PACIFIC COAST NICKEL SYNDICATE (OWNER) BIG NIC PROPERTY

PACIFIC COAST NICKEL CORP. (OPERATOR) ASSESSMENT REPORT PACIFIC COAST NICKEL SYNDICATE (OWNER) BIG NIC PROPERTY

M.McCLAREN, P.Geo. Crockite Resources Ltd. . (604)986-5873 e-mail: [email protected]

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Geological and Geophysical Report on the Big Nic Property WORK CARRIED OUT ON THE BIG NIC 2 - 406269, BIG NIC 5 - 414677, BIG NIC 6 – 414700, BIG NIC 17- 415244, SLIM - 517029, 512546 and 512555 MINERAL TENURES

NEW WESTMINSTER MINING DISTRICT BRITISH COLUMBIA

NTS: 092H/043 and Southeastern Portion of 092H/042.

Latitude: 49 degrees 26 minutes 10 seconds Longitude: 121 degrees 34 minutes 51 seconds Prepared for: PACIFIC COAST NICKEL CORP. OPERATOR And PACIFIC NICKEL SYNDICATE OWNER Period of Field Work: June 22nd to Sept 23rd, 2006.

Prepared by: Murray McClaren, P.Geo. CROCKITE RESOURCES LTD. 283 Woodale Road, North Vancouver, British Columbia, V7N 1S6 March 19th, 2007.



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INTRODUTION Pacific Coast Nickel Corp. completed $40,518.52 of work on the Big Nic Property in 2006. This work involved the collection of rock samples (both for analytical and thin section analysis) and the collection of approximately 3.1 kilometers of magnetometer survey data. Both reconnaissance scale and detailed geological mapping were carried out on Big Nic tenures 414677, 414700, 517029 and 521555. The work was carried out during the period of late June to late September 2006. The purpose of the surveys was to define nickel-copper-cobalt exploration target areas and broadly assess other areas for their nickel-copper (+/-PGM) mineral potential. Previous exploration located several areas of massive sulphide rubble located on the Big Nic mineral tenures 414677 and 414700 mineral tenures. Prospecting during the 2006 field season located additional areas of rubble mineralization (Sp Gabbro, MS-8 and MS-10) on mineral tenure 512555. In addition, an AeroTem II electromagnetic and magnetometer survey carried out by Aeroquest Limited for

Pacific Coast Nickel Corp. in 2005 (A.R. #28019) identified areas on the Big Nic

Property that warranted further assessment. These areas were examined during the 2006 field program. Access to these areas was either by road; helicopter or by foot on mineral tenures 406269; 512555;415244 and 512546. Access to the Big Nic property is by the Garnet Creek Forest Access Road and other spur roads that take off from this road. A number of areas of more difficult access were examined by helicopter. Access to most areas of the property is by foot either through thick underbrush developed on previously logged off areas, or by walking through moderate to little undergrowth in areas in which no previous logging has taken place. Mineralization located in the northern portion of the Big Nic property is primarily found as angular rubble, that is close to its source area. Assays of mineralized rubble material (grab samples) from the MS Gabbro Area have yielded up to 0.93% Nickel; 7.44% Copper and .09% Cobalt. Mineralization consists of pyrrhotite, chalcopyrite and pentlandite associated with pyroxenite. At the MS Gabbro Area pyroxenite found mingled with a melanocratic hornblende gabbro is altered to hornblende. A magnetometer grid survey was carried out over the MS area and a walkmag survey to the west of this area. The grid survey was able to define the probable source of rubble mineralization in the MS area and the walkmag survey was able to detect other areas of interest. Geological mapping identified structural features similar to those found at the former Giant Mascot Nickel Mine. Work was carried out under Mines Act Permit MX-7-165; Approval # 06-1610334-0613 issued June 13, 2006. Units of measure used in this report are metric. Coordinates on maps are in latitude and longitude or in Universal Transverse Mercator (UTM) projection, using the North American Datum of 1983 (NAD’83).



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LOCATION The Big Nic Property consists of 46 contiguous mineral tenures which encompases an area of 9,826.685 hectares. The Big Nic Property lies to the south and southwest of the former Giant Mascot Nickel Mine. The main area in which work was carried out is located at a distance of approximately 5.5 kilometers southwest of Giant Mascot and at a distance of approximately 114 kilometers east northeast of Vancouver, B.C. and 12 kilometers northwest of Hope, B.C. The portion of the Big Nic Property that is the subject of this report is located in southwestern British Columbia on NTS mapsheet 92H/043 and the southeastern portion of NTS mapsheet 92H/042. The portion of the property lies along Garnet Creek and its tributary Ruby Creek and the headwaters of American Creek, located in the northern Cascade Range of British Columbia. FIGURE 1 LOCATION MAP – BIG NIC PROPERTY M.McCLAREN, P.Geo., February 2007



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CLAIMS and HISTORY

The initial Big Nic Property mineral claims (512555; 512546 and 406269) were located in October 2003, to cover, in part, an area previously explored by Santoy Resources Ltd.(A.R. #26876) and an area in which there was anomalous values for nickel and chrome in silts (Regional Geochemistry Survey; NGR stream sediments and waters, NTS 92H, Hope, British Columbia, 1981). Additional claims were acquired by the Pacific Nickel Syndicate after discovery of rubble consisting of massive sulphide mineralization located on the northern portion of mineral tenure 512555 in late September, 2004. The claims acquired by the Pacific Nickel Syndicate (E.Dodson, Manager) were subsequently optioned by Pacific Coast Nickel Corp. The Big Nic Property is comprised of the following contiguous mineral tenures. TABLE 1

Tenure Number Claim Name

Map Number Good To Date Mining Division Area

406269 BIG NIC 2 092H043 2008/dec/31 NEW WESTMINSTER 400.0

414677 BIG NIC 5 092H043 2008/jun/30 NEW WESTMINSTER 25.0

















505167 092H 2008/dec/31 NEW WESTMINSTER 735.919



512555 092H 2008/jun/30 NEW WESTMINSTER 735.342



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501351 Ruby 092H 2008/nov/30 NEW WESTMINSTER 503.913

501554 Ruby 2 092H 2008/nov/30 NEW WESTMINSTER 503.997

502082 Steve 092H 2008/dec/31 NEW WESTMINSTER 147.035

502099 Steve 4 092H 2008/dec/31 NEW WESTMINSTER 357.253

502127 Steve 6 092H 2008/jun/30 NEW WESTMINSTER 126.115

503896 Wood 092H 2008/dec/31 NEW WESTMINSTER 210.237

512534 CORNER 092H 2008/dec/31 NEW WESTMINSTER 210.319

512551 SQUARE 092H 2008/jan/31 NEW WESTMINSTER 273.289

517029 SLIM 092H 2007/dec/31 NEW WESTMINSTER 63.013

517088 POWERLINE 092H 2008/jan/31 NEW WESTMINSTER 21.015

517135 BIG NIC NE 092H 2008/jan/31 NEW WESTMINSTER 63.012

517156 BIG NIC SOUTH 092H 2008/jan/31

NEW WESTMINSTER 21.017

517170 BIG NIC EAST 092H 2007/dec/31

NEW WESTMINSTER 168.085

517188 BIG NIC NW 092H 2008/nov/30 NEW WESTMINSTER 41.984

518245 BRITNIT 092H 2008/dec/31 NEW WESTMINSTER 483.525

414938 MAS 12 092H043 2008/jun/30 NEW WESTMINSTER 25.0




543623 Mineral GAP 2007/oct/19 NEW WESTMINSTER 357.335

524831 Mineral 2008/dec/31 NEW WESTMINSTER 524.805

524834 Mineral BEAR 2 2008/dec/31 NEW WESTMINSTER 524.743

TOTAL # Mineral Tenures 46

TOTAL Ha 9,826.685



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ZOFKA RIDGE Countour Interval = 20 meters FIGURE 2 MINERAL TENURES ON WHICH WORK CONDUCTED M.McCLAREN, P.Geo., February 2007



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PHYSIOGRAPHY, CLIMATE , VEGETATION AND LOGISTICS The Big Nic Property area lies in the Cascade Range on the eastern edge of the Pacific Ranges of British Columbia's Coast Mountains. The Cascade Range lies to the east of the Pacific Range and is flanked by and merges in the Kamloops Plateau. Elevation in the area of the property ranges to 1425 meters at the summit of Zofka Ridge. The majority of the property lies at an elevation of 800 meters to 1300 meters. Vegetation below tree line is typical coast rain forest and comprises cedar, hemlock, spruce trees with alder, willow and cottonwood on old roads and in poorly drained areas. Undergrowth is typically a variable mixture of salal, Devil's club and salmonberry. Tree line varies between 1200 and 1650 m asl. Above tree line the vegetation is alpine, becoming progressively sparser at higher elevations. Average temperatures at Hope, B.C., approximately 12 km to the southeast of the property, vary from 1.1°C in January to 18.8°C in August. Annual rainfall in Hope is 176.9 cm and an average snowfall of 169.2 cm during the winter months of November to March. Despite this, all major and many subsidiary drainages flow throughout the year. Fieldwork is possible until late October and depending on the year until early-November at nearly any elevation and lower areas are accessible almost year round. Much of the area of the Big Nic Property has been extensively logged in previous years. Networks of logging roads cover the property and most of these roads are in very poor repair, making even poor foot trails. The main access road to the property is by the Garnet Creek Forest Access Road that begins approximately 1 kilometer east of Ruby Creek on Highway #7. Dense and thick vegetation has made access on portions of the Big Nic Property difficult. Active logging operations and new access roads on the southern portion of the Big Nic Property will allow examination of areas previously difficult to access.



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GEOLOGY OF NORTH CENTRAL BIG NIC PROPERTY FIGURE 3 AFTER: VINING, M.R., 1977 UTM ZONE 10 NAD 83 CONTOUR INTERVAL 20 METERS M.McClaren P.Geo., February 2007



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Legend for Figure 3



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GEOLOGY SPUZZUM PLUTON IN THE NORTH CENTRAL BIG NIC PROPERTY AREA The north-central portion of the Big Nic property is underlain primarily of rocks of the Spuzzum Pluton. The Spuzzum Pluton is a compositionally zoned and irregularly shaped body; approximately 10 x 30 km in plan view (Richards and McTaggart, 1976). The Spuzzum Pluton ranges from 96.3 +/- 0.5 Ma (zircon) (Brown,E.H. et al.; 2000) in the north northwest to 79 +/- 4 Ma (biotite) (Richards, T.A. and McTaggart, K.C. 1976) at the southern tonalitic portion of the pluton. Magmatic fabric is prevalent in the southern portion of the pluton but the northernmost part of the pluton is overprinted by solid-state foliation.

(1) PYROXENE DIORITE: Pyroxene >hornblende + biotite (+chlorite). Minute inclusions of hematite in plagioclase feldspars commonly give it a pink colour. The average anorthite content is An53 and ranges from a low of An43.7 to a high of An62.1 (Vining, M.R., 1977).

(2) HORNBLENDE DIORITE: Hornblende > pyroxene. Pyroxene < 10% and

hornblende > 10% + biotite + plagioclase. Plagioclase has an average composition of An47.5 and ranges from a low of An41.2 to a high of An53.8. (Vining, M.R., 1977).

(3) TONALITE: Largely composed of anhedral quartz and biotite, subhedral hornblende and plagioclase (An50 – An32). Locally foliated; locally hornblendized to resemble hornblende gabbro. Shows a gradational and conformable contact with metamorphic rocks. Small to large

zenoliths of gneiss and schist are included in tonalite in all parts. (Vining, M.R., 1977).

Tonalite was considered to be younger than diorites of the Spuzzum Pluton (Richards, T., 1971) and considered to be contemporaneous with other diorites of the Spuzzum Pluton by Vining, M.R., 1977. There is no presence of pyroxene with the tonalities.

(4) HORNBLENDIZED DIORITE AND TONALITE: Rocks believed to have formed by the hornblendization of diorite or tonalite are characterized by the abundance of hornblende, with plagioclase and perhaps quartz and biotite, but no pyroxene. These rocks grade into normal diorite or tonalite. Ultramafic bodies are closely associated with hornblendized rocks. Pyroxenes (predominately hypersthene) may be found in transitions to diorite and occur as corroded relicts in hornblende clots (Vining,M.R., 1977).



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Reconnaissance Geological Traverses Road, helicopter and foot traverses were carried out during the 2006 field season over various portions of the Big Nic (north central) Property. The purpose of these traverses was to define lithologies and to assess total field magnetic results obtained during an Aerotem II survey conducted by Aeroquest Limited in April, 2005 for Pacific Coast Nickel Corp (Ass.Rept. # 28019). Specific features noted in the various areas located on Figure 4 and Figure 5 are as follows:

(1) Contact relationship between hornblende diorite and pyroxene diorite are primarily transitional throughout most of the area of north central Big Nic. Sharp and not transitional contact relationships are found in the area of LOCALITY 1 where pyroxene diorite found in sharp contact with fine grained hornblende diorite. (2) Hornblende diorite contains an abundance of mafic enclaves. The

composition of these enclaves is primarily hornblende and a lesser number of enclaves consist of hornblende pyroxenite and pyroxenite. Areas of hornblendization of diorites are widespread and are primarily located within hornblende diorite.

Pyroxene diorite is primarily altered to granofels* in areas of mafic- ultramafic intrusions. The areaLextent of granofels may in part reflect the size of a potential mafic-ultramafic intrusion.

(3) Mafic-Ultramafic Rocks Several localities of previously unmapped mafic-ultramafic rocks were located during the 2006 field season. Dunite and its altered equivelants are found at Locality 9 and coincides with a total field magnetic high. Gabbro and pyroxenite found at Locality 8 is associated with sporadic magnetic highs and is located on the southwestern flank of an antiformal structure. *The term granofels is used to denote a medium grained; equigranular rock lacking foliation or lineation. The granofels is believed to be the result of mafic-ultramafic intrusive thermal action on pyroxene diorite.



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Medium grained pinkish pyroxene diorite in contact with fine grained PLATE 1 hornblende diorite. Note thin pyroxenite veinlets at left of photo. Location: LOCALITY 1

Hornblendite and feldspathic Hornblendite as fracture fillings in hornblende pyroxenite with fingers in hornblende diorite. hornblendized diorite. PLATE 2 PLATE 3 Location: LOCALITY 2. Location: LOCALITY 3.



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PLATE 4 Hornblende schilieren and enclaves in hornblende diorite. Location: LOCALITY 4. PLATE 5 Hornblende pyroxenite fingers and enclaves in granitic lithology. Location: LOCALITY 5.



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Pyroxenite enclave in hornblende diorite. PLATE 6 Location: LOCALITY 3. Folded pyroxenite enclave in hornblende diorite. PLATE 7 Location: LOCALITY 7.



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PLATE 8 Gabbro (to right of hammer head) and pyroxenite (to left of hammer head) enclosing partially assimilated granitic zenoliths. Location: LOCALITY 8.



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Dunite. Location: LOCALITY 9. PLATE 9 Altered Dunite. Location: LOCALITY 9. PLATE 10



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PLATE 11 Pyroxene diorite granofels with lenticular segregation of hematite in a feldspathic matrix. Location: LOCALITY 10.



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PLATE 12 Pyroxenite intrudes granofelsic pyroxene diorite. (Pyroxenite dark grey). . Location: LOCALITY 11.



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PLATE 13 Granofelsic pyroxene diorite at contact with hornblende gabbro dike. Location: LOCALITY 12.



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Location Map for Plates 1 to 13 FIGURE 4 UTM NAD 83 ZONE 10 M.McCLAREN, P.Geo. February 2007. Contour Interval = 20 meters (see figure 3 for legend)



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TOTAL MAGNETIC INTENSITY OF BIG NIC PROPERTY FIGURE 5 WITH LOCATIONS. M.McCLAREN, P.Geo., February 2007.



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INTERPRETATION OF GEOLOGICAL FEATURES AND TOTAL MAGNETIC INTENSITY MAP

(1) Areas of mafic enclaves and of hornblende pyroxenite intrusions occur predominately on the margins of elevated high total magnetic intensity features or within those magnetic high features. In specific, Localities 3, 7 and 5 (and possibly 2 and 4) are locations of mafic mingling features that are in proximity or within elevated total magnetic intensity features.

(2) The location of pyroxene diorite granofels appears to be located primarily

on the margins of moderately elevated total field magnetic intensity features (Localities 11 and 12) and in the case of Locality 10, within an area of a high total field magnetic intensity feature.

(3) The location of ultramafic (dunite) lies within a broad feature of elevated

high total field magnetic intensity. (Locality 9). (4) The location of gabbro-pyroxenite (Locality 8) lies on the southwestern

flank of a north to northeasterly trending arch of a moderate to high total magnetic field intensity feature.

(5) Waypoint 001 is located in an area where ultramafic (dunite) float was

encountered.

(6) Waypoints 002 and 003 are located in areas of hornblendized pyroxene diorite.

(7) Locality 2 is located in an area in which hornblende pyroxenite has

intruded and hornblendized diorites.

(8) Locality 1 marks a change from predominately hornblende diorite to pyroxene diorite.

In summary, it appears that large areas of the north central portion of the Big Nic Property are underlain by mafic-ultramafic intrusions. Many of these areas of mafic-ultramafic intrusions are not exposed and the presence of these cryptic intrusions is indicated by the features noted in (1) through (7).



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STRUCTURAL GEOLOGY The amalgamation of Wrangellia to North America about 100 million years ago contributed to the complex structural development of the east Harrison Lake area. The tectonic evolution of the region during and after accretion was accompanied and followed by Cretaceous (>96 Ma to locally 73 Ma) SW-NE contraction. This period of contraction was followed by dextral transpression (~73 to 55 Ma) then transtension (<55Ma ) (Paterson, R.L. et al.; 2004). Contraction was driven by thrusting and the east Harrison Lake area lies within the imbricate zone of the Coast Belt Thrust System. The region is characterized by low-angle thrust faults that envelop high-grade schists and gneisses and out-of-sequence, thick-skinned thrusting that caused southwestward telescoping of lithologies (Monger and Journeay, 1994). The age of thrusting is bracketed by a 146 Ma zircon age of dacite and the 95-104 Ma pluton belt that is intruded across the thrusts (Brown, E.H., et al; 2000). Bartholomew, P.R.;1979, recognized three periods of folding, in the Yale Creek area (approximately 10 kilometers north of the north central portion of the Big Nic Property). The earliest phase of folding, F1, preceded emplacement of the Spuzzum Pluton while F2 was contemporaneous with the emplacement of the Pluton. F3 folding was later than pluton emplacement and this event folded F2 structures. F1 folding is characterized by S1 fabric in Settler Schist and slaty cleavage in phyllites of the Slollicum Schists (Hettinga, M.A.; 1981). S1 foliation strikes northwest and is associated with the period of thrusting and contraction throughout the east Harrison Lake area. Macroscopic structures are reflected only in the F2 and F3 folding events. F2 folds are axial-planar to recumbent isoclinal folds. F3 folds may be developed into well defined synform-antiform structures in part coaxial with F2 folding Mineral fabric within portions of the Spuzzum Pluton is concordant with F2 structures (Bartholomew, P.R.; 1979). F3 folds are characterized as macroscopic folds and are upright to locally overturned with orogen-parallel axes that plunge variably northwest or southeast as much as 50 degrees and have wavelengths and amplitudes up to 7 or 8 km. The folds are entirely ductile structures and are closer to parallel rather than similar in style. Although on a broad scale F3 and F2 structures are approximately coaxial, in detail, F3 structures overprint F2 structures. On the basis of fold shape and absence of axial plane shear surfaces, these folds have been interpreted to be buckle structures (Brown, et al.; 2000) Ductile, high angle fault and shear zones that crosscut F1 to F3 deformational events record oblique slip; northeast side up and orogen parallel and orogen normal motions. These structures are older than approximately 91 Ma but younger than F3 folds (Brown,E.H.,et al.;2000).



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STRUCTURAL GEOLOGY OF NORTH CENTRAL BIG NIC PROPERTY The north central Big Nic Property has several dominant structural features:

(1) A shear dislocated, upright antiformal buckle fold can be traced for a distance of approximately 2 kilometers. An east northeast trending and northeasterly plunging forced fold (?) is developed at the base of the eastern portion of the F3 buckle fold.

(2) Antiformal F3 folds have accompanying parasitic folds. The parasitic folds

have axial planes that dip clockwise on the west and anticlockwise on the east of F3 antiforms. Tranverse jointing is developed on the flanks of F3 parasitic folds.

(3) Two prominent linear structures are associated with the sheared antiform:

(I) North 50 degree east striking and subvertical fault (F5). (II) North 45 degree west (315) striking and northeast (85 degrees)

dipping fault (FLT) and shear zone. (4) A north northeasterly trending high angle fault (Vining’s Fault). Vining’s

Fault strikes N30E and dips at approximately 60 degrees southwesterly. Movements associated with the buckle fold to the west of Vining’s Fault suggest a clockwise sense of rotation within an area between Vining’s Fault and a subparallel northeasterly structure approximately 2.5 kilometers west of the trace of Vining’s Fault.



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Minor Structural Features Gabbro Dikes Gabbro dikes are located within areas of extension. The dikes show little to no structural deformation. Dikes are generally less than 1 meter in width. Gabbro Dike 1: 298/68SW (W28N/68SW) Gabbro Dike 2: 30/68SE (N30E/68SE) Gabbro Dike 3: 50/60NW (N50E/60NW) Gabbro Dike 4: 314/58SW (N46W/58SW) Gabbro Dike 5: 310/75SW (N50W/75SW) Gabbro Dike 6: 310/70NE (N50W/70NE) Gabbro Dike 7: 320/77SW (N40W/77SW) Gabbro Dike 8: 290/74SW (W20N/74SW) Gabbro Dike 9: 30/34SE (N30E/34/SE) Gabbro-Pyroxenite Dikes Only gabbro dikes with a pyroxenite component have associated nickel-copper mineralization. Three outcrops of dikes of this nature were located in the field and are listed as follows: SP Gabbro: 10/55SE Hornblende gabbro dike with mineralized pyroxenite. Width of dike approximately 2 meters. EN Gabbro: 55/45SE Hornblende gabbro dike with mineralized pyroxenite. Width of dike approximately 0.5 meters. MS Gabbro: Strike 315 degrees; dip uncertain. Hornblende gabbro dike with abundant mineralized pyroxenite rubble. Width of dike is estimated to be up to 50 meters. Other intrusive features include: Pyroxenite Veinlets: Fracture-fillings in altered pyroxene diorite: 40/56SE Hornblendized Pyroxenite Dike (MFD): 20/85SE Other Structural Features: Schist Zenolith: 292/Vertical Fault (F5): 50/subvertical Fault (FLT): 315/85SW (shear) and 40/15NW (fault) CONCLUSIONS Four directions of extension are indicated: North 30 to 55 degrees East ; North 30 to 70 degrees West; North 10 degrees East and West 20 degrees North. These strike orientations are similar to the orientations of faults that control mineralization at the former Giant Mascot Nickel Mine (Clark, W.E.,1969).



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. Map of Major Structures and Location of Gabbroic Dikes: North Central Big Nic M.McCLAREN, P.Geo., February 2007 FIGURE 6 Contour Interval = 20 meters



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Legend for Figure 6



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MS Gabbro The MS Gabbro dike is the best exposed gabbroic dike found to date on the north central Big Nic Property. The dike occurs on the western margin of an F3 upright antiform. A variety of textures occur between the gabbro and the hornblende pyroxenite and include the following: PLATE 14 Ridge structures of pyroxenite and pillow structures of hornblende gabbro. PLATE 15 Hornblende gabbro “breccia” with pyroxenite matrix.



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PLATE 16 Hornblende gabbro in structural contact with hornblende gabbro-pyroxenite admixture. Melanocratic hornblende gabbro. PLATE 17



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PLATE 18 Hypersthene diorite (pyroxene diorite) breccia fragments within pyroxenite. Summary Pyroxenite intrudes hypersthene diorite (pyroxene diorite) and mingles with hornblende gabbro. Textures suggest that the hornblende gabbro was not fully consolidated at the time of emplacement of the pyroxenite.



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ANALYTICAL RESULTS During the 2006 field season one grab sample of mineralization from the location of MS-8 (see Figure 11 for Location) and two grab samples from the SP Gabbro (SPG-1 and SPG-2) were collected and analysed (see Figure 6 for Location). The samples were crushed to 70% passing <2mm; split by riffle splitter and then the split portion was pulverized to 85% < 75 um. A 0.25 gram sample was digested in a four acid digestion treatment and analysed by the induced coupled plasma technique for 27 elements. A 30 gram sample was analysed for Pt, Pd and Au by fire assay with an induced couple plasma finish. The results of the analyses are as follows:

PGM-ICP23

PGM-ICP23

PGM-ICP23

ME-ICP61a

ME-ICP61a

ME-ICP61a

SAMPLE Au Pt Pd Ag Co Cr

DESCRIPTION ppm ppm ppm ppm ppm ppm

MS-8 0.037 <0.005 0.091 6 990 230 ME-ICP61a

ME-ICP61a

ME-ICP61a

ME-ICP61a

ME-ICP61a

ME-ICP61a

Cu Fe Ni Pb S Zn

ppm % ppm ppm % ppm

43100 42.3 6620 20 18.4 170

PGM-ICP23

PGM-ICP23

PGM-ICP23

ME-ICP61

ME-ICP61

ME-ICP61

ME-ICP61

ME-ICP61

SAMPLE Au Pt Pd Ag Co Cr Cu Fe

DESCRIPTION ppm ppm ppm ppm ppm ppm ppm %

SPG-1 0.032 <0.005 0.027 <0.5 251 480 2860 19.4

SPG-2 0.113 0.008 0.036 0.7 358 502 6580 23.2

ME-ICP61

ME-ICP61

ME-ICP61

ME-ICP61

Ni Pb S Zn

ppm ppm % ppm

2510 2 6.11 223

3370 7 7.96 208

Mineralization found at MS-8 is similar to that found at the MS Gabbro Area and also to rubble massive sulphide found near the EN Gabbro area (MS-9). The mineralization is associated with rubble of hornblende gabbro at both the MS-8 and EN Gabbro areas (MS-9) and the sulphide mineralization is massive in character. Mineralization found at the SP Gabbro area (UTM co-ordinates 602822E and 5476880N) is found to be disseminated within pyroxenite (websterite).



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RESULTS OF THIN SECTION ANALYSIS The results of an analysis of eight thin sections (2 samples from the SP Gabbro and 8 samples from the MS Gabbro areas) indicate that the mafic-ultramafic lithologies consist of websterite; plagioclase-bearing websterite and norite. The MS Gabbro is characterized by an anastomosing network of masses of fine amphibole in a fine to medium-grained groundmass of plagioclase. Magnetite and rare sheaves of biotite occur associated with amphibole and interstitial quartz sporadically occur in the plagioclase groundmass. Plagioclase is typically unaltered and undeformed allowing determination of plagioclase composition: An 53, (labradorite) based on 6 measurements. The host for mineralization at both the MS Gabbro area and the SP Gabbro area is websterite that may have a feldspathic component (plagioclase-bearing websterite). One sample of websterite containes biotite as large sheet-like flakes which replace augite and are spatially associated with pyrrhotite grains. The country rock pyroxene diorite (MS Gabbro area) is petrographically characterized as a hornblende-hypersthene diorite. Hypersthene forms relatively small rounded, anhedral grains averaging 0.2mm but ranging up to 0.6mm, which are commonly surrounded by inclusion-rich plagioclase. Large poikioblastic crystals of green hornblende replace hypersthene and plagioclase and are up to 2.1mm in length, which give the slight porphyritic appearance to the rock. Plagioclase is about the same size range as the early hypersthene grains. Hypersthene and plagioclase form a tight interlocking mosaic. Average plagioclase composition is about An54.



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GEOPHYSICS Magnetic Survey A GEM Systems, Inc., GSM-19 v. 7.0 portable high-sensitivity Overhauser effect magnetometer designed for hand-held use was used as a mobile /walkmag instrument. This instrument was used in conjunction with a GEM Systems, Inc., GSM-19 v. 5.0 magnetometer that collected base station total magnetic field intensity readings. Survey signal quality of the mobile/walkmag unit was monitored during the survey and any poor signal readings were repeated until a quality signal was obtained. Readings of the earth’s total magnetic field were taken every 7.5 meters intervals along grid lines with an approximately 20 meter separation on the MS Area grid (see Figures 8 and 9) with the GSM-19 v.7.0 mobile/walkmag magnetometer. The diurnal variation was monitored in the field by a base station (GSM-19 v. 5.0) at a common site, located at 604143 E and 5477732 N (UTM NAD 83 Zone 10). With the Big Nic Walkmag Survey readings were taken continuously from UTM 604465 E and 5477774 N (UTM NAD 83 Zone 10) to UTM 602612 E and 5477710 N and tied into waypoints along the road (see Figures 12 and 13) The diurnal variation was monitored in the field by a base station at a common site, located at 604143 E and 5477732 N (UTM NAD 83 Zone 10). To facilitate this, the surveying unit was initialized with the base station at a common site, located at 604143 E and 5477732 N (UTM NAD 83 Zone 10). The surveying unit (mobile/walkmag) was initialized with the base station unit at the beginning of the surveying, so that each of the units had the exact same time. In addition, readings were taken with the mobile/walkmag magnetometer at the base station site at the end of each day of surveying. Magnetic Survey Data Handling The mobile/walkmag (surveying unit) magnetometer magnetic data was dumped into a computer with the surveying unit interconnected with the base station unit thus enabling the magnetic data to be automatically corrected for diurnal variation. Then, using Geosoft software, the data were reduced, plotted, and contoured onto plan maps (Figure 9 and Figure 13 respectively) for the MS grid and Big Nic Road Walkmag.



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FIGURE 7 NTS TRIM MAP 092H/043 INDEX MAP FOR GEOLOGICAL AND MAGNETOMETER SURVEY MAPS M.McCLAREN, P.Geo., February 2007 Contour Interval = 20 meters



36

80N 60N 40N 20N 0N FIGURE 8 MS GABBRO AREA MAGNETOMETER SURVEY LOCATIONS M.McCLAREN, P.Geo., February 2007



37

Line 0N 0E - 285E

285285277.5

270

262.5

255

247.5

240232.5225217.5210202.5195187.5180180172.5165157.5150142.5135127.5

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22.5157.5

00

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55900

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80N 60N 40N 20N 0N CONTOUR PLAN MAP OF MS GABBRO AREA MAGNETOMETER SURVEY FIGURE 9 PROFILE OF LINE 0N 0E TO 285E Corrected Total Magnetic Intensity



38

FIGURE 10 FIGURE 11 GEOLOGICAL MAP OF MS GABBRO AREA Contour Interval = 20 meters Scale 1:2000 LEGEND M.McClaren, P.Geo. February 2007



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PLATE 19 Contact between altered pyroxene diorite and hornblende pyroxenite dike. (MFD; Figure 11). Note enclaves of hornblende pyroxenite in hornblendized pyroxene diorite.



40

INTERPRETATION OF MAGNETOMETER SURVEY AND MINERALIZATION – MS GABBRO AREA A number of rubble massive sulphide mineralization localities have been found on the northern portion of the north central Big Nic Property. Three locations of mineralizated rubble have been found to be associated exposures of gabboic dikes (MS Gabbro; SP Gabbro and EN Gabbro). The MS Gabbro is a northwesterly striking intrusion located in an area of parasitic folds formed on the western flank of a north northwesterly striking F3 antiform. Rubble mineralization found in the MS area consists of pyrrhotite, chalcopyrite and pentlandite as massive sulphides with ragged and altered pyroxene inclusions. The analysis of 18 samples from the MS Gabbro Area gave an average of 0.52% Ni; 1.71% Cu and 0.064% Co (M.McClaren, 2006). The pyrrhotite content of the massive sulphides is up to 80% of the sulphide content and the massive sulphides have a high magnetic susceptibility. A magnetic high feature that trends north 45 degrees east and is approximately 30 meters in length and up to 25 meters in width, occurs at the southern boundary of the MS Gabbro. The nature of the magnetic feature suggests that it is a vertical to subvertical body (S.Rastad,2006; personal communication). The highest magnetic response occurs at UTM co-ordinates 603703 E and 5477725 N where it is believed that massive sulphide mineralization subcrops on a logging road. Additional magnetic high features that lie along a northeasterly trend may represent additional mineralized bodies with a high pyrrhotite content. The sulphide mineralization found in the northern portion of the Big Nic Property is an injection style of mineralization that is characterized by the dominance of massive sulphides and 2 - 5% gangue minerals. A generalized metallogenic model for this type of deposit is as follows:

(a) Nickel bearing magmas go through a stage of liquation and fractional crystallization and differentiation in the progenitive magma chamber

(b) Silicate magma; sulphide-rich magma and sulphide magma are formed and

(c) These magmas may separate through time to form a variety of orogenic magmatic deposit types.

(d) These magmas can be captured from the progenetive intrusive during an energetic triggering event (e.g. tectonic squeezing, seismic pumping, the development of dilational structures related to major faults and/or injection of new magma into progenitive magma chamber) and injected into accommodating structures.

(Papunen, H, 2003; Tornos, F. et al.; 2006; Wang, C.Y. and Zhou, M-F.; 2006; and Zhongli,T, Duanjin, R.,Zengrui, X.,Yaokai, M.;1992).



41

FIGURE 12 Contour Interval = 20 meters LOCATION OF BIG NIC WALKMAG SURVEY M.McClaren, P.Geo. February 2007



42

FIGURE 13 CONTOUR PLAN OF BIG NIC WALKMAG ROAD SURVEY Corrected Total Magnetic Intensity



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Scale 1: 6500 FIGURE 14 Contour Interval = 20 meters GEOLOGY AND BIG NIC ROAD WALKMAG NORTH CENTRAL BIG NIC PROPERTY LEGEND M.McClaren, P.Geo. February 2007



44

DISCUSSION OF BIG NIC ROAD WALKMAG The Big Nic Road Walkmag located an area of anomalous total field magnetic intensity at 0N 3W (UTM 603224E and 5477562N). This magnetic feature is located in an area of granofelsic pyroxene diorite that is cut by altered pyroxenite veinlets and minor sulphide mineralization is found on fractures of altered pyroxene diorite (SULFRAC). Prospecting in conjunction with further magnetometer and geological work should be undertaken to assess the sulphide mineral potential of this area.



45

CONCLUSIONS AND RECOMMENDATIONS The North Central portion of the Big Nic Property is predominately underlain by. pyroxene diorite, hornblende diorite and to a lesser extent tonalite of the Spuzzum Pluton. The northernmost part of the pluton is overprinted by solid-state foliation and an upright, shear disrupted fold is recognized on the northern boundary of the Big Nic Property. The structural development of the east Harrison Lake area includes a period of Cretaceous (>96 Ma to locally 73 Ma) SW-NE contraction. During this period of transcompression a set of extensional structures was developed. These structures trend North 30 to 55 degrees East ; North 30 to 70 degrees West; North 10 degrees East and West 20 North. Both exposed and unexposed mafic-ultramafic intrusives were emplaced into these extensional structures. Areas of mafic-ultramafic intrusives can be recognized by a high total magnetic intensity and a variety of lithological features associated with their host lithologies. In hornblende diorites these features include mafic enclaves; mafic schilieren and mafic filled fractures. In pyroxene diorites the features associated with mafic-ultramafic intrusives include the development of granofels (a medium grained; equigranular rock lacking foliation or lineation and is believed to be the result of mafic-ultramafic intrusive thermal action on pyroxene diorite) and the intrusion of gabbroic and hornblende pyroxenite dikes. The MS Gabbro area consists of a melanocratic hornblende gabbro intrusion that is mingled with hornblende pyroxenite. Pyroxenite intrudes hypersthene diorite country rocks. The hypersthene diorites have been overprinted by solid-state foliation and upright antiformal folds and associated parasitic folds are found associated with the diorites in the MS Gabbro area. In an area approximately 75 meters to the east of the MS Gabbro, hypersthene diorites have been altered to a granofels that is cut by veins of altered (cummingtonite ?) pyroxenite. Rubble massive sulphide mineralization has been found along a decommissioned logging road that cuts the MS Gabbro. The sulphide mineralization is massive and consists of pyrrhotite (up to 80%); chalcopyrite and pentlandite with ragged and altered pyroxene crystals as gangue constituents (2-5%). Pyrrhotite content of the massive sulphides is up to 80% of the sulphide content and the massive sulphides have a high magnetic susceptibility. A magnetometer survey conducted over the MS Gabbro area located a magnetic high feature approximately 30 meters in length and up to 25 meters in width at UTM co-ordinates 603703 E and 5477725 N and it is believed to be the source area of the rubble mineralization. Lower strength magnetic high features that trend N 45 degrees E from the MS Gabbro magnetic high feature have a strike length of approximately 40 meters and may represent additional areas of sulphide mineralization. It is recommended that aseries of drill holes be located to test the MS Gabbro magnetic feature and the lower strength magnetic features. During the 2006 field season two new areas of massive sulphide rubble were located (MS-8 and MS-9). MS-8 is located approximately 175 meters southeast



46

of the MS Gabbro southern boundary and consists of angular rubble of gabbro and massive sulphides of a similar character as those found at the MS Gabbro area. MS-9 is located at UTM co-ordinates 604270E and 5477662N (approximately 130 meters south of EN Gabbro). Mineralized rubble similar in character to the MS Gabbro mineralization is found at this location. It is recommended that a grid be established and a magnetometer survey conducted over the MS-8 and MS-9 areas. The Big Nic Road Walkmag located a magnetic high feature at UTM co-ordinates 603224E and 5477562N in an area of granofelsic pyroxene diorite cut by pyroxenite veinlets and sulfide filled fractures. It is recommended that a grid be established in this area and a magnetometer survey be conducted. Further prospecting in conjunction with geological mapping in this area is warranted. Mineralization found on the north central portion of the Big Nic property is thought to be an injection style orogenic magmatic deposit type. Prospecting in conjunction with geological mapping and silt geochemistry is warranted for the area of Locality 8 (UTM 600686E and 5473515N) and in the area of waypoint 001 (UTM 603054E and 5473296N). Mafic-ultramafic lithologies were located at both of these locations and in the case of the area of Locality 8 total magnetic intensity highs are located to the northwest.



47

BIBLIOGRAPHY Aeroquest Limited, (2005): Report on a Helicopter Borne AeroTEM II Electromagnetic and Magnetic Survey, Big Nic Project, Hope Area, British Columbia, 092H/05,06, Private Report for Pacific Coast Nickel Corp., pp 1-19, 3 maps. Barbarin, B., (2005): Mafic magmatic enclaves and mafic rocks associated with the Sierra Nevada batholith, California, nature, origin and relations with the hosts, Lithos, Vol. 80, pp.155-177. Bartholomew, P.R., (1979): Geology and Metamorphism of the Yale Creek Area, British Columbia, Unpublished M.Sc.Thesis, University of British Columbia. Brown, E.H. and Talbot, J.L., (1969): Orogen-Parallel Extension in the North Cascades Crystalline Core, Washington, Tectonics, Vol. 8, No.6, pp. 1105-1114. Brown, E.H., Talbot, J.L., McClelland, W.C., Feltman, J.A., Lappen, T.J., Bennett, J.D., Hettinga, M.A., Alvarez, K.M., Calvert, A.T., (2000): Interplay of plutonism and regional deformation in an obliquely convergent arc, southern Coast Belt, British Columbia, Tectonics, Vol. 19, No.3, pp. 493-511. Carreras, J., Druguet, E., Griera, A., (2005): Shear zone-related folds, Journal of Structural Geology, Vol. 27, 1229-1251. Charon,D., Anronicos, C.L. and Hollister, L.S., (1999): Large-scale transpressive shear zone patterns and displacements within magmatic arcs: the Coast Plutonic Complex, British Columbia, Tectonics, Vol. 18, No.2, pp 278-292. Clarke, W.E. (1969): Giant Mascot Mines Ltd., Geology and Ore Control; Western Miner, Volume 42, pages 40-46. Cobbold, P.R., (1976): Fold Shapes as Functions of Progressive Strain, Philosophical Trans. of Royal Society of London. Section A, Vol. 283, p.129-138. Diego, P., Giampiero, P., (2000): Chaotic dynamics and fractals in magmatic interaction processes: a different approach to the interpretation of mafic microgranular enclaves, Earth and Planetary Science Letters, Vol. 175, pp. 93-103. Journeay, J.M. and Friedman, R.M. (1993): The Coast Belt thrust system; evidence of Late Cretaceous shortening in southwest British Columbia; Tectonics, 12, pp. 756-775.



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Hettinga, M.A., (1989): Metamorphic Petrology, Geothermobarometry and Structural Analysis of a Portion of the area East of Harrison Lake, B.C., Unpublished M.Sc. Thesis, Western Washington University, Washington State. Jones, R.R., Holdsworth, R.E., Clegg, P., McCaffrey, K., Tarvarnelli, E., (2004): Inclined transpression, Journal of Structural Geology, Vol. 26, pp. 1531-1548. Lowes, B.E., (1972): Metamorphic Petrology and Structural Geology of the area East of Harrison Lake, B.C., Unpublished Ph.D Thesis, University of Washington, Washington State. McClaren, M. (2006): Big Nic and Emory Creek Project, Private Report for Pacific Coast Nickel Corp. McClaren, M. (2005): Report on a Helicopter-Borne AeroTEM© II Electromagnetic and Magnetic Survey On the Emory Creek Property, New Westminster Mining Division; British Columbia Ministry of Energy and Mines, Geological Survey Branch, Assessment Report # 28019. Miller, R.B., Patterson, S.R., Hermann, L., Alseben, H., Luneburg, C., (2006): Significance of composite lineations in the mid-deep crust, a case study from the North Cascades, Washington, Journal of Structural Geology, Vol. 28, pp 302-322. Morton, W.J. (2005): Draft Summary Report on the Big Nic Property, New Westminster Mining Division, British Columbia with Recommendations for Exploration, Mincord Exploration Consultants Ltd., December 9th, 2005; Private Report for Pacific Coast Nickel Corp., pp. 38. Orteiga, L., Lunar, R., Pina, R., Gervillla, F., Alapieti, T., Marinez, T., (2006): Petrology and Geochemistry of Mafic-Ultramafic Fragments from the Aguablanca Ni-Cu Ore Breccia, Southwest Spain, Economic Geology, Vol. 101, No. 4., pp. 865-881. Paterson, S.R., Miller, R.B., Alseben, H., Whitney, D.L., Valley, P.M., Hurlow, H., (2004): Driving mechanisms for >40 km of exhumation during during contraction and extension in a continental arc, Cascades Core, Washington, Tectonics, Vol. 23, 30 pages. Papunen, H,(2003): Ni-Cu sulfide deposits in mafic-ultramafic orogenic intrusions- Examples from the Svecofennian area, Finland, Mineral Exploration and Sustainable Development, Elipoulos et al. (eds). Peltonen, P,(1995): Magma-country rock interaction and the genesis of Ni-Cu deposits in the Vammala Nickel Belt, SW Finland, Mineralogy and Petrology, Vol. 52, pp. 1-24.



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Pinsent, R.M.( 2001): Ni-Cu-PGE Potential of the Giant Mascot and Cogburn Creek Ultramafic-Mafic Bodies, Harrison –Hope Area, Southwestern British Columbia (092H);Geological Survey Branch, Geological Fieldwork 2001, Paper 2002-1. Rastad, S., (Sept. 2006); SJV Consulting Ltd., personal communication. Regional Geochemistry Survey, (1981); NGR stream sediments and waters, NTS 92H, Hope, British Columbia. Richards, T.A. and McTaggart, K.C.(1976): Granitic rocks of the southern Coast Plutonic Complex and northern Cascades of British Columbia; Geological Society of America Bulletin, V. 87, pp. 935-953, June 1976. Tornos, F., Galindo, C., Casquet, C., Pevida, L.R., Martinez, C., Martinez, E.,Velasco, F., Iriondo, A., (2006): The Aguablanca Ni-(Cu) sulfide deposit, SW Spain,: Geological and Geochemical Controls and the relationship with a mid-crustal layered mafic complex, Mineralium Deposita, Vol. 41, pp. 737-769. Travis, A.(2002): Assessment Report Undertaken on the Emory Creek Property, Report for Santoy Resources Ltd., New Westminster Mining Division; British Columbia Ministry of Energy and Mines, Geological Survey Branch Assessment Report #26876. Umhoefer, P.J. and Miller, R.B. (1996):Mid-Cretaceous thrusting in the southern Coast Belt, British Columbia and Washington, after strike-slip fault reconstruction, Tectonics, Vol. 15, No.2, pp. 545-565. Vining, M.R.(1977): The Spuzzum Pluton, Northwest of Hope, B.C.; Unpublished MSc Thesis, The University of British Columbia, 147 pages, plus map. Wang, C.Y. and Zhou, M-F (2006): Genesis of the Permian Baimazhai magmatic Ni–Cu–(PGE) sulfide deposit, Yunnan, SW China, Mineralium Deposita, Vol. 41, pp.771-77 Zhongli, T., Duanjin, R., Zengrui, X., Yaokai, M., (1992): Nickel Deposits of China: in Mineral Deposits of China, Vol. 2,., Geological Publishing House, Bejing, China, Nailong, L. (editor).



50

APPENDIX 1 STATEMENT OF EXPENDITURES M,McClaren P.Geo June 22 to July 28, 2006 10 days @ $350/day $3500.00 August 26 to Sept 23, 2006 14days @ $350/day $4900.00 4days $450/day $1800.00 D. Cardinal P.Geo June 22 to July 28, 2006 3 days @ $350/day $1050.00 August 26 to Sept 23, 2006 18 days @350/day $6300.00 D. Kay August 26 to Sept. 23, 2006 12 days @ $200/day $2400.00 SJ Geophysics Ltd. Sept. 8 to Sept 10, 2006 Senior Geophysicist plus Assistant $3,156.53 Equipment Rental Valley Helicopters June 30th 2006 $4,617.05 S.J. Geophysics Ltd. Magnetometer Rental $1800.00 Truck 24 days @ $85/day $2040.00 Gas and accessories $1725.53 Accomodation $2040.00 Meals $960.00 Report Costs Maps and Reproductions $204.41 S.J.V. Consultants Ltd. Magnetics Processing $686.00 Report and map preparation, compilation and research M.McClaren P.Geo. 7 days @ $450/day $3339.00

TOTAL $40,518.52



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APPENDIX 2 GMS-19 V.7.0 INSTRUMENT DESCRIPTION



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59

HOMEGOLD RESOURCES LTD. Unit 5 – 2330 Tyner Street, Port Coquitlam, B.C., V3C 2Z1

-- PETROGRAPHIC DESCRIPTION --

FOR: Pacific Coast Nickel, Big Nic Project, Harrison Lake Area

MS Gabbro massive sulphides HANDSPECIMEN DESCRIPTION: Large handspecimen, massive sulfides, mainly pyrrhotite, chalcopyrite and approximately 25% silicates, approximately 5% chalcopyrite closely associated with pyrrhotite, one grain of graphite (?) 2mm in length in handspecimen only, medium grained with average grain size between 1 to 2mm., abundant vugs, silicates are characteristically rounded, the feldspar zones contain traces of potassium feldspar, one cross-cutting calcite hairline, some of the silicate minerals are sub-porphyritic. HANDSPECIMEN NAME: Chalcopyrite-bearing Massive Pyrrhotite

THINSECTION EXAMINATION:

ESTIMATED MODE: Pyrrhotite 65% Chalcopyrite 5% Pyrite 2% Graphite (?) trace in Handspecimen Calcite 2% Biotite 1% Enstatite 13% Augite 6% Chlorite 2% Brown Hornblende 1% Plagioclase trace Cavities (filled with epoxy) 5%

The silicate minerals are well rounded and embayed by the enclosing pyrrhotite. The main silicate mineral is the orthopyroxene enstatite. Small biotite flakes occur on the edges of the larger enstatite grains often associated with biotite. Minor calcite forms narrow irregular veinlets up to 0.15mm wide. Augite forms large poikioblastic porphyroblastic grains Traces of dark brown chlorite and traces of brownish hornblende replacing enstatite. Poikioblastic augite forms the large cleavage traces noted in handspecimen. Plagioclase forms small interstitial grains replaced by a net texture of chlorite. Pyrrhotite is mainly relatively uniform and there is trace amounts of exsolution lamellae which could be pentlandite.



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Chalcopyrite is anhedral and forms large, crudely aligned lenses which contain abundant small angular to feathery gangue inclusions, chalcopyrite lenses also contain minor subhedral pyrite crystals up to 0.18mm on a side. ROCK NAME: Chalcopyrite-bearing Massive Pyrrhotite



61

-- PETROGRAPHIC DESCRIPTION -- FOR: Pacific Coast Nickel, Big Nic Project, Harrison Lake Area

MS Gabbro Area HANDSPECIMEN DESCRIPTION: Abundant chalcopyrite in disseminations and small lenses, chalcopyrite mainly confined to the mafic areas or rimming mafics, network of pyroxene anhedral grains separated by anhedral to subhedral plagioclase, strongly magnetic, no potassium feldspar content. HANDSPECIMEN NAME: Chalcopyrite-bearing Feldspathic Pyroxenite


ESTIMATED MODE: Plagioclase 46% Enstatite 24% Cavities 2% Biotite 8% Hornblende 8% Chalcopyrite 6% Magnetite 5% Pyrite trace

Plagioclase occurs as large, unaltered crystals over 3mm in length but also as small rounded grains in an interlocking mosaic. Enstatite forms a network of smaller anhedral grains. Average Plagioclase composition is about An48 with minor variation Biotite flakes are closely associated with the chalcopyrite lenses and irregular grains. Chalcopyrite forms individual grains 0.05mm in diameter which commonly coalesce into large lenses. Magnetite less commonly forms composite grains with chalcopyrite. Magnetite occurs as smooth rounded grains separate but often in close proximity to chalcopyrite. Magnetite will also form elongate grains up to 0.6mm in length along fractures at the boundary between plagioclase and enstatite. Pyrite is rare, mainly occurring as small grains with magnetite ROCK NAME: Altered Chalcopyrite-Magnetite-bearing Feldspathic Pyroxenite (Norite)



62


MS Gabbro Area HANDSPECIMEN DESCRIPTION: Chalcopyrite rimming mafic minerals and disseminated throughout associated, mainly melanocratic, fine to medium crystalline pyroxene, very large euhedral greater than 8mm crystals of brownish plagioclase, some broken plagioclase crystals. HANDSPECIMEN NAME: Chalcopyrite-bearing Feldspathic Pyroxenite


ESTIMATED MODE: Enstatite 48% Augite 9% Plagioclase 24% Chalcopyrite 2% Pyrrhotite 4% Magnetite trace Pyrite trace Cavities 5% Biotite 2% Cavities 6%

Augite forms an interlocking mosaic of large poikioblastic crystals. Cavities occur in the cores of some enstatite, radial fractures common around larger core cavities. Cavities also occur along microfractures and cleavage, traces in pyroxene. Plagioclase largely unaltered, polysynthetic twinning commonly bent at grain edges. Enstatite occurs as small anhedral grains throughout. Average plagioclase composition is about An48. Chalcopyrite forming elongate lenses along the edges of large plagioclase crystals and interstitial to the small anhedral enstatite grains. Chalcopyrite often is closely associated with pyrrhotite forming smooth composite grain boundaries. *Minor chalcopyrite is found along microfractures/twin boundaries and irregular replacements within the plagioclase laths. Minor subhedral magnetite is present in straight line contact with larger grains of chalcopyrite. Chalcopyrite is also in contact with traces of pyrite. There are trace amounts of 0.02mm wide “layers” of biotite between chalcopyrite/pyrrhotite grains and the adjacent enstatite or plagioclase crystals (21.5x62.4). ROCK NAME: Chalcopyrite-bearing Feldspathic Pyroxenite (Plagioclase-bearing Websterite)



63


MS Gabbro Area HANDSPECIMEN DESCRIPTION: Lighter grey dominant, plagioclase is relatively anhedral and fine grained, dark mafic-rich “fragment” on one side of off-cut, speckled appearance due to rounded hornblende/pyroxene up to 1.5mm diameter, non-magnetic HANDSPECIMEN NAME: Quartz Feldspar “Diorite”


ESTIMATED MODE: Hypersthene 32% Plagioclase 42% Biotite 4% Hornblende 14 Augite 6% Pyrite <1% Magnetite <1% Iron Oxides trace

Hypersthene forms relatively small rounded, anhedral grains averaging 0.2mm but ranging up to 0.6mm, which are commonly surrounded by inclusion-rich plagioclase. Slightly pleochroic. Large poikioblastic crystals of green hornblende replace hypersthene and plagioclase and are up to 2.1mm in length, which give the slight porphyritic appearance to the rock. Plagioclase is about the same size range as the early hypersthene grains. Hypersthene and plagioclase form a tight interlocking mosaic. Average plagioclase composition is about An54. Trace amounts of pyrite occur as small grains less than 0.04mm in diameter mainly disseminated within the plagioclase. Magnetite also is observed as slightly larger smooth rounded grains up to 0.1mm within and along the edges of augite crystals. Minor black non-reflecting material in one part of the slide – probably iron oxides. ROCK NAME: Hornblende-Hypersthene Diorite (Hypersthene Diorite or Pyroxene Diorite)



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MS Gabbro Area HANDSPECIMEN DESCRIPTION: Melanocratic, hypidiomorphic granular, medium to coarse crystalline, disseminated pyrrhotite and minor chalcopyrite throughout, some apple green chlorite in places, minor interstitial quartz, main mineral black enstatite (pyroxene) in euhedral crystals up to 4mm in length. HANDSPECIMEN NAME: Pyrrhotite and Chalcopyrite-bearing Chloritized Pyroxenite


ESTIMATED MODE: Pyrrhotite 6% Chalcopyrite 1% Enstatite 28% Augite 48% Biotite (stilpnomelene) 7% Quartz 2% Plagioclase 4% Muscovite 2% Iron Oxides 2%

Enstatite forms small anhedral grains, minor quartz occupies an interstitial position associated with similar interstitial plagioclase. Augite occurs as poikioblastic large crystals. Biotite forms large sheet-like flakes which replace augite and are spatially associated with pyrrhotite grains (could be stilpnomelene). Pyrrhotite forms smooth round grains up to 0.1mm in diameter within poikioblastic enstatite. The largest pyrrhotite lens is 0.3mm long. Occasionally there are similar to slightly larger grains of magnetite. Pyrrhotite forms large lenses over several mm in length between augite grains. Chalcopyrite forms small discrete grains often contained with the poikioblastic grains of augite. Larger chalcopyrite grains are associated with the large biotite flakes. ROCK NAME: Pyrrhotite and Chalcopyrite-bearing Biotitized Pyroxenite (Websterite)



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MS Gabbro Area HANDSPECIMEN DESCRIPTION: Melanocratic, hypidiomorphic granular, medium to coarse crystalline, pyroxene euhedral crystals up to 4mm in length, non-magnetic, no potassium feldspar content, apple green chlorite throughout, disseminate minor pyrrhotite, minor plagioclase in small areas, anhedral clinopyroxene, golden coloured weathering on broken face. HANDSPECIMEN NAME: Pyroxenite


ESTIMATED MODE: Augite 46% Enstatite 18% Hornblende 5% Pyrrhotite 4% Chalcopyrite 2% Magnetite 2% Biotite (stilpnomalene) 11% Plagioclase 6% Iron Oxides 2%

Enstatite occurs as anhedral relatively small rounded grains. Augite is much more abundant as porphyritic poikioblastic crystals which are randomly oriented. Plagioclase forms interstitial grains and relatively clear unaltered grains. Some of the plagioclase contains no twinning suggesting that some minor quartz may be present in small amounts. Hornblende occurs as replacing augite and biotite appears to be late-stage replacing the rims of the poikioblastic augite with smooth embayments and cleavage cracks. Rarely biotite forms larger clear sheets up to 0.35mm across. Pyrrhotite forms small, up to 0.2mm, regular straight and irregular lenses sided grains often along the edges of enstatite grains. Chalcopyrite occurs as roughly rectangular isolated grains up to 0.1mm. Occasionally, pyrrhotite grains have small zones of chalcopyrite and traces of exsolution lamellae (pentlandite?). Magnetite is associated with biotite. ROCK NAME: Porphyritic, Slightly Feldspathic Pyroxenite (Plagioclase-bearing Websterite)



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Sample: MS GABBRO AREA

LITHOLOGY: Gabbro ALTERATION TYPE: ? Hornblende Hand Sample Description: Composed of approx. 60% black mafic and 40% creamy felsic minerals with mafic

minerals occurring in anastomosing masses. Contains fine-grained disseminated black

magnetite (magnetic), no reaction with dilute HCl, no stain with sodium cobaltinitrite (no

K-feldspar).

Thin Section Description: The sample is characterized by an anastomosing network of masses of fine amphibole in a fine to medium-grained groundmass of plagioclase. Magnetite and rare sheaves of biotite occur associated with amphibole and interstitial quartz sporadically occur in the plagioclase groundmass. Plagioclase is typically unaltered and undeformed allowing determination of plagioclase composition: An 53, (labradorite) based on 6 measurements

MAJOR MINERALS

Mineral % Distribution & Characteristics Optical

Hornblende 50 Fine anhedral to hexagonal grains, commonly displaying 124º cleavage intersection and sporadically associated with biotite

Pleochroic

pale to dark

green

Plagioclase 45 Fine to medium-sized anhedral to tabular grains with polysynthetic twinning, forming a granular assemblage. Incipient deformation and alteration. Maximum extinction angles in plagioclase reaches 29.5º (based on 6 measurements using the Michel Levy method) suggesting an anorthite content of approx. 53º



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MINOR MINERALS


Magnetite / ilmenite 01 Fine to very fine anhedral magnetite grains typically within masses of amphibole and rarely associated with ilmenite

Unknown tr-01 Very fine stubby grains disseminated, typically associated with masses of amphibole ?high relief, zoned from core to rim, pleochroic pink to purple, ?apatite

Biotite tr Approx. 5 fine elongated grains disseminated within masses of amphibole or within the plagioclase groundmass

Quartz tr Fine anhedral interstitial grains



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A

B

03 - A: A & B) Representative view of the sample, showing a fresh, virtually unaltered assemblage of plagioclase and hornblende. A) PPL, B) XPL, FOV = ~ 8.5 mm.



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Sample: SP GABBRO AREA

LITHOLOGY: Websterite ALTERATION TYPE: Weak chlorite, sericite, carbonate Hand Sample Description: Medium-grained, equigranular mafic sample containing euhedral mafic grains and cut by

very thin winding and oxidized fractures. Weakly magnetic, no reaction with dilute HCl,

no stain with sodium cobaltinitrite (no K-feldspar).

Thin Section Description:

A granular assemblage of fine to medium-grained orthopyroxene and lesser clinopyroxene forms the sample. Sporadic interstitial grains of quartz occur as well as masses of biotite, commonly altered to chlorite and enclosing fine pyroxenes. Interstitial clusters of fine sericite ± carbonate ± serpentine are disseminated locally and additionally fill pyroxene cracks and open boundaries. Magnetite is disseminated and trace pyrite and chalcopyrite was observed. Several thin cracks cut the sample, lined by Fe-oxides / hydroxides. MAJOR MINERALS


Orthopyroxene 70 Fine- to medium-grained, anhedral to tabular, cracked, commonly lamellar with blebs of biotite and chlorite. Forms the sample groundmass

low δ colors,

Clinopyroxene 15 Fine- to medium-grained, lamellar, anhedral to subhedral, cracked.

Oblique

extinction

MINOR MINERALS


Hornblende 03 Fine to medium-sized masses interstitial to pyroxenes with the larger fraction commonly enclosing fine pyroxenes. Also as fine blebs within pyroxenes. Likely after biotite

Brownish,

pleochroic,

124º cleavage

?Sericite 02 Extremely fine-grained clusters and very fine sheaves altering pyroxenes along fractures and grain boundaries

Plagioclase 01 Fine interstitial grains

Biotite tr-01 Rare fine interstitial masses, commonly enclosing pyroxenes Birds eye

Carbonate tr-01 Fine-grained masses with sericite, replacing pyroxenes Magnetite / Ilmenite tr-01 Very fine anhedral grains of variously intermixed magnetite /

ilmenite

Fe-oxides / hydroxides

tr-01 Very thin veinlets throughout

?Serpentine tr Very fine stylolitic ribbons within pyroxenes Quartz tr Few fine interstitial grains Pyrite tr On very fine mass associated with chalcopyrite Chalcopyrite tr Very fine grains, with pyrite or as inclusions in magnetite



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APPENDIX 4

PACIFIC COAST NICKEL SYNDICATE (OWNER) BIG NIC PROPERTY

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