 1 0.017 30 2.5 10 0.5 2.5 2.5 2.5 10 0.5 0.25 30 1 0.194 213 14 10 0.5 2.5 2.5 2.5 10 0.5
60 LA LI MN GA SC NB MGO# CA_AL NI_MGO ISHIKW ZN_NA2O UTM_E UTM_N 5 10 232 5 2.5 2.5 0.52 0.01 12 21 9 708613 5172289 75 8 246 5 2.5 5 0.6 0.03 8 18 7 708197 5172333 12 9 657 5 2.5 2.5 0.55 0.03 7 33 20 708488 5172521 21 6 244 12 2.5 2.5 0.54 0.01 13 19 4 708494 5172397 2.5 5 272 5 2.5 2.5 0.25 0.01 16 9 3 708612 5172264 2.5 11 405 11 2.5 2.5 0.63 0.01 7 41 14 708333 5172253 26 5 126 5 2.5 2.5 0.11 0.01 100 14 9 708561 5172350 21 11 105 5 2.5 2.5 0.63 0.03 3 55 4 707532 5172354 12 4 61 10 2.5 2.5 0.12 0 30 6 2 708625 5172353 8 3 50 5 2.5 2.5 0.17 0.02 23 5 2 708496 5172347 8 2 106 4 <5 7 0.02 0 13 4 6 708631 5172350 17 10 165 17 2.5 2.5 0.63 0.04 5 42 6 707784 5171411 7 3 114 14 2.5 2.5 0.35 0.03 14 46 5 707500 5172354 5 16 214 5 2.5 2.5 0.59 0.01 5 49 7 708745 5172377 30 18 541 5 6 7 0.66 0.02 7 64 36 708724 5172305 79 14 275 5 2.5 2.5 0.64 0.02 7 30 7 708554 5172267 11 8 170 5 2.5 2.5 0.6 0.01 7 34 4 708678 5172472 87 23 417 5 6 8 0.57 0.05 8 57 14 708641 5172575 13 20 476 21 5 3 0.62 0 7 59 33 708610 5172341 39 12 400 5 6 2.5 0.6 0.02 8 32 11 708600 5172348 17 3 106 12 2.5 17 0.14 0.02 25 3 2 708426 5172738 30 14 1271 5 21 23 0.41 0.47 7 31 40 707598 5172204
61