Assessment Report for the ILOGNO: AUG 2 5 1994d RD. ' 1 MONS Claim Group
Golden Mining Division N.T.S.82 NA4E I- Latitude 5 1O 49' 27" N, Longitude 1 17' 0OrF3f3f! NO: -- I for
I Gwen Resources Ltd. 1595 Grifiths Place Kelowna, B.C. V1Z 2T7
Submitted by:
Richard T. Walker, P.Geo.
of
Gemquest Geological 1916 - 5th Street South Cranbrook, B.C. VlC 1K4
Submitted: August 17,1994
GEOLOGBCAL ASSESSMENT Table of Contents I Page
Summary 1 Introduction 2 Diamond Exploration Potential .3 Location and Access 4 Claim Status 8 Physiography and Climate 10 Regional Geology 12 History 14 Local Geology 16 1993 - 94 Program 17 Results 18 Discussion 20 Conclusions and Recommendations 22 Proposed Budget 24 References 25 I I List of Figures
I; Page Figure 1 - General Location Map 5 Figure 2 - Location of RepresentativeBreccia Diatremes I in the southern Rocky Mountains 6 Figure 3 - Location Map of Diatreme Occurrences of 7 I the Golden Cluster Figure 4 - Claim Location Map 9 I Figure 5 - Property Geology Map 11 I 1 List of Tables
I Table 1 - Representative Trace Element Content 19 I I
I List of Appendices Appendix A - Statements of Qualifications I Appendix B - Claim Records Appendix C - Analytical Results Appendix D - Statement of Expenditures I Appendix E - Program Related Documents I I 1 I 1 I SUMMARY
Alkaline intrusive diatremes, dykes and sills have been examined and documented in the southern I; Rocky Mountain Alkaline Belt (RMAJ3) of British Columbia, extending from Fernie to northeast of Golden. Documented lithologies include olivine melilites, limburgites, alkaline to basaltic lamprophyres, kimberlites and diamond-bearing lamproites. The Cross kimberlite is a Perm+ Triassic intrusive breccia located north of Elkford on the southeastern edge of a broadly defined north-trending belt of alkaline diatremes. The Joff Pipe is located on the western edge of this same belt east of invermere and is considered to be either a kimberlite or an olivine melilite. The northern portion of this belt is located in the area west of the Columbia Icefields and consists of diamond-bearing lamproites. Of particular significance regarding this program is the presence of diamond-bearing lamproites in a mobile belt.
The Mons Claim Group was acquired by staking in May, 1993 and consists of 24 2-post claim I units which overlie at least five reported ultrapotassic occurrences of lamprophyric and / or lamproitic affinity. The claims are located between the diamond-bearing Jack and Mark claims of Dia Met Minerals Ltd. The alkaline lithologies identified on the claims by independent sources are I interpreted as olivine - pyroxene - phlogopite f sanidine f amphibole Iamproite breccia or alkaline biotite camptonite (lamprophyre). Abundant indicator minerals have been recovered from diatremes in this area, including pyrope garnets, G5 (eclogitic and / or primitive mantle source) I garnet, high chrome diopside, high chrome (diamond inclusion field) chromites and picroilmenites. In addition, one microdiamond has been recovered from each of the Jack and Mark claims and 10 I microdiamond fragments were also identified from samples taken on the Jack claims. The objective of the 1993 program was to identify potential diamond-bearing properties in the Rocky Mountains and secure the ground by staking in order that a more in-depth examination may I be carried out in the future. A cursory geological examination was made of the property, With limited prospecting and sampling carried out. Sampling included one 53.3 kg sample of diatreme material for heavy mineral separation and several thin sections for description and 1ithologic;al I identification.
I I 2 I INTRODUCTION
Diatremes in the southern Canadian Cordillera are interpreted to have been intruded predominantly I; in the early Paleozoic yet contain zircon xenocrysts of Archean to early Paleozoic age. Crustal- type xenoliths are documented from many of the pipes (eg. Blackfoot, Summer, Cross and HP) as well as mantle-derived xenoliths such as pyroxenites, peridotites and eclogites. In addition to I abundant indicator minerals, at least twelve microdiamonds have been reported and five recovered fiom heavy mineral separates fiom the Jack and Mark diatreme occurrences northeast of Golden.
I Although these diatremes are contained within a Paleozoic mobile belt, recent geophysical programs have identified underlying Proterozoic and Archean basement. More significant is I recent identification of a large composite block of Archean craton, part of the Hearn Province, in southern Alberta which projects into eastern British Columbia (Ross et ai. 1991). 1 The basement of the Alberta Basin has recently been correlated to stratigraphic and / or structural provinces identified in the Canadian Shield using U - Pb age determinations of basement exposures from drill core and aeromagnetic signatures (Ross 1991, Ross et al. 1991, Hoffinan 1988). Exposures of basement gneisses in the southern Cordillera coupled with numerous other studies (Le. Lithoprobe deep reflection seismic studies, geochronological and isotopic studies, aeromagnetic, gravity and seismic refraction studies) demonstrate the presence of l%oterozoic and Archean basement underlying miogeoclinal strata west of the Rocky Mountain Trench. Canadian Shield exposures have been correlated fiom Saskatchewan and northwestern Alberta into the subsurface of Alberta. These "northwest - trending anomalies ... can be traced into the Cordillera and support the interpretation that North American cratonic basement projects westward beneath the Rocky Mountains, Rocky Mountain Trench and eastern part of the PurcelI Anbclinorhm" (Cook et al. 1991). Lithoprobe deep seismic reflection data has "... imaged a regionally extensive, west - facing transition (on the west side of the Monashee Mountains) from thick craton on the east to thin transitional, basinal or oceanic crust on the west ...tt (Cook et al. 1991).
The presence of Proterozoic and Archean basement beneath the Cordillera has been interpreted based on many complimentary lines of evidence. Ross et al. (1991) have correlated gneisses of the Canadian Shield with basement gneisses of the Alberta Basin while others (Armstrong et al. 1991, Manough and Pamsh 1991, Murphy et ai. 1991, Parkinson 1991) have proposed a Canadian Shield origin for basement gneiss exposures in the Canadian Cordillera. Canadian Shield gneisses extend into the subsurface of the Alberta Basin and extend beneath the Cordillera to at least the west edge of the Monashee Mountains, where transitional crust is interpreted to occur.
Therefore, diamonds have been recovered from two alkalic diatremes located in a Paleozoic mobile belt. The mobile belt consists of thrust sheets tectonically emplaced upon Archean and Proterozoic basement. Diatremes of the southern Cordillera appear to have intruded a composite I Archean cratonic block correlated to the Hem Province. One possible interpretation for the source of Archean age zircons recovered from diatremes in the Rocky Mountains is fiom the underlying mantle. It is therefore reasonable to expect the presence of diamonds with mantle- derived peridotitic / eclogitic nodules and zircons of Archean age. 3
Diamond Exploration Potential
Diatreme Occurrences in the Rocky Mountains, in general, have silica deficient compositions, are potassium enriched and have high MgO and TiO, contents. Mineralogically, they contain olivine (partially to completely altered to calcite and / or serpentine), clinopyroxene ( as xenocrysts and / or phenocrysts), orthopyroxene, feldspathoids (including nepheline, melilite, leucite and sodalite) and spinels (chromite). Kimberlite indicator minerals have been found throughout the Rh4AB in many occurrences. One widely recognized kimberlite (Crossing Creek) has been identified and documented while another (Joff - Shatch Mountain) has been identified as both a kimberlite and as an alkaline lamprophyre (olivine melilitite). One true kimberlite and at least twelve dykes of kimberlitic affinity have been documented in the Purcell Mountains and are coeval with the Crossing Creek Occurrence (Pope and Thirlwall 1992). Diatremes, dykes and sills of lamproitic composition have been described at the northern end of the Rocky Mountain Alkaline Belt (RMAB), west of the Columbia Icefields and north of Golden, B.C. Several diamonds have reportedly been recovered from two Occurrences (Jack and Mark claims) although not in economic quantities. However, diamonds have been recovered from ultrapotassic Occurrences in the southern Rocky Mountains, a Paleozoic mobile belt. One true kimberlite and twelve dykes of kimberlitic affinity occur west of Invermere, B.C. in the Purcell Mountains (Pope and Thirlwall 1992). They have been dated at 245 2 2.4 Ma and are therefore coeval with the Cross kimberlite at the southern end of the RMAB (241 2 5 Ma and 249 L 12 Ma, Smith et al. 1988; 244 Ma, Grieve 1982). Dates determined from phlogopite separates for the occurrences at the northern end of the RMAB include: 334 f 7 Ma, 348 * 7 Ma, 391 f 12 Ma and 396 f 12 Ma (Pell 1987). Emplacement ages have been interpreted for other occurrences based on intrusive relationships and three intrusive episodes have been postulated: Ordovician - Silurian, Devonian - Mississippian and Permian - Triassic (Pell 1987). Geochronological evidence determined to date supports these proposed periods of alkaline, ultrapotassic intrusive activity.
The presence of diatremes and dykes having lamproitic composition and / or affinity and abundant kimberlite indicator minerals, located between documented diamond-bearing ultrapotassic intrusive bodies, all of which overlie Archean age basement is sufficient to warrant fbrther evaluation and exploration of the MONS claim group to : I) determine the diamond potential of these Occurrences using an integrated exploration program including: a) soil sample geochemistry, b) whole rock geochemistry, e) heavy mineral and xenolith inclusion suites, and d) identification of kimberlitic indicator mineral suites. 2) identify additional Occurrences of kimberlitic dykes through mapping, prospecting and remote sensing, and
3) determine .the possible presence and location of hidden diatremes in subsurface or under cover using geophysics. I 4 I LOCATION AND AWES
The MONS claim group is located in the southern Rocky Mountains (latitude 51 O 49' 27" N, I; longitude 1 17" 00' 33" W), approximately 46.5 kilometres north of the community of Golden, B.C. on N.T.S. mapsheet 82 N/14E(see Figure 1 to 3). The claim group consists of 24 2-post claim units located over the headwaters of Mons Creek. At least five separate occurrences have been identified in the Mons Creek valley at elevations above 198 1 metres (6500 feet).
The claim group can be accessed by helicopter fiom Golden, B.C.. A logging road has been built along Icefall Brook and could be used for as a staging area for helicopter access. The logging road is approximately 7 kilometres west of the Mons claim group at its closest point (as of May 30, 1993). It is not feasible to hike into the properly fiom that point for bulk sampling and therefore helicopter access is recommended. Fly camps could be utilized for maximum economy to enable mapping and sampling to be carried out on the property. I
.- 1 --\ \ ! L.
Pacific Ocean
u. s. A I GWEN RESOURCES LTD. j
I MONS CLAIM GROUP1
Location Map
Gemquest Geological NTS 82 -9 h!e Sole . Fig P4G. Aug. '94 I 'E: .@oo,ooo I Figure 2 - General location map of diatreme localities in the southern Rocky Mountains (Pel1 1987) Fig 8
CLAIM STATUS
The property consists of 24 2-post claims (see Figure 4), staked in accordance with existing government claim location regulations. Significant claim data are summarized below:
Claim Name Units Tenure ## Date of Record Expiry Date*
MONS A1 1 3 17945 May 30,1993 May 30,1995 MONS A2 1 3 I 7946 May 30,1993 May 30,1995 MONS A3 1 3 17947 May 30,1993 May 30,1995 MONS A4 1 3 17948 May 30,1993 May 30,1995 MONS A5 1 3 17949 May 30,1993 May 30,1995 MONS A6 1 3 17950 May 30,1993 May 30,1995
MONS B1 1 3 17957 May 30,1993 May 30,1995 MONS B2 1 3 17958 May 30,1993 May 30,1995 MONS B3 1 3 17973 May 30,1993 May 30,1995 MONS B4 I 3 17974 May 30,1993 May 30,1995 MONS B5 1 3 17975 May 30,1993 May 30,1995 MONS B6 1 3 17976 May 30,1993 May 30,1995 'I-MONS B7 1 3 17977 May 30,1993 May 30,1995 MONS B8 1 3 17978 May 30,1993 May 30,1995 MONS B9 1 31 7979 May 30,1993 hAay30,1995 MONS BIO 1 3 17980 May 30,1993 May 30,1995 MONS C1 1 3 1795 1 May 30,1993 May 30,1995 MONS C2 1 3 17952 May 30,1993 May 30,1995 MONS C3 1 3 17953 May 30,1993 May 30,1995 MONS C4 1 3 17954 May 30,1993 May 30,1995 MONS C5 1 3 17955 May 30,1993 May 30,1995 MONS C6 I 3 17956 May 30,1993 May 30,1995 MONSCRWl I 317981 May 30,1993 May 30,1995 MONSCRW2 1 3 17982 May 30, I993 May30,1995
Total: 24
Copies of claim application fonns are provided in Appendix B.
*After 1994 assessment credit applied. I- U I- GWEN RESOURCES LTD. MONS CLAIM GROUP CLAIM LOCATION MAP I I i PHYSIOGRAPHY AND CLIMATE The MONS claim group is located within the headwaters of Mons Creek in the southern Rocky Mountains. Relief in the area varies from 1981 metres (6500 feet) along Mons Creek to more than 3 139 metres ( 10,300 feet) on Valenciennes Mountain (see Figure 3 and 5).
Outcrop is moderately well exposed throughout the claim group on moderately steep terrain. Small icefields and hanging glaciers with associated moraines are abundant and cover much of the lower levels of the claim group. Alpine to subalpine vegetation in the area consists predominantly stunted coniferous with subordinate deciduous trees (slide alder).
The ciaims are located east of the Rocky Mountain Trench and immediately west of the Columbia Icefields and are therefore subject to heavier precipitation than further north and south. As a result, many icefields and small glaciers are developed in the area. The property is available for geological exploration from mid-May to late October. I Figure 5 - Property Geology Map of the Gal claims (simplified from Nassichuk et al. 1989) I. LEGEND I; G - Glaciers and Perennial Snowbanks Qal - Alluvium I Qbs - BIock Stream I Qt - Talus Qmr - Recent Moraine
I Qmo - Older Ground Moraine I DM - Devonian - Mississppian (?) carbonate sequence DM 8 - youngest to DM 1 - oldest
I Ooc - Moddle Ordovician Owen Creek Formation I Osk - Middle Ordovician Skoki Formation ? 1 Oou - Lower Ordovician Outram Formation - upper member Oom - - middle member 1 001 - - lower member I Osp - Lower Ordovician - Upper Cambrian Survey Peak Formation (?) ospu - - upper member c Ospm - - middle member II cospl - - lower member I 1 I f I
I- I; I I I I I I I I I I I I I I I I 12
REGIONAL I. GEOLOGY Due to a lack of public domain mapping of the area, the following account has been taken from Dr. M.E. McCallum (Nassichuk et al. 1989):
No known previous detailed geological mapping has been done in the Mike area, and the rapid nature of this study did not allow for detailed stratigraphic descriptions. Consequently, formational designations are inferred on the basis of apparent similarity with units described in nearby areas. The major thrust fault that passes through the Mike area apparently is the Mons Fault ... The upper plate of this thrust consists of a moderately thick (>I300 m), carbonate dominated sequence of Cambro-Ordovician sediments in a southeast trending anticline with a steep overturned northeast limb (most beds dipping 60-85" SW). This anticline, informally referred to as the Valenciennes Anticline ..., has overridden a steeply dipping (70-80"S-SW), west-northwest trending package of Devonian (?)- Mississippian (?) carbonates that apparently exceeds 1400 meters in thickness.
The lower plate Devonian (?)-Mississippian (?) sequence is comprised predominantly of buff, gray and black, thin to thick bedded limestones and dolomites. Massive biohermal reefs occur locally. In the lower part of the sequence, gray limestones and dolomites contain progressively more interlayers of thin buff to tan beds and lamellae of calcareous siltstone, shale and sandy dolomite.
The upper plate Cambro-Ordovician carbonate sequence contains considerably greater proportions of shale, siltstone and mudstone. These have been tentatively correlated with the Middle Ordovician Owen Creek and Skoki Formations, the Lower Ordovician Outram Formation, and the Lower Ordovician-Upper Cambrian Survey Peak Formation. Informal members (upper, middle and lower) have been established for the Outram (?) and Survey Peak (?) Formations based on calcareous mudstone, shale and / or siltstone content of the carbonate. The latter units, along with thin bedded limestones commonly exhibit complex folding within the core of the Valenciennes Anticline, especially where they are bounded by more competent thick bedded carbonates. The less competent units also generally are characterized by well developed axial plane cleavage which strikes approximately 45-60" northwest and dips 60-80" to the southwest. Axial plane cleavage is best developed in the lowermost member of the Survey Peak Formation(?) and the Iower and upper members of the Outram Formation(?). These Same units were more susceptible to failure during thrusting and shear cleavage is commonly locally, 1 especially in proximity to fault traces. Slippage within more argillaceous units is well expressed by apparent fault repetition of the upper member of the Outram Formation (?) 450 meters south of Mike 2 diatreme. This sequence exhibits intense shearing and strongly oxidized planar zones are common 13
The Mons Thrust appears to be quite complex in the Mike area. It clearly is 1 '- imbricate, but the northernmost or lowest surface expresses maximum displacement. Failure zones range fiom thin (< lm) mylonite plates to thicker
~ I; zones (10's of meters thick) of mixed mylonites, protomylonites, breccias, and fractured host rocks. Anastomosing tectonic fabric is present locally. The intensely sheared to mylonitized mafic rock above (north of) the Mike 2 diatreme may have I been intruded along the thrust plane and was subsequently deformed by later movement along the fault."
I The Golden cluster of diatremes is a curvilinear array of alkalic occurrences which extends over approximately 55 kilometres (see Figures 2 and 3), all located west of the west-dipping Mons Creek Fault. They have been interpreted as lamprophyres, ranging from caicalkaline olivine I kersantite to the north (Bush River), through alkaline camptonites at Mons Creek and Valenciennes River to ultramafic aillikites (melilite fiee) to alnaites (melilite bearing) at the Hp occurrence to the south. In general, they are characterized as macrocryst-rich breccias and dykes I in which the macrocrysts present include titaniferous augite, phlogopite, green diopside, spinel and olivine. Melilite may or may not be present as microphenocrysts (Pell 1987).
I The alkalic intrusive occurrences (diatremes, dykes and / or pipes) are generally hosted by sediments of Upper Cambrian or Lower Ordovician age (see Figure 5). They all have deformation fabrics that are similar to the host strata., indicating emplacement of the alkalic intrusives prior to I deformation associated with Late Jurassic to Paleocene contraction in the Rocky Mountain Fold I and Thrust Belt (Parrkh and Reichenbach 1992). Dating has been attempted on several of the occurrences in the Golden area Two of the pipes have returned Rubidium / Strontium (Rb / Sr) ages of 334 * 7 Ma and 348 f 7 Ma fiom I phlogopite separates (Pell 1987). The HP pipe is the best preserved of the fifteen or more occurrences reported in the Golden cluster and has returned the following phlogopite separate ages: 348 f 7 Ma (Rb-Sr); 391 f 12 Ma and 396 f 12 Ma (Potassium / Argon) (Pel1 1987). Pamsh and Reichenbach (1992) attempted to determine emplacement ages for four of the diatremes in the Golden cluster, namely the Jack, Mark, Mike and HP occurrences. A total of sixteen zircons were utilized for U-Pb geochronology. The resulting ages ranged fiom Archean to Paleozoic and are therefore interpreted to be inherited xenocrysts from underlying lithologies sampled by the diatremes during ascent (Parrish and Reichenbach 1991). Possible lithologies proposed include: detrital grains from sedimentary rocks overlying basement (Purcell and / or I Windermere Supergroup), sills intruding these strata and / or heterogeneous basement complex lithologies. None of the zircons dated were interpreted as cu-magmatic in age.
'I 14
HISTORY
Alkaline occurrences in the Golden area have been previously sampled for recovery of heavy
~ I, mineral concentrates (including diamond and kimberlite indicator minerals). Diamonds (both micro- and macrodiamonds) have reportedly been recovered from both the Jack and Mark claims, north east and southwest of the MONS claims group respectively. In 1983, the Jack and Mark I claims (probably the Larry claims as well) were sampled by Dia Met Minerals Ltd The following excerpts have been paraphrased fi-om Minfiles 082N 088 (Jack), 089 (Mark) and 083C 001 I (Larry). In 1983, treatment of seven bulk samples from an upper breccia portion of the Jack diatreme resulted in the recovery of pyrope garnets, ilmenites and chromites. One 29.5 kg sample, 1 described as "sandy marl", produced an excellent, gem quality, colourless, octahedral microdiamond weighmg 0.00037320 carats. Further sampling, analysis and diamond drilling in I 1985 and 1986 failed to confirm the presence of diamonds. in 1983, a 30 kg portion of a 160 kg bulk sample of the Mark diatreme produced one ilmenite, thirteen chromites and one 0.00015820 carat microdiamond fragment. Further examination, I sampling and analysis in 1986, 1988 and 1990 has identified ilmenite, chromite and garnet but failed to confirm the presence of diamonds.
I A total of four bulk samples of diatreme material have been taken form the Larry claims and processed for recovery of diamonds and kimberlite indicator minerals. Diamonds were not found I in the sampies processed. The mineralogy of the diatreme was determined to be chromium diopside, chromite, G5 (eclogitic and / or primitive mantle source) magnesium almandine garnet, magnetite, grossular garnet, forsterite and clinopyroxene. The presence of G5 garnets, in I particular, is consistent with a diamond paragenesis. Furthermore, a brief review of pertinent Assessment Reports revealed additional information regarding these claims. The Jack claims have been interpreted to contain outcrops of kimberlite and kimberlitic tuff together with the sandy marl from which the microdiamond was reportedly recovered. Reported heavy mineral recovery includes abundant pyrope (6 4000 pyrope grains 1 from samples Jack 10 and 14B), Cr diopside, chromite, picroilmenite and 10 diamond chips (3 recovered following heavy liquid separation) (Assessment Report 15289). An additional seven bulk samples (no weights given) from "upper breccia portion" produced 33 pyrope, 48 ilmenite and 15 chromite, two G9 and six GI 1 garnets and one sapphire.
The Mark claims produced a singe clear white microdiamond chip recovered from a 35 kg talus I sample of a tuffaceous crater facies breccia and / or olivine - clinopyroxene lamprophyre (Assessment Report 15 15 1). A picroilmenite analyzed from heavy mineral concentrate reportedly had the following partial composition (4.32 YO Cr,O, and 13.46 YO Me). Assessment Report I 17753 documents 1 microdiamond, I3 chromite and 1 picroilmenite grain, probably as a summary of past results. An additional 44 chromites, 1 G5 eclogitic garnet (Mg - almandine) and 24 I 15
almandine garnets were detected using a scanning electron microscope (SEM). The host lithology I I- was interpreted to be a lamproite
Finally, sampling was undertaken on the Mike claims (restaked as the current MONS claim group I; for Gwen Resources Ltd.). The main pipe was described as a heterogeneous, polyphase diatreme having a sub-vertical exposure of 250 metres by 400 metres. The ‘North”diatreme is reportedly I dyke-like and north - south trending, comprised of a kimberlitic sandy marl similar to the Jack Occurrence (10.5 kilometres to the northwest) and having approximate dimensions 800 metres by 200 metres. The occurrences contain serpentine (altered olivine) in a matrix of sericite, carbonate, I serpentine and commonly rounded quartz pellets. Secondary overgrowths of quartz, carbonate and sericite are present on carbonate and quartz (Assessment Report 14748).
I Recovery of* 75 ilmenite, f 75 chromite and 9 chrome diopside were reported from 10 kg (?) stream sehentsamples (Assessment Report 14748). Furthermore, high chrome (diamond inclusion field) chromites were reported, having chrome contents in excess of 55 weight per cent I (Assessment Report 17303).
The Mike claims have been thoroughly described in terms of field examination and mapping, thin 1 section descriptions, whole rock / mineral chemistry and heavy mineral concentrates (Nassichuk et al. 1989). A total of 114 chromites and 1 high chromium clinopyroxene grain were andyzed in the come of the study. Although the chromites were interpreted to have been derived from a I chromite harzburgite source, none of the chromites analyzed are high chrome chromites comparable to compositions in the diamond stability field.
I The description of mineral grains in the heavy mineral fraction include spinels (steel gray to black, metallic, euhedral to subhedral, octahedral), ilmenite (black, metallic, opaque, subangular anhedrd grains with lightly pitted surfaces) and diopside (green, translucent to transparent, angular to sub I angular, dull, anhedral) (Nassichuk et al. 1989). Furthermore, both rounded tourmaline and high Cr,O, chromite were identified from Mons Creek, interpreted to have been derived from an as yet I undetected (covered) diatreme of lamproitic afinity (Fipke, in Nassichuk et al. 1989). I I I I I I 16
LOCAL GEOLOGY I The following has been paraphrased from Dr. M.E. McCallum (Nassichuk et al. 1989):
The Mike diatremes are comprised predominantly of a pale brown to dark brown or pale reddish brown weathering, pale gray to olive and olive gray phase with the exception of the Mike 2. The Mike 2 is comprised of an intensely oxidized, red to maroon phase. Both phases range from coarse to fine (clasts >I metre to -4centimetre) matrix supported breccia. A minor coarse clast supported breccia occurs at or near diatreme margins. The clasts are angular to well rounded, and consist predominantly of supracrustal sedimentary lithologies (carbonates with variable amounts of mudstone-siltstone-shale). Inclusions of crystalline Iithologies (up to 30 cm in diameter) are generally intensely altered and include basalt / andesite fragments, coarser 5ined lamprophyre, rare quartzite, quartzofeldspathic gneiss, granite / granodiorite, gabbro, quartz diorite, granulite and pyroxenite. There is a well developed cleavage in the breccias that is essentially parallel to axial planar cleavage in the host sedimentary strata (northwest trend, dipping 45" to 70" SW).
Lamprophyric clasts have a porphyritic texture and are comprised predominantly of fresh phlogopite with subordinate sanidine. Coarser lamprophyres consist of chloritized phlogopite, pyroxene (replaced by a turbid mixture of finely crystalline dolomite, chlorite and leucoxene) and olivine (replaced by dolomite, minor quartz and minor serpentine and having red - brown spinel inclusions) in a fine-grained groundmass of calcite / dolomite, sericite, talc, chlorite'and finely crystalline quartz that may be replacing sanidine. Plagioclase and spinel have also been reported as phenocryst phases (ijewliw and Schulze 1988). Accessory phases include abundant tiny grains ( Mafic and lamprophyric dykes and sills occur throughout the area. The mafic dykes are comprised of a dark 5yto greenish black, porphyritic to microporphyritic aphanitic lithology, ranging from 5 centimetres to 6 metres in thickness. They are typicalfy intensely sheared, chloritized and commonly oxidized and therefore the primary mineralogy is diff'icult to identify. They have been interpreted as basaltic to andesitic in composition. The lamprophyric dykes and sills (?) intrude diatreme breccias as well as host sedimentary strata and appear to be younger than the mafic intnisives. They are typically phlogopite-rich (minor to abundant macrocrysts of phlogopite) with Cr-diopside and / or salite. The lamprophyric dykes and sills "... appear to be temporally related to the diatremes, but at least one of the dykes appears to I have a kersantitic rather than possible lamproitic affinity". 17 1993-94 PROGRAM A total of two mandays were spent on the property by the authors, in an attempt to determine the economic potential of the property. One 53.3 kg bulk sample was taken from diatreme float on the MONS claims (see Figure 9, I representing various phases of the diatreme. The bulk sample was shipped to Loring Laboratories Ltd. in Calgary, where it was initially crushed to -6 mesh A representative portion was split from the crushed, homogenized sample and analyzed for whole rock, gold and 47element ICP at I Activation Laboratories Ltd. in Ontario. The remaining crushed material was then placed in an acid bath for 24 hours to remove carbonates, washed, deslimed and further processed through I heavy-liquid media. The heavy liquid separation resulted in two sets of mineral separates: one containing minerals having specific gravities between 2.96 and 3.30 and a second having minerals greater than 3.30 1 S.G.. The heavy mineral hction (>3.3 S.G.) was further separated using a Frantz Isodynamic Magnetic Separator into four fiactions: non-magnetic, weakly para-magnetic, para-magnetic and 1 magnetic. The resulting heavy mineral concentrates were examined by R. Walker. Due to a Section 35 complaint under the Mineral Tenure Act, sufficient work was performed to retain the claims in the event of a decision favouring Gwen Resources Ltd.. As a result, no 1 electron microprobe analyses were determined for any grains from the Mons claims group. Samples analyzed by ICP methods were crushed to -80 mesh and dissolved in qua-regia solution. 18 RESULTS A representative fraction of crushed, homogenized bulk rock material was sent to Activation Laboratories Ltd. in Ontario for whole rock and ICP analysis. The results are included in Appendix C. Whole rock data for sample MON93-1 indicate a mafic composition (>45 weight per cent SiOJ with a nominal MgO content for kimberlitic. With the exception of A120hFe203 and MgO, major trace element falls within the ranges provided by Dawson (1980). The values returned for M203 and Fe,O, are only sIightly greater than the ranges provided. However, MgO is substantialIy Iowa than kimberlitic values. In contrast, major element data does not compare well with generalized data for Iamproitic lithologies. Furthermore, the trace element data (see Table 1) is generally comparable to kimberlitic values established from worldwide occurrences as compared to the range for average ultramafic compositions. However, both Cr and Ni are substantially lower than I comparable kimberlite values fiom worldwide occurrences. Deviation fiom kimberlitic cornpositim is expected as the samples submitted for geochemical analysis were not free of contamination by host IithoIogies, The diatremes in the Golden cluster I are described as inclusions rich breccias. Therefore, xenoIiths of host lithologies are present and include both carbonate- and silica-rich compositions (eg. Upper Cambrian and / or Lower Ordovician sedimentary lithologies). Therefore, a characteristic kimberlitic composition will be 1 diluted by inclusion of these sedimentary inclusions (xenoliths). Sample MON93-1 was a bulk sample taken of diatreme material found in Mons Creek below the Mike 2 (?) occurrence. It was processed at Loring Laboratories as described in " 1993-94 Program" above. The weights of the fractions obtained through heavy liquid separation are tabulated below. Middlings (g) Heavies (2.96-3.3 S.G.) p3.3 S.G.) Original Mag. Non-Mag. Magn. Non-Map. Sample ID Weight (kg) (g) (8) (8) (g) MON93-1 53.3 11.09 35.41 20.37 3.98 I 19 I Table 1: Representative trace element content for ultramafic and kimberlitic lithologies. Column A - average ultramafic, Column B - kimberlite, Column C - Mons Creek homogenized sample, Column D - Group A kimberlitic lamprophyres and Column E - true I; kimberlites. Columns A and B data from Dawson (1980); Columns D and E from Pope amd I ThirlwaIl(1992). All values in ppm. I !Element 1 A I B C I D 1 E I I I I I Ce 1.93 45 - 522 47 106-119 75-78 I I co 110 35 - 130 50 1 I - Cr 3090 550- 160 489-917 591-698 I 2900 1 cu 47 10 - 300 100 - - Nb 1.3 32 - 450 - 104 - 127 67 - 73 I ~ ~ Nd 1.44 25 - 180 23 42-50 33-35 Ni 1450 710- 50 217 - 362 478 - 631 I 1600 I Sr 22 40 - 1900 72 342 - 992 514 - 544 I Y 2.9 4-75 36 i Zn 56 15-287 91 - - I Zr 16 84-700 106 170 - 213 228 - 235 1 I I I I 20 DISCUSSION Most of the garnets identified in the heavy mineral separate are light to medium orange in colour and are almost certainly not pyrope rich. Based upon previous experience, these garnets are probably predominantly G5 (eclogitic source) and / or regional metamorphicderived magnesium almandine garnets. Ijewliw (1991) reported that "-..chrome ranges from 36.52 to 45.12 weight per cent Cr@, with one sample measuring at 53.24 weight per cenf Cr,O,. Titanium does not exceed 0.91 weight per cent TiO,." Evaluation of the chromite analyses in Open File 2124 (Nassichuk et al. 1989) in terms of the four chromite categories defined by Griffin et ai. ( 1992) indicates there are 43 PI ,4 P2,28 P3 and 8 P4 chromites. P1 chromites are interpreted to represent xenocrysts in Group I kimberlites and to be a significant xenocryst phase in Group II kimberlites, derived from disaggregated dunites, haxzburgites and subordinate lherzolites. P2 chromites are interpreted to be representative of Group II kimberlites, present as high pressure magmatic phenocrysts in a kimberlitic magma. P3 chromites are interpreted as lamproitic in origin and essentially magmatic in origin. P4 chromites are interpreted as xenocrysts derived from low temperature - pressure spinel f garnet Iherzolite. The chromites described above are transitional in that, in many cases, they have TiOz values slightly higher than those described in Griffin et el. (1992). However, outliers were also described and so TiO, ranges were not rigorously adhered to in classifying chromites. In summary, the Chromites recovered and documented in the literature for the Mike diatremes (MONSclaim group) compare we\! with Group I, Group fI and lamproitic chromites. "The Golden cluster magnesiochromites ... are closer in composition to the subset of ceylonites, chromites or magnesiochromites from specific, ultramafic lamprophyres, especially aillikites. ... . Magnesio- chromite spinels from lamprophyres of extreme composition, lurnberlites and lamproites, also have similarities ... Either they crystallized from a hydrated, peridotitic mantle melt or are merely xenocrysts from disaggregated peridotites" (Ijewliw 1991). The high chrome clinopyroxene reported in Open File 2124 (Nassichuk et al. 1989) is a CP3 (Ti- Cr diopside), considered representative of kimberlite, garnet Iherzolite and garnet pyroxenite source iithologies (Stephens and Damn 1977). CIinopyroxenes noted in the hcavy mineral concentrate recovered from the 1993 - 1994 program are predominantly translucent green in colour and range from angular (broken fragments) to euhedral, columnar in morphology. These are probably medium to high chrome diopsides. Ijewliw (1991) states that "-.-variations in the zoning directions and patterns (in clinopyroxenes) indicate a relatively prolonged period of crystal interaction with fractionated, primitive and xenocrystic melts. ... zoning is multiple, and sometimes oscillatory. It is the product of repetitive interaction among xenocrystic, fractionated and primitive melts ... Mons Creek diatreme had a comparatively longer residence time prior to ascent to the surface." 'I 21 The definition of a lamprophyre (Rock 1987) states that essential minerals should include I amphiboles, biotites, phlogopites and other volatile-rich minerals such as halides, carbonates, ~ 1- sulphates and zeolites, in addition to feldspars and quartz with coexisting magnesium-rich minerals, olivine and clinopyroxene. Neither feldspars nor quartz occur as phenocrysts and olivine does not 5 occur in the groundmass. I The presence of titanaugite with plagioclase confined to the groundmass, is consistent with a biotite - camptonite classification (Ijewliw and Schulze 1988). However, in their description they list plagioclase as a phenocryst (xenocryst) phase. Other reports have described the lithologies I present in the MONS claim group as kimberlitic (Assessment Report I4748), Iamprophyric (Ijewliw and Schulze 1988, Fell 1987) and lamproitic (Nassichuk et al. 1989). The extraordinary concentrations of leucoxene infer high titanium heritage, and abundant accessory apatite is I characteristic of ultrapotassic rock suites such as ultramafic lamprophyre, kimberlite and Iamproite (Nassichuk et a1 1989). I Ijewliw and Schdze (1988) conclude that "... fiom north to south, there is an apparent trend fiom the calcalkaline kersantites at Bush River, through the alkaline camptonites of Mons Creek and Valenciennes River, to the ultramafic ailiikite at HP. ... variation within the Golden cluster, 1 however, demonstrates that a diverse suite of lamprophyre magmas was generated and emplaced in response to extension along the western margin of North America in the early Paleozoic. It is postulated that an extensional tectonic regime contributed to conditions initiating the original I lamprophyre melts and these conditions could also have caused the necessary fractures or zones of weakness allowing their emplacement in a linear array. The variation in the Iamprophyre compositions may be due to variations in depth of melting, crustal residence time during ascent and 1 interaction with crustal material." 1 I I 1 I I 1. I I 22 I CONCLUSIONS AND RECOMMENDATIONS At least 50 diatremes are known to be present within the Rocky Mountains of southeastern British I; Columbia. However, regardless of their diamond potential, the fact that they originated in the lower levels of the crust or from within the mantle suggests potential for hosting Rare Earth Elements (REE's) and / or Platinum Group Elements (PGEs). Furthermore, having intruded the I crust from mantle depths and being comprised of a high proportion of carbonate and volatiles, they may also have acted as conduits through which mineralized ff uids passed, precipitating base and I precious metals. Preliminary geochemical results of samples taken from the Occurrence confirm an ultrapotassic (mafic to ultramafic) affinity. Furthermore, ultramafic nodules (pyroxenites) and abundant I kimberlitic indicator minerals have been reported fiom the claims and in the immediate area- At present, it is not clear where these intrusives originated relative to the diamond stability field It is particularly significant that the diamond-bearing lamproites north of Golden restore palinspastically outboard of the Crossing Creek kimberlite occurrence. Dr. K.L. Currie regards the diamond potential of the Rocky Mountains alkaline province as good for the following reasons: I "(i) The alkaline rocks clearly came up through continental crust. (ii) The alkaline (rocks) have diverse compositions and ages. Both these conditions are necessary, but not sufficient. Likewise, it is not sdficient to demonstrate "kimberlitic" I chemistry, unless the appropriate xenocrysts are present (chrome diopside, pyrope, magnesian ilmenite) ... it has not been demonstrated that any Cordilleran kimberlite or lampite-like rocks have passed through the diamond stability field. It seems to me that the appropriate P-Tdetermination (from indicator minerals or I thermobarometry) is essential..." (K.L. Currie, pers. comm. 1993). The Rocky Mountains are underlain in this area by Archean basement for which an age of 2.6 to 3.2 billion years has been determined, consistent with the ages of peridotitic diamonds determined I world-wide (3.3 billion years - Levinson et al. 1992, Kirkley et al. 1992). Zircons recovered from several diatremes in the Rocky Mountains have been determined to have Archean ages. Abundant indicator minerals have been recovered, including compositions comparable to world-wide I diamond inclusion field compositions and Group I and lamproite chromites. Must important of all, the most reliable diamond indicator mineral, diamonds, have been recovered from alkaline I occurrences which were once outboard of the Crossing Creek kimberlite. If the results of additional work do confirm a kimberlitic affinity for the dykes in terms of composition, elemental suites, kimberlitic indicator minerals and / or deep seated xenoliths (peridotitic and / or eclogitic inclusions) a follow-up program of trenching and drilling is recommended. Trenching, possibly with blasting, would enable the collection of a large sample of I pristine diatreme material for a determination of diamond content. Drilling is recommended upon . favourable geochemical results, in terms of a kimberlitic indicator (heavy mineral) and / or xenolith suite. A preliminary budget has been prepared for the above work and is presented on the following page. 24 PROPOSED BUDGET . Re-Field $5,000.00 Field Program Diamond Drilling $30,000.00 Personnel $20,000.00 Helicopter Support $5,000.00 AndflCal $5,000.00 camp costs $2,000.00 Food/Grocery $4,000.00 TruckEquipment Rentals $ 1,000.00 Fuel $ 1,000.00 Transportation $2,000.00 Supplies $ 1,000.00 Miscellaneous $ I,ooo.oo $77,000.00 Contingency on Field Program (10%) $7,700.00 Post-Field $5,000.00 TOTAL: $89,700.00 'I 25 REFERENCES ~ I: Armstrong, R.L., Parrish, R.R., van der Heyden, P., Scott, K., Runkle, D. and Brown, RL. 1991. ' - Early Proterozoic basement exposures in the southern Canadian Cordillera: core gneiss of I, Frenchman Cap, Unit I of the Grand Forks Gneiss, and the Vaseaux Formation, Canadian I Journal of Earth Sciences, vol. 28, pp. 1169 - 1202. Cook, F.A., Varsek, J.L. and Clarke, E.A. 199 1. Proterozoic craton to basin transition in western Canada and its influence on the evolution of the Cordsllera, Canadian Journal of earth I Sciences, vol. 28, pp. 1 I48 - 1158. Dawson, J.B. 1987. The kimberlite clan: relationship with olivine and leucite lamproites and I inferences for upper mantle metasomatism. In Alkaline igneous rocks. Edited by J.G. Fitton and B.G.J. Upton. Geological society of London, Special Publication 30, pp. 95- I 101. . 1980. Kimberlites and Their Xenoliths. Springer - VerIag New York. 252p. I Grieve, D.A. 1982. Petrology and chemistry of the Cross kimberlite (82J/2), British Columbia Ministry of Energy, Mines and Petroleum Resources, Geology in British Coliunbia, 1977- I 1981, pp. 34 - 41. Gnfin, W.L., Ryan, C.G., Gurney, J.J. Sobolev, N.V. and Win, T.T. 1992. Chromite I macrocrysts in kimberlites and lamproites: geochemistry and origin. In Proceedings of the 5th International Kimberlite Conference, in press. I Helmstaedt, H.H., Mott, J.A., Hall, D.C., Schulze, D.J. and Dixon, J.M. 1987. Stratigraphic and structural setting of intrusive breccia diatremes in the White River - Bull River area, southeastern British Columbia - Cross, Blackfoot and Hp (825,82G, 82N), British I Columbia Ministry of Energy, Mines and Petroleum Resources, Geological Fieldwork, Paper 1988-1, pp. 363-368. I Hoffman, P.F. 1988. United plates of America: the birth of a craton, Annual Review of Earth and Planetary Sciences, vol. 16, pp. 543 - 604. I Hdy, T. 1993. Geology of the PurcelI Supergroup in the Fernie West-Half Map Area, Southeastern British Columbia, British Columbia Ministry of Energy, Mines and Petroleum I Resources, Bulletin 84, 157p. Ijewliw, 0.J. 199 1. Petrology of the Golden cluster lampphyres in southeastern British 1 Columbia (82N), British Columbia Ministry of Energy, Mines and Petroleum Resources . Geological Fieldwork, Paper 1992-1, PP. 37 - 45. IC 'I I III 26 and Schulze, D.J. 1988. The Golden cluster of diatremes and dykes, British - Columbia Ministry of Energy, Mines and Petroleum Resources Exploration in British Columbia, pp- B39 - B46. ' I,I Kirkley, M.B., Gurney, J.J. and Levinson, A.A. 1992. Age, origin and emplacement of diamonds: I a review of scientific advances in the last decade, CIM Bulletin, vol. 84, pp. 48 - 57. Levinson, A.A., Gurney, J.J. and Kirldey, M.B.1992. Diamond sources and production: past, I present and hture, Gems and Gemmology, vol. 28, pp. 234 - 254. Mmnough, M.R., and Parrish, R.R. 1991. Proterozoic gneisses of the Malton Complex, near Valemount, British Columbia: U - Pb ages and Nd isotopic signatures, Canadian Journal of I Earth Sciences, vol. 28, pp. 1202 - 1216. Murphy, D.C., Walker, R.T. and Panish, R.R. 1991. Age and geological setting of Gold Creek I Gneiss, crystalline basement of the Windermere Supergroup, Carib00 Mountains, British Columbia, Canadian Journal of Earth Sciences, vol. 28, pp- 12 17 - 123 1. I Nassichuk, W.W., Fipke, C.E., Moore, R.O. and Gurney, J.J. 1989. The development of advanced technology to distinguish between diamondiferous and barren diatkmes, I Geological Survey of Canada, Open File 2 124,1175~. Parkinson, D. 1991. Age and isotopic character of Early Proterozoic basement gneisses in the I southern Monashee Complex, southeastern British Columbia, Canadian Journal of Earth Sciences, vol. 28, pp. 1 159 - 1 168. I Parrish, R.R. and Reichenbach, I. 199 1. Age of xenocrystic zircon fiom diatremes of western Canada, Canadian journal of earth Sciences, vol. 28, pp. 1232 - 1238. I Pell, J. 1987. Alkaline Ultrabasic Rocks in British Columbia: Carbonatites, Nepheline Syenites, Kimberlites, Ultramafic Lamprophyres and Related Rocks, British Columbia Ministry of I Energy, Mines and Petroleum Resources, Open File 1987-17,109p. 1986. Alkalic ultrabasic diatremes in British Columbia: Petrology, Geochronology and Tectonic Significance (82G, J, N; 83C; 94B), British Columbia Ministry of Energy, Mines I and Petroleum Resources, Geological Fieldwork, Paper 1987-1 ,pp. 259-267. ------. 1985. Diatreme breccias in British Columbia (82G, J, N; 83C; 94B), British CoIumbia I Ministry of Energy, Mines and Petroleum Resources, Geological Fieldwork, Paper 1986-1 , I pp. 243 - 253. . Pope, A.J. and Thirlwall, M.F. 1992. Tectonic setting, age, and regional correlation of ultrabasic - ultrapotassic dykes in the northern Purcell Mountains, southeast British Columbia, IC Canadian Journal of Earth Sciences, vol. 29, pp. 523 - 530. I I I 27 I Rock, N.M.S. 1987. The nature and origin of lamprophyres: minettes, vogesites, kersantites and spessartites, Royal Society of Edinburgh Transactions, Earth Sciences, vol. 74, pp. 193 - 227. Ross, G.M.I99 1. Precambrian basement in the Canadian Cordiflera: an introduction, Canadian I Journal of Earth Sciences, voi. 28, pp. 1133 - 1139. ,Parrish, R.R., Villeneuve, M.E.and BoWrtng, S.A. 1991 Geophysics and geochronology of the crystalline basement of the Alberta Basin, wesfern Canada, Canadian I Journal of Earth Sciences, vol. 28, pp. 512 - 522. Smith, C.B., Colgan, E.A., Hawthorne, J.B. and Hutchinson, G. 1988. Emplacement age of the Cross kimberlite, southeastern British Columbia, by the Rb - Sr phlogopite method, Canadian Journal of Earth Sciences, vol. 25, pp. 790-792. Stephens, W.E. and Dawson, J.B. 1977. Statistical comparison between pyroxenes fiorn kirnberlites and their itssociated xenoliths, Journal of Geology, vol. 85, pp. 433 - 450. Woodsworth, G.J., Anderson, R.G. and Armstrong, R.L. 1991. Plutonic regimes, Chapter 15 in Geology of the Canadian CordiIleran Orogen in Canada, H. Gabrielse and CJ. Yorath (ed.); GeoIogical Survey of Canada, Geology of Canada, m. 4, pp. 491 - 53 1. I 28 I Appendix A - I; Statement of Qualifications I I I I I I I I I 29 1 STATEMENT OF QUALIFICATIONS 1; I, Richard T. Walker, of 1916 - 5th Street South, Cranbrook, BC, hereby certify that: 1) I am a graduate of the University of Calgary of Calgary, Alberta, having obtained a Bachelors 1 of Science in 1986. 2) I obtained a Masters of Geology at the University of Calgary of Calgary, Alberta in 1989. I 3) I am a member in good standing with the Association of Professional Engineers, Geologists and Geophysicists of Alberta I 4) I a member of good standing with the Association of Professional Engineers and Geoscientists of the Province of British Columbia. 5) I am a consulting geoIogist and Principal with the fmof Gemquest Geological with oflices at 19165th St. S., Cranbrook, British Columbia. 6) I am the author of thls report which is based on work I personally performed on the property 'I between May 3Oth, 1993, and May 29th, 1994. 7)I was personally involved in the acquisition ofthe claims described herein. I 8) I hold at present 130,500 common shares of Gwen Resources Ltd.. I Dated at Cranbrook, British Columbia this 17th day of August, 1994. 1 I 1 32 Appendix C Analytical Results I v. UCI-IWuCa I UtULdtJILHL 1-1 le NO. s3a10-u 1916 - 5th Street South: Date July 29, 1993 ICranbccok, B.C. V1C 1K4 Samp 1es # Certificate of Assa LORING LABORATORIES [TD I SAMPLE NO. Sample ID. Samole Tn. SamDle ID. Samole ID. SamDle ID. Sam le ID. I--- - H& 93-1 Original Wt. (kg) 48.5 50.6 50.5 50.1 59.3 53.3 2.9-3.3 Middling Wt. (gin) 2.96 0.31 0.35 33.59 0.75 46.64 2.9-3.3 1Middling Magnetic Wt. (9m) 0.006 0.07 0.15 26.8 0.04 11.09 12.9-3.3 Middling Non-Magnet ic ,Wt. (gm) 2.96 0.23 0.19 6.73 0.71 35.41 >3.3 Heavy Wt. I(w) 0.55 1.81 1.99 119.82 1.64 24.35 >3.3 Heavy (Hagnetic Wt. (gm) 0.24 0.59 1.53 118.53 0.14 20.37 >3.3 Heavy ,:;n-Magnet ic - (9m) 0.31 1.21 0.46 1.26 1.49 3.98 I NOTE: Only 20 kg were processed for each sample. I 1 Herebi certifl that the above, results -are those assays ade by e upon the herein described samples .... i *ejects retained one month. ulpa retained one month oless specific arrangements ere made in advance. Aseayer Activation Laboratories Ltd. Work Order: 5363 Report: 5258C SAmLE # Si02 Ti02 A1203 Pe203 lln0 wo CaO Ha20 K20 P205 Lo1 mAL 8 8 8 8 8 8 8 8 8 8 8 8 44.41 2.86 12.56 17.21 0.19 5.67 3.97 3.28 0.91 0.27 10.01 98.21 no~93- 1 47.95 2.15 14.15 13.17 0.13 5.90 5.06 2.14 1.76 0.27 7.30 97.56 36.35 1.21 8.96 7.05 0.11 11.66 15.96 0.70 0.26 0.32 19.67 100.71 35.70 1.56 7.54 8.90 0.19 13.56 11.77 0.39 0.41 0.17 20.19 98.64 35.70 2.07 8.92 11.39 0.24 7.59 13.67 0.03 2.69 <0.01 20.33 100.57 39.11 1.05 13.10 9.29 0.14 7.91 11.69 1.00 0.95 0.42 16.00 99.19 Activation Laboratories Ltd. Work Order: 5363 Report: 5258 Sample description AU AG AS BA BR CA co CR cs PE KF EO IR no NA NI RB SB sc SE SN SR TA TE PPB PPH PPI PPI PPW 8 PPH PPW PPH 8 PPW PPH PPB PPH 8 PPH PPI4 PPH PPH PPH PPH PPW PPH PPH 2 <5 6.2 390 ~0.5 2 60 130 <1 14.0 7 <1 <5 3 2.81 120 26 11 52 <3 <2 <5 5.5 350 <0.5 9 50 750 2 7.67 3 <1 <5 <1 0.93 180 82 0.4 28 <3 Activation Laboratories Ltd. Work Order: 5363 Report: 5258 Sample description u w ZN LA CB ND sn EU TB YB LU naes ppn ppn PPn ppn PPn ppn ppn PPn ppn PPM PPn 9 .. ~0.5 <1 169 21 50 22 7.5 2.3 0.9 5.9 0.80 18.79 MON 93-1 2.0 <1 151 18 47 23 6.1 2.2 eO.5 4.7 0.71 12.34 .. 2.5 <1 100 64 120 37 6.1 1.8 0.6 1.6 0.24 15.49 2.7 <1 130 80 160 62 9.0 2.8 qO.5 1.5 0.25 18.29 3.1 12 187 150 290 91 16 4.3 1.5 2.8 0.40 14.45 4.4 <1 116 100 190 48 7.5 2.5 <0.5 2.2 0.33 17.34 Activation Laboratories Ltd. Work Order: 5363 Report: 52588 Sample deecription CU PB ZN AG NI UN 6R CD BI V CA P HG TI AG U Y BE ppn PPH ppn ppn PPn PPn ppn PPH ppn PPn t t t t t t PPn PPH 105. 29. 118. <0.4 52. 1292. 66. <0.5 <5. 282. 3.25 0.118 3.68 0.39 6.62 0.50 16. <2. 100. <5. 91. ~0.4 50. 903. 72. ~0.5 <5. 265. 4.11 0.087 3.97 0.61 7.31 1.94 12. <2. 27. <5. 52. <0.4 390. 725. 546. <0.5 <5. 79. 2.43 0.140 7.63 0.52 4.69 0.14 13. <2. 27. 12. 112. <0.4 457. 1200. 554. <0.5 <5. 122. 9.34 0.234 9.03 0.36 4.04 0.06 12. <2. 50. 14. 100. 0.4 262. 1447. 369. <0.5 <5. 144. 0.06 0.318 4.78 0.60 4.43 2.21 22. <2. 61. <5. 105. <0.4 220. 847. 341. eO.5 <5. 119. 8.83 0.168 5.18 0.43 6.66 1.16 14. <2. Activation Laboratories Ltd. Work Order: 5363 Report: 5258CC SAMPLE I Ba Sr Y zr PPn PPn PPn ppn 272 76 67 138 728 70 36 106 97 565 27 111 112 558 22 90 395 412 36 145 321 374 23 98 I 33 . Appendix D Statement of Expenditures . I 34 I STATEMENT OF EXPENDITURES I The following expenses were incurred on the MONS claim group for the purpose of geological [ exploration within the period May 30,1993 to May 29,1994. I PERSONNEL R.T. Walker, P-Getl.: 1.0 days x $350.00 /day $ 350.00 I T. J. Termuende, P.Geo. 1.0 days x $350.00 / day $ 350.00 EQUIPMENT RENTAL 4WDVehicle: 1.O days x $50.00 / day $ 50.00 1 Mileage: 497 km x $.20 / km $ W.40 Radios (2): 1.0 days x $10.00 /day $ 20.00 I Helicopter: 1 hour at $700 / hour $ 700.00 ANALYTICAL,: Whole rock / Au + 47 element analysis $ 50.00 I 1 50kg. Bulk Samples $ 350.00 FIELD SUPPLY I 2.0 man-days x $20.00 / day $ 40.00 MISCELLANEOUS I Fuel $ 100.00 Shipping $ 100.00 I REPORT / wpRoDucTroN I R. T. Walker, P.Geo.: 1.0 days x $350.00 / day $ 350.00 TOTAL EXPENDITURES: $2,559.40 I I I I a I I