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Special Report 12

Alteration Mineralogy of Alberta Kimberlites: PIMATM Infrared Spectroscopic Analysis

EUB Special Report 12 (July 2001) • i

Alteration Mineralogy of Alberta Kimberlites: PIMATM

Infrared Spectroscopic Analysis

By

Phoebe L. Hauff

Spectral International, Inc., P.O. Box 1027, Arvada CO 80001, USA; www.pimausa.com; [email protected]

With contributions from

Roy Eccles and Eric Grunsky

Alberta Geological Survey, Edmonton

AGS AEUB

Published as Alberta Energy and Utilities Board Alberta Geological Survey Special Report 12

AGS AEUB

AGS AEUB

EUB Special Report 12 (July 2001) • ii

PREFACE

The Alberta Geological Survey (AGS) assists the Alberta Department of Resource Development in administering the Metallic and Industrial Minerals Regulations of the Mines and Minerals Act for the Province of Alberta. Under these regulations the Crown collects mineral core and rock samples from companies working on mineral permits and after a period of confidentiality makes these materials publicly available for use by prospectors, mineral exploration companies and academia for mineral exploration and research purposes. Mineral core and rock samples are selected by an AGS geologist and exploration companies are directed to send these materials to the Mineral Core Research Facility (MCRF) in Edmonton. The core is cataloged and stored and is available for logging or sampling by the public, industry or the scientific community. At the Mineral Exploration Group (MEG) meeting held in Calgary on April12-13, 2000, the AGS displayed selected sections of diamond drill core from kimberlitic rocks within Alberta. The display caught the interest of Dr. Phoebe Hauff of Spectra International Inc. and Dr. Hauff offered to analyze the drill core sections using a portable infrared mineral analyzer (PIMA) with the expectation of identifying suites of minerals that can be recognized within the short wave infrared spectrum. The selection of a variety of kimberlitic rock types that were on display enabled a timely and comprehensive analysis on alteration minerals that are commonly found in kimberlites. The AGS agreed to have these samples analyzed and the results of the analysis are contained in this report, courtesy of Dr. Hauff. The AGS is pleased to make this information available to the public and hopes that the information contained within the report will assist in further identification and classification of kimberlitic rocks. Eric Grunsky, Information Geologist, AGS

THE SIGNIFICANCE OF RECOGNIZING ALTERATION ASSEMBLAGES IN ALBERTA KIMBERLITES

Rocks, soils, vegetation and water are separable using infrared spectroscopy, according to their spectral characteristics. The objective of this report is to provide spectrometer measurements from selected Alberta ultramafic diatremes, including kimberlite, using PIMA (portable infrared mineral analyzer). Like hydroxides, the mineral assemblages associated with and weathered from kimberlitic diatremes include for example, carbonates and the serpentine group minerals, both of which are widely distributed in kimberlites and frequently constitute 80 to 90% of their volume. However, little or no attention has been paid to the detection of these mineral assemblages using their possibly distinctive

EUB Special Report 12 (July 2001) • iii

spectral absorption band patterns. Instead, emphasis has been given to some other accessory minerals (e.g., pyrope garnet, chromite, etc.) as well as to mantle xenoliths. Spectral imaging may have particular application for the detection of kimberlites in Alberta. Especially since some kimberlitic diatremes form topographic highs and the minerals found in kimberlitic terranes may be easily distinguishable from surrounding Phanerozoic shales and sandstones in the mid-infrared spectral range. The data presented within this report provide alteration information that may be used both regionally with hyper spectral remote sensing and in the field to provide quick and accurate analysis of potential target rocks, soil, etc., or to assist mapping. For example, the spectral analysis of surficial materials may reflect underlying lithologies because spectral features are often indicators of products associated with the weathering and alteration of the underlying materials. Thus, a better understanding of the possible alteration assemblage will increase our knowledge about the Alberta ultramafic diatremes and may yield data important for the development of deposit models and regional exploration programs. D. Roy Eccles, Senior Geologist, AGS

DISCLAIMER The information provided with this report is provided, “as-is”, by the principal author, Dr. Phoebe Hauff. The report and its contents, conclusions and/or recommendations do not necessarily reflect the view of the Alberta Energy and Utilities Board or the Government of Alberta, its officers, employees or agents. Specifically, the Alberta Energy and Utilities Board and the Government of Alberta, its officers, employees or agents, make no warranty, express or implied, representation or otherwise in respect of this report and its contents. For greater certainty, the Alberta Energy and Utilities Board and the Government of Alberta, its officers, employees and agents are exempted, excluded and absolved from all liability for damage for injury howsoever caused, to any person in connection with or arising out of use by that person for any purpose of this report or its contents.

EUB Special Report 12 (July 2001) • iv

CONTENTS Preface ii Introduction 1 Reflectance Spectroscopy 2 Background on Alberta Kimberlites 4 PIMA Mineralogy 7 Common Alteration Minerals – Kimberlites 8 Minerals in this Sample Suite ASHK01 14 ASHK02 16 ASHK03 18 ASHK04 20 ASHK05 22 ASHK06 25 ASHK07 27 ASHK08 29 ASHK09 31 ASHK10 33 ASHK11 34 ASHK12 38 ASHK13 40 ASHK14 42 ASHK15 44 ASHK16 47 Summary/Discussion 50 References 52 Appendix A 55 Drill Logs (Buffalo Head Hills) Appendix B 70 PIMA Mineral Identification Logs

EUB Special Report 12 (July 2001) • 1

INTRODUCTION

This report contains data collected with the PIMA� portable infrared spectrometer from a sample suite of kimberlite and ultramafic cores from Alberta, Canada, including 14 core samples from the Buffalo Head Hills kimberlite field, one core sample from the Mountain Lake diatreme, and one hand sample from the Black Butte minette. The suite was supplied by the AGS. There were a number of objectives for the work. These include, to generally demonstrate the operation of the PIMA� portable Short Wave Infrared (SWIR) spectrometer, to evaluate the applicability of the SWIR analytical method to kimberlite alteration minerals, and to show the usefulness of PIMA� for logging core. This was accomplished using core samples and one hand sample. A brief overview of reflectance spectroscopy and how it relates to alteration mineralogy and zoning is provided as background. The infrared active minerals observed in the samples are summarized using reference spectra from SPECMIN�, to represent “ideal” examples of the spectra of these alteration minerals. This report illustrates how PIMA� is a convincing tool for the identification and evaluation of alteration minerals found in kimberlites. The Short Wave Infrared (SWIR) technique is extremely sensitive to alteration minerals such as clays, carbonates and selected sulfates, and phyllosilicates such as serpentines and amphiboles. It can track elemental substitution and changes in order or crystallinity in the minerals. In hydrothermal deposits, this is often an indicator of temperature changes in the alteration halo. It is also useful for examining weathered surfaces, and weathering profiles. In kimberlites it appears to be able to discriminate between the two alteration types common to these complex rocks: deuteric alteration, and weathering from meteoric and/or ground water activity.


SWIR REFLECTANCE SPECTROSCOPY Reflectance Spectroscopy has been used by chemists for years. It was “re-discovered” by the remote sensing discipline. Sensors such as Thematic Mapper on the Landsat V Satellite, the NASA-JPL aircraft based scanner AVIRIS (Airborne, Visible, InfraRed, Imaging Spectrometer) and various commercial aircraft systems all use information from the visible through short infrared bands for mapping, vegetation investigation, mineral exploration and environmental monitoring. Geologists are beginning to recognize that this method has far reaching applications beyond remote sensing, especially in mineral exploration, core logging, alteration zone delineation and lithology mapping.

Reflectance spectroscopy can be defined as the technique that uses the energy in the Visible (0.4-0.7µm), Near Infrared (0.7-1.3µm) and Short Wave InfraRed (1.3-2.5µm) wavelength regions of the electromagnetic spectrum to analyze materials. Certain atoms and molecules absorb energy as a function of their atomic structures. The manifestation of this takes the form of a reflectance spectrum, with absorption features, positions and distinctive profiles that can be used to identify mineral and organic phases. Each mineral detected within the SWIR region has a fairly unique set of spectral characteristics combined into this reflectance spectrum. The features have characteristic frequencies or wavelength positions and bandwidths. Both the spectral features and the hull or background component are influenced by multiple variables, the presence of which (such as iron oxides) are not always visibly detectable within the SWIR wavelength region of 1.3 to 2.5 µm.

The reflectance properties, particle size, degree of sample orientation, presence of surface water and interlayer water, associated organic and inorganic phases, particle orientation, degree of structural ordering, data collection and instrument parameters all influence the spectral curve and absorption features. The profile of the feature is also of great importance as this will change with changes in the listed variables.

SWIR is particularly sensitive to the clay minerals and selected other alteration minerals such as carbonates, jarosites, alunites, pyrophyllite and chlorites. Therefore the application to exploration becomes apparent as these are usually pivotal minerals for defining a deposit type. This sensitivity is a function of the molecules present in the mineral phases, especially water, hydroxyls and carbonate. Table I summarizes the common mineral groups detected by SWIR and the positions of their major spectral features.


Table 1. Major Absorption Features.

POSITION MOLECULE MINERAL/COMPOUND ~1.4 µm OH and WATER ILLITE, KAOLINITE, SMECTITE BERYL, ZEOLITES, BRUCITE PYROPHYLLITE, GIBBSITE, TALC 1.4µM ATMOSPHERIC WATER 1.4-1.48 OH ALUNITE, GYPSUM, JAROSITE ~1.56µM NH4 AMMONIUM-BEARING SPECIES 1.76 -1.82µM WATER ALUNITE, JAROSITE, GYPSUM ~1.9 µM MOLECULAR WATER SMECTITE, BERYL, ZEOLITES 1.9 µM ATMOSPHERIC WATER ~2.02, 2,12µM NH4 AMMONIUM-BEARING SPECIES ~2.15-2.2µM B-O BORATE ?? ~2.18µM P-O-H PHOSPHATE ?? ~2.2 µM Al-OH SMECTITE, KAOLINITE, ILLITE ALUNITE, JAROSITE, MICAS AMPHIBOLES, SERPENTINE 2.2-2.6µM Fe(OH) CHLORITE JAROSITE, FE-ILLITE 2.24-2.26 Si(OH) OPALINE SILICA ~2.3µM Mg(OH) AMPHIBOLES, CHLORITE, MICAS, TALC, EPIDOTE ~2.29 - 2.35µM CO3-2 CARBONATES ~2.38µm P-O-H PHOSPHATE ??


BACKGROUND

Buffalo Hills Kimberlites. (The following is abstracted from a talk given by Ashton Mining of Canada Inc. (ACA - TSE/ME) to the Vancouver Mining Exploration Group and also to the Cordilleran Roundup meeting in January of 1999. It is provided here as background material. Authors were not cited in the Internet documents.) The Buffalo Hills kimberlite province is located in north-central Alberta and represents a new kimberlite province discovered in 1997. To date 14 kimberlites have been discovered with inferred surficial areas. Diamonds have been recovered from small (~ 50 kg) core samples from 10 of the 14 kimberlites. Exploration for diamonds in Alberta is still in the early stages of evaluation.

Early in 1996 Pure Gold and its Joint Venture partners began diamond exploration on the Buffalo Head Craton in North Central Alberta, an area that remained essentially unexplored for its diamond potential. By the end of 1997, a new kimberlite province representing a significant discovery in the history of worldwide exploration was unfolding. To date, thirty-two kimberlite pipes have been discovered roughly in the middle of the Buffalo Head Craton by the Ashton/Alberta Energy/Pure Gold Joint Venture. The majority of the newly discovered pipes are diamondiferous. Kimberlites of the Buffalo Hills province intrude a sequence of Devonian and Cretaceous sedimentary rocks overlying the Proterozoic basement, with U-Pb dating of kimberlitic perovskite indicating ages of approximately 86 to 88 Ma for tested pipes. Intrusion of the bodies apparently occurred before complete lithification of the


Cretaceous Shaftesbury Formation, which forms the host unit at surface for many of the kimberlites. Pipe surface expressions range from <1 to ~45 hectares in area, with several of the pipes forming distinct outcrops in an otherwise low-relief region. Continuation of the bodies at depth is supported by seismic profiles, which confirm a pipe-like morphology. All of the kimberlite intersected to date consists entirely of crater facies, which has been identified at depths of up to 200 meters (the maximum permitted drill hole depth in the area, without requiring special blowout protection for drill rigs) in the more heavily drilled bodies. Lapilli-bearing olivine crystal tuffs are predominant, with occasional distinct bedding containing wide variations in average grain size. Local intercalations with the host Shaftesbury shales may also be present. Mineralogy is dominated by macrocrystalline olivine, with phlogopitic mica forming a relatively minor constituent. Apatite, perovskite, spinel, and mica form the microphenocryst assemblage, with a fine-grained, sometimes segregational mix of carbonates, serpentine, and chlorite forming the groundmass. Compositional trends of spinel and mica phenocrysts have been found to be representative of Group I kimberlites. Indicator mineral populations from each of the pipes include peridotitic garnet, chromian spinel, chromian augite, and lesser picroilmenite and eclogitic garnet. Pyropic garnet compositions most frequently suggest a lherzolitic source region, with higher chromium, subcalcic ("G10") pyrope being a relatively minor constituent. Mantle xenoliths define a similar, lherzolitic contribution. Chromian spinel of diamond inclusion composition varies in abundance from pipe to pipe. Sixteen of the Buffalo Hills kimberlites have been found to be diamondiferous. A significant macrodiamond population, including larger stones displaying resorption features, has been identified in five of the kimberlites (K5, K6, K11, K14, and K91). A preliminary grade of 17.5 carats per tonne has been proposed for the K14 kimberlite, and work is continuing on the evaluation of a 450 tonne bulk sample drilled in early 1998. The Buffalo Hills kimberlites were first detected on a fixed-wing aeromagnetic survey conducted during February and March of 1995. The 600 m flight line data was acquired by Alberta Energy Company to assist in the interpretation of the Precambrian basement grain for oil and gas exploration. The 64,000 km2 of survey data was dominated by deep long-wavelength features. However, 10, shallow, high-frequency anomalies (not related to culture) were also observed in the data. An investigation of pre-existing seismic profiles in the vicinity of these anomalies revealed very strong diffractions and atypical reflections, suggesting that the anomalies might be the result of disruptive volcanic intrusives. Mountain Lake Diatreme


Kimberlitic pipes were first discovered by Monopros Ltd. in 1990 in the Mountain Lake area, in the Peace River Arch region, about 75 km east-northeast of Grande Prairie. The pipes occur within the Wapiti Formation, and are believed to be about 68 Ma (mid-Maastrichtian) in age. One sample from Mountain Lake (ASHK15) is analyzed in this report. The Mountain Lake kimberlitic bodies consist of extrusive volcaniclastics, either juvenile-rich volcaniclastics (dominated by altered olivine), or quartz-rich volcaniclastics. The pipes contain low abundances of chromite, chrome diopside, and garnet, and are uneconomic (Wood et al, 1998). Black Butte Minette The Black Butte minette, part of the Sweet Grass Intrusive suite (Eocene), occurs in the Milk River area, near the Alberta-Montana border. Exposed outcrops at Black Butte consist of dark to light grey minette intrusives, with no extrusive volcanics occurring (Kjarsgaard, 1994). One hand sample from Black Butte (ASHK16) is included in this report.


PIMA MINERALOGY

The following section summarizes the infrared active mineralogy for 14 drill core samples from the Buffalo Head Hills kimberlite field, one core sample from the Mountain Lake diatreme, and one hand sample from Black Butte minette.

Table 2. Sample Suite for PIMA Analysis

Sample ID

Description

ASHK01 Buffalo Head Hills, kimberlite K1 DDH 1A-01 08-08-089.12W5ASHK02 Buffalo Head Hills, kimberlite K4 DDH 4A-02 10-32-09011 ASHK03 Buffalo Head Hills, kimberlite K5 DDH 5A-02 08-14-091-11W5ASHK04 Buffalo Head Hills, kimberlite K1 DDH 1B-02 07-08-089-12W5ASHK05 Buffalo Head Hills, kimberlite K4 DDH 4B-01 07-32-090-11W5ASHK06 Buffalo Head Hills, kimberlite K6 DD6-02 15-19-091-10W5ASHK07 Buffalo Head Hills, kimberlite K2 DDH2-01 05-22-089-12W5ASHK08 Buffalo Head Hills, kimberlite K4 DDH 4C-01 09-32-090-11W5ASHK09 Buffalo Head Hills, kimberlite K7 DDH 7A-01 11-36-091-11W5ASHK10 Buffalo Head Hills, kimberlite K14 DDH 14-01 13-12-092 11W5ASHK11 Buffalo Head Hills, kimberlite K19 DDH 19-03 03-25-089-12W5ASHK12 Buffalo Head Hills, kimberlite K91 DDH91-03 03-23-092-11W5ASHK13 Buffalo Head Hills, kimberlite K7 DDH 7C-01 05-01-992-11W5ASHK14 Buffalo Head Hills, kimberlite K7 DDH 7B-01 04-01-092-11W5ASHK15 Mountain Lake diatreme ML 02-91 12-36-74-25W5 ASHK16 Black Butte minette SW 18-01-

08W4 hand sample

Reference spectra from the SPECMIN� database for the common infrared active minerals observed in kimberlites are first compiled as a background to understanding the spectra from the Buffalo Head Hills samples. Selected references are included at the end of the mineral identification section as further background. Drill core logs of the Buffalo Head Hills samples (ASHK01-ASHK14, above) are given in Appendix A. The drill data are derived from the Assessment Report by Skelton and Bursey (1998).


COMMON ALTERATION MINERALS

KIMBERLITES The common infrared active alteration minerals for selected Canadian kimberlites include carbonates, phlogopite, biotite, chlorite, serpentine, richterite, talc, septechlorite. smectite and saponite.

Figure 1 - The most common alteration minerals observed in the Buffalo Hills sample suite include (in order plotted above) [A] serpentine, [B] calcite, [C] phlogopite, [D] biotite, [E] chamesite, [F] clinochlore, [G] saponite. Vertical scale is in % reflectance. Of this group of minerals, those most likely to be detectable by an airborne (hyperspectral) sensor include serpentine, carbonates, chlorites and smectites.


SERPENTINES

Figure 2. Different species of serpentine: [A] antigorite (Mg, Fe2+)7Si8O22(OH)2, [B] cerolite [C] chyrsotile, Mg3Si2O5(OH)4 and [D] williamsite (Ni,Mg)3Si4O10(OH)2. The red line highlights the diagnostic absorption feature, which shifts slightly as a function of major cation composition.


CHLORITES and VERMICULITE

Figure 3. Additional standards to match against the species identified from the sample suite. These include [A] vermiculite, [B] chamesite – Fe-chlorite, [C] ripidolite – Fe>Mg chlorite, [D] chlinochlore = Mg-chlorite, [E] sheridanite – Mg>Fe chlorite. Vermiculite is a weathering product of chlorite.


BIOTITE, PHLOGOPITE and SAPONITE

Figure 4. Spectra for [A] biotite, [B] phlogopite, [C] Mg-saponite, [D] Fe-saponite. The saponites are swelling clays in the smectite family.


Table 3. Summary of the Minerals Detected by Infrared Spectroscopy.

Sample ID Sap Ser CO3 Apo Gyp Ver Chl Mg Non Amp Description

ASHK01 DDH 1A-01 x tr x Grey green nodules, fine grd mtx/black sh?

ASHK02 DDH 4A-02 M tr oxidized bleached tan

ASHK03 DDH 5A-02 x fine grained grey-green mtx

ASHK04 DDH 1B-02 x x grey-tan mtx, white stringers

ASHK05 DDH 4B-01 x x fine grey-green matrix

ASHK06 DD6-02 x V fine gry, green mtx,white clst

ASHK07 DDH2-01 x ? x gry, fn mtx w/variable sz clasts

ASHK08 DDH 4C-01 x sandy-tan, wht mtx, gry green grains

ASHK09 DDH 7A-01 x med grey, very fine grains, silic

ASHK10 DDH 14-01 x ?? grey-green mtx - multiple clasts large white clast

ASHK11 DDH 19-03 x x muddy brn,arglzd mtx- clsts

ASHK12 DDH91-03 x ? grey, green fine mtx, lg clasts

ASHK13 DDH 7C-01 ??? ??? tan, ornge mtx-oxidized lg

clsts Smectite , saponite?? CO3??

ASHK 14 DDH 7B-01 x x fi gr gry mtx, wht grains, blk

sh clsts

ASHK 15 ML 02-91 x gry grn matrix, silic dense,clsts

ASHK 16 SW 18-01- 08W4 x x x

green, gd mass,brown, mica in mtx; amphibole, vermiculite,nontronite

Key: Sap = Saponite: Ser = Serpentine; CO3 = Carbonate; Apo = Apophyllite; Gyp =

Gypsum; Ver = Vermiculite; Chl = Chlorite; Mg = Mg-silicate; Non = Nontronite; Amp = Amphibole


Table 4. Samples Plotted Relative to Depth and Mineralogy

Sample ID Depth Sap Ser CO3 Apo Gyp Chl Mg

ASHK10 DDH 14-01 14.65 x ?? ASHK11 DDH 19-03 14.65 x x ASHK02 DDH 4A-02 49.15 M tr ASHK13 DDH 7C-01 58.40 Sm ??? ASHK07 DDH2-01 59.13 x ? x ASHK08 DDH 4C-01 63.00 x ASHK04 DDH 1B-02 66.15 x x ASHK01 DDH 1A-01 76.70 x tr x ASHK14 DDH 7B-01 76.93 x x ASHK03 DDH 5A-02 84.23 x ASHK12 DDH91-03 84.93 x ? ASHK06 DD6-02 110.15 x ASHK09 DDH 7A-01 119.00 x ASHK05 DDH 4B-01 140.65 x x

Some useful trends for the prediction of mineral distribution in drill core can be seen in this sample suite. There are too few samples to make any generalizations, however, it appears that saponite is found in the upper half of the core, along with the altered Mg-silicate. Serpentine is more likely to occur in the lower depths. Chlorite is somewhat ubiquitous, but seems to be in the lower half of the core. Carbonate is found in the upper half. It is certainly useful to be able to tie the alteration minerals to core depths, and in that way determine where the alteration types change.


Sample ASHK01 DDH 1A-01 08-08-089-12W5 76.7m This sample (an olivine lapilli tuff) is very altered, with saponite and chlorite occurring. The saponite is particularly indicative of a high magnesium environment.


Several spectra were run for this sample. This is a summary table of the minerals detected.

Sample

ID Sap Chl Mg Mineral Description

ASHK01 DDH 1A-01 08-08-089.12W5 76.7m

Grey green nodules - diff sizes, fine grn mtx/ black sh?

a x tr saponite? tr chlorite? matrix b x tr saponite, tr Mg silicate matrix c silica? black nodule d x tr saponite, tr Mg silicate fract surface - whitish e x x saponite, tr chl, Mg silic

The plot below compares a saponite reference (black) against sample ASHK01 (red).


Sample ASHK02 DDH 4A-02 10-32-09011 49.15m This sample of altered kimberlite is strongly oxidized. It contains poorly crystalline magnesite (red arrow) and very minor gypsum (blue arrow).


Several spectra were run for this sample. This is a summary table of the minerals detected. Sample

ID CO3 Gyp Mineral Description

ASHK02 DDH 4A-02 10-32-09011 Buffalo Hills Assmt. Rpt MIN 9815

a M magnesite oxidized bleached tan, v silic w/qtz trans grains

b M tr magnesite, trace gypsum matrix w/quartz grains c M tr magnesite, trace gypsum large spongy area - leached? d M magnesite small spongy area

The presence of the magnesium carbonate, shown here as a reference in black over the sample in red, indicates a high magnesium environment.


SAMPLE ASHK03 DDH 5A-02 08-14-091-11W5 84.23m

The infrared active mineral in this sample (volcaniclastic kimberlite) is serpentine. It is not highly altered. There are low amounts of serpentine present. The clasts are also serpentine.



ID Ser Mineral Description

ASHK03 DDH 5A-02 08-14-091-11WS Buffalo Hills Assmt. Report Min 9815

a x serpentine fine grained grey-green matrix, silicified matrix b x serpentine small swarm grains, lighter alt grains, more clay c x serpentine edge of core - lighter grain d x serpentine light color, elongated clast

The plot shows the serpentine reference in black plotted against the unknown in red.


SAMPLE ASHK04 DDH 1B-02 07-08-089-12W5 66.15m The alteration is not intense in this sample (olivine lapilli tuff). It consists of calcite (blue) and chlorite (green). The white stringers appear to be calcite.



Sample ID

CO3 Chl Mineral Description

ASHK04 DDH 1B-02 07-08-089-12W5 grey-tan mtx, small grain swarms, white

diagonal stringers a ? ? chlorite? CO3 matrix - grey, tan, fine grained b C x CO3 - chlorite white stringers c C ? chlorite? CO3 darker, circular area d tr x chlorite, trace

calcite nodules and stringers

The plot below demonstrates some of the problems with mineral identification and especially with carbonates and chlorites. Iron chlorite (top spectrum) has very similar wavelengths to calcite (bottom spectrum reference). There is a plateau in the 1900nm feature that indicates chlorite.


Sample ASHK05 DDH 4B-01 07-32-090-11W5 140.65m This kimberlite is not very altered. The spectra have low reflectance implying low concentrations. There is serpentine present, and possibly some chlorite. There are obvious mica grains. These could be altered to chlorite. This core is from fairly deep in the hole.



ID Ser Chl Mineral Description

ASHK05 DDH 4B-01 07-32-090-11W5 Buffalo hills Assmt. Report 9815

very low reflectance different serpentine

fine grey-green matrix, large mica grains - fresh?

a x ? chrysotile? chlorite matrix b x chrysotile end - mica grains c x ? chrysotile? chlorite matrix with mica grains d x ? chrysotile? chlorite end - mica grains

The noise in the red spectrum (sample) below is a function of the low reflectance. The serpentine reference is shown in black.


This spectral plot shows absolute intensities and plots the reference (top plot) against the sample spectra without a normalizing factor. By this comparison, the low intensities of the sample spectra are contrasted against the reference. The implication is that this rock is not highly altered.

The above plots the sample (black) against the serpentine references (red).


SAMPLE ASHK06 DDH6-02 15-19-091-10W5 110.15m In this sample (olivine-rich kimberlite) an interesting contrast occurs between the matrix [C, D, E] and the clast [A, B]. Both contain serpentine. As can be seen from the plot, the concentrations and crystallinity are very different. This alteration has been very selective to the clasts. In the plot below, the first two spectra were collected from the clast.



Sample ID Ser Mineral Description ASHK06 DD6-02 15-19-091-10W5 110.15m

Buffalo Hills Assmt. Report 9815 very fine grey, green matrix, pervasive alt of

sm grains, mica grains, black shale clasts a x serpentine matrix b x serpentine? large white nodule/clast c x serpentine? large pale clast, side of core d x serpentine? matrix e x serpentine? large white clast

The reference (red) is plotted against the sample (black).


SAMPLE ASHK07 DDH2-01 05-22-089-12W5 59.13m This kimberlite sample is uncut core and somewhat harder to analyze, as the rounded surfaces of the core tend to produce noisier spectra. This sample is very altered. It contains saponite and a magnesium silicate similar to an amphibole.



Sample ID

Sap Chl Mg Mineral Description

ASHK07 DDH2-01 05-22-089-12W5 Buffalo Hills Assmt. Report 9815

uncut piece of core-grey, fine matrix w/variable size clasts, gr

a x x saponite > silicate side of core, large pale clast b x x saponite > silicate edge of core, matrix, fine grey c x x Mg silica > saponite pale green grains, argillized,

rough edge, bad angle d x x saponite > silicate edge again - altered clasts e x ? x saponite > silicate weathered surface

This plot displays the unknown in the center (red) against a saponite (cyan) and the magnesium silicate (green). Note the sharpness of the features in the silicate reference. This silicate pattern (green) was also observed in a mining district in Utah. This sample should be x-rayed as it is an interesting combination of clay and amphibole layers.


SAMPLE ASHK08 DDH 4C-01 09-32-090-11W5 63.0m This sample (altered kimberlite) is primarily serpentine, however, it probably has some chlorite or vermiculitic layers developing because of the very large water feature developed in the 1900nm region (blue arrow). The other indicator of another phase is the slope from ~1500 to ~1850nm. This usually indicates the presence of iron. There could be magnetite in this rock.

There is not a lot of difference between the clast [B] and the matrix [A, C], except that the clast appears to have slightly better crystallinity, as a function of slightly sharper absorption feature definition. The iron slope is indicated by the red arrow and the unique water feature by the blue arrow.



Sample ID Ser Mineral Description ASHK08 DDH 4C-01 09-32-090-11W5

Buffalo Hills Assmt. 9815 grainy, sandy - tan, white mtx, arglzd grey

green grains a x serpentine matrix b x serpentine large grey-green clast c x serpentine matrix - end of core

The plot below compares the unknown [B] against two different types of serpentine, antigorite [A] and cernolite [C]. The water feature and the iron slope for the Buffalo Hills sample are still very different from the profiles of the references.


SAMPLE ASHK09 DDH 7A-01 11-36-091-11W5 119.0m This sample (kimberlite breccia) has been pervasively altered to serpentine. However, the matrix [A, B, C] is considerably less altered then the clasts [D]. Note the differences in intensities.



ID Ser CO3 Mineral Description

ASHK09 DDH 7A-01 11-36-091-11W5 Buffalo Hills Assmt. 9815

low reflectance except for "d"

medium grey, very fine grains, silic

a x serpentine fine grey matrix b x serpentine small white stringers around

darker grain c x serpentine end d x serpentine - chrysotile white clast, side of core

This plot of the reference (red) against the sample (black) shows a reasonable match to chrysotile.


SAMPLE ASHK10 DDH 14-01 13-12-092 11W5 14.65m This kimberlite sample is very altered to serpentine and possibly carbonate. It is from a level high in the core profile. This is pervasive alteration as can be seen from the spectra below, which all have similar reflectance even though they are collected from matrix and clasts.



Sample ID

Ser CO3 Mineral Description

ASHK10 DDH 14-01 13-12-092 11W5 Buffalo Hills Assmt. 9815

?? Two Phases, carbonate?

grey-green mtx - multiple clasts, whitish, some zoned?

a x serpentine large white clast b x serpentine small clast xl faces, white c x serpentine end - more matrix - green, fine d x serpentine green matrix, sawn surface e x serpentine swarm of small grains, altered, whitish

The plot below shows the ideal match between the reference (red) and the unknown (black).


This plot is a computer mixture of carbonate and serpentine using spectra from the SPECMIN� reference database. It is mixed in 10% increments. It illustrates how difficult it is to determine the presence of carbonate mixed with serpentine (in proportions less than about 50%). This may require a computer program to provide carbonate percentages. At the least, it requires mixtures such as these to compare and calibrate against. It is easier to detect serpentine mixed with carbonate, and that can be detected in low percentages, possibly less than 10% serpentine.


SAMPLE ASHK11 DDH 19-03 03-25-089-12W5 14.65m This kimberlite sample shows a lower temperature alteration, with saponite and a Mg-silicate mineral occurring. There is a very large water feature indicating high fluid flow through this sample, probably groundwater.



ID Sap Mg Mineral Description

ASHK11 DDH 19-03 03-25-089-12W5 Buffalo Hills Assmt. 9815

solid core - muddy brn, argillized matrix - arglzd clasts

a x x Mg silicate > saponite muddy brown matrix c x x Mg silicate > saponite end - xls/grain swarm d x x Mg silicate > saponite altered grains

This plot shows the sample [B red] bracketed by saponite [A] and Mg-silicate [C] references.


SAMPLE ASHK12 DDH91-03 03-23-092-11W5 84.93m This kimberlite sample is weakly altered. The spectra show low reflectance and are noisy and poorly developed. Serpentine is the dominant mineral with possibly some minor chlorite.



ID Ser Chl Mineral Description

ASHK12 DDH91-03 03-23-092-11W5 Buffalo Hills Assmt. 9815

grey, green fine grained mtx, large clasts, arglzd mtx

a x serpentine matrix w/white altered b x serpentine swarm of grains in white matrix c x ? serpentine ? chlorite

trace argillized white grains

d x ? serpentine large grey - shale? clast e x serpentine white altered clast, side of core

The plot below shows the reference (red) overlain on the sample (black).


SAMPLE ASHK13 DDH7C-01 05-01-992-11W5 58.4m This kimberlite sample is oxidized with large white altered clasts. The alteration is pervasive through the matrix and clasts. There are several mineral phases present. The most easily identified mineral is smectite or montmorillonite (red). There is another clay phase, which could be a nontronite or vermiculite and also there is probably some carbonate, magnesite and/or calcite. The problem is that the absorption features are very small and it is difficult to get an unequivocal identification.



ID Sme CO3 Non Mineral Description

ASHK13 DDH 7C-01 05-01-992-11W5 58.4m Buffalo Hills Assmt. 9815

tan, orange matrix - oxidized large alt white clasts

a x smectite +? CO3? +?? matrix b x smectite +? + CO3? clasts - white c x smectite +? + CO3? swarm, small clasts d x smectite +? + CO3? smaller swarm

This plot overlays several different references on the unknown. The carbonates (magnesite=magenta and calcite=cyan) show the best match.


SAMPLE ASHK14 DDH 7B-01 04-01-092-11W5 76.93m This kimberlite breccia is highly altered. It contains saponite with very minor Mg-silicate. The water feature is quite large indicating low temperature meteoric or ground water alteration.



Sample ID

Sap Mg Mineral Description

ASHK14 DDH 7B-01 04-01-092-11W5 Buffalo Hills Assmt. 9815

fi gr grey mtx w/alt sm white grains, blk shale clasts

a x x saponite, Mg silicate matrix b x saponite matrix c x x saponite, Mg silicate matrix


SAMPLE ASHK15 ML 02-91 12-36-74-25W5 45.0m (Mountain Lake) This sample is quite different from the Buffalo Hills suite. It contains a mixture of apophyllite and the Mg-silicate mineral seen in the Buffalo Hills samples. This implies a zeolitic phase. The rock is very dense. There has been alteration and a moderate-sized water feature has developed.



ID Apo Mg Mineral Description

ASHK15 ML 02-91 12-36-74-25W5 Mountain Lake AR Min 9404, GSC OFR 3441

grey green matrix, arglzd, silic dense, small phenos/ clasts, alt grains - some large, others obviously clay

a x Mg silicate matrix b tr x Mg silicate, tr

apophyllite matrix

c x x Mg silicate + apophyllite

large clast, alt - side of core

d x x apophyllite + Mg silicate

large clast, altered, side of core (could be distorted)

e x apophyllite large clast, altered, side of core (could be distorted)

This shows the unknown (black) against the apophyllite reference (red).


This plot shows the alteration of the Mg-silicate to saponite. This would indicate low temperature alteration. Note how the profiles of the absorption features change from very sharp to broader as the mineral phase changes form the higher temperature magnesium silicate to the lower temperature, less ordered saponite, clay mineral.


SAMPLE ASHK16 SW 18-01-08W4 hand sample (Black Butte)

This hand sample is a very interesting rock (minette). It contains an iron-amphibole (red) altering to vermiculite (green) and probably a magnesium-bearing nontronite or an iron-bearing saponite (blue).



ID Depth Ver Non Amp Mineral Description

ASHK16 Hand Spl

SW 18-01-08W4 Black Butte ARM 9522

green, gd mass w/brown, mica in matrix

a x x amphibole + vermiculite

mica flake

b x nontronite? nodule, brown-white

c x x amphibole + vermiculite

large brown mica flake

d x x amphibole + vermiculite

large brown flake

e x x amphibole + vermiculite

large brown flake

f x x amphibole + vermiculite

matrix - green

The sample [B] is plotted in red against a saponite-Mg reference [A] and vermiculite [C]. Note the large water feature, which is usually associated with vermiculite. The iron slope also indicates the presence of iron, which would be in vermiculite.


These plots show various iron-bearing amphiboles against the unknown. The best match is hornblende.

The plot below matches the unknown (black) against nontronite references (red). The unknown has slightly different chemistry as the wavelengths do not match exactly.


SUMMARY/DISCUSSION This is a small sample population and therefore it is difficult to make any type of general conclusions about patterns of alteration. However, having said that, it is possible to make some observations on the trends observed in the samples, and to make suggestions about future work with reflectance spectroscopy that will provide substantive data for these observations. The fact that trends can be discerned, and distinguishable differences within such a small sample suite, is most encouraging for the application of the method to the characterization of kimberlite alteration systems. There are two different infrared active mineral suites observed in the Buffalo Hills samples. The first is dominated by serpentine, and the samples are almost always confined to the lower depths of these drill holes. It is difficult to correlate other minerals unequivocally with the serpentine. Given the origins and mechanisms involved, chlorite may be the only logical phase. Calcite is also a consideration, however, it appears to be confined to the upper regions of the cores. This does allow the speculation that alteration of previously consolidated kimberlite by fluids that deposited serpentine plus possibly calcite may result in the development of “modified kimberlites”, whose magnetic signature may vary and essentially differentiate them from unaltered kimberlite. The upper core sections are characterized, in this suite, by saponite (Mg-smectite – swelling clay), carbonates, (which are somewhat difficult to speciate because of interference from other Mg-bearing phases), chlorite and a Mg-silicate mineral that has similar structure to an amphibole. The Mg-clay, chlorite and amphibole all can be secondary, alteration products of serpentine. This would explain their presence in the upper regions of the core and also provide excellent pathfinders for the transition between the different alteration “zones”. Because of the extra water content (contained in clays), these minerals have a diagnostic signature, which can be exploited in kimberlite exploration, using both geophysical and hyperspectral remote sensing techniques . A very important area of investigation to pursue is whether alteration types can be used to characterize diamond-bearing zones from barren zones. There are very definite differences between the Buffalo Head Hills, Mountain Lake (documented as an alkaline ultrabasic volcanic) and Black Butte (minette) kimberlites. Since there is only one sample from each of the other two locations, it is only possible to document that those differences exist. The Black Butte sample shows a much higher iron content and consequent mineralogy. It appears to have come from the secondary alteration zone and shows an iron smectite as opposed to the magnesium smectite or saponite observed form a hypothesized similar zone in Buffalo Hills. The Black Butte sample is possibly more altered as it contains a vermiculitic mineral, which carries more water then an amphibole and some clays.


The Mountain Lake sample is more similar to Buffalo Hills in that the secondary minerals are magnesium-bearing. This short study demonstrates the potential of this technique for kimberlite exploration. The combination of spectral, geochemical (trace and stable isotope), and petrological work may help to distinguish serpentine and carbonate characteristics of primary (magmatogenic), hydrothermal-metasomatic, and extensive secondary processes. This can lead to the development of an effect tool for rapid reconnaissance of kimberlite rocks.


SELECTED REFERENCES

Atkinson, W.J. (1988): Diamond exploration philosophy, practice, and promises: a review; in Proceedings

of the Fourth International Kimberlite Conference, Kimberlites and Related Rocks, Their Mantle/crust Setting, Diamonds and Diamond Exploration, Ross, J., Editor, Geological Society of Australia, Special Publication 14, v.2, p. 1075-1107.

Averill, S.A. and McClenaghan, M.B. (1993): Distribution and character of kimberlite indicator minerals in

glacial sediments, C14 and Diamond Lake kimberlite pipes, Kirkland Lake, Ontario; Geological Survey of Canada, Open File 2819, 46 p.

Carlson, S.M., Hillier, W.D., Hood, C.T., Pryde, R.P., and Skelton, D.N. (1998): The Buffalo Hills

Kimberlite Province, north-central Alberta, Canada; in Seventh International Kimberlite Conference, Cape Town, South Africa, Extended Abstracts, p. 138-140.

Clement, C.R., Harris, J.W., Robinson, D.N., Hawthorne, J.B. (1986). The De Beers kimberlite pipe - a

historic South African diamond mine; in Mineral Deposits of South Africa, C.R. Anhaeusser and S. Maske, Editors, Geological Society of South Africa, Johannesburg, South Africa, p. 2193 -2214.

Clement, C.R. and Reid A.M. (1989): The origin of kimberlite pipes: an interpretation based on a

synthesis of geological features displayed by southern African occurrences; Geological Society of Australia Special Publication 14, p. 632-646.

Cox, D.P. (1986): Descriptive model of diamond pipes; in Mineral Deposit Models, Cox, D.P. and Singer,

D.A., Editors, U.S. Geological Survey, Bulletin 1693, 379 p. Dawson, J.B. (1971). The genesis of kimberlite; in Diamond Research for 1971, p. 2-7. Demaiffe, D., Fieremans, M., Fieremans, C. (1991): The kimberlites of central Africa: a review; in

Magmatism in Extensional Structural Settings, the Palaeozoic African Plate, Kampunzu, A.B. and Lubala, R.T., Editors, Springer Verlag, Berlin, p. 537-559.

Dufresne, M.B., Eccles D.R., McKinstry, B., Schmitt, D.R., Fenton, M.M., Pawlowicz, J.G., Edwards,

W.A.D. (1996): The diamond potential of Alberta; Alberta Geological Survey, Bulletin 63, 158p. Eggler, D.H. (1989): Kimberlites: how do they form; in Kimberlites, related rocks, Ross, J., Editor,

Geological Society of Australia Special Publication, v. 1, p. 489-504. Field M. and Scott Smith B.H. (1998): Contrasting geology and near-surface emplacement of kimberlite

pipes in southern Africa and Canada: in Seventh International Kimberlite Conference, Cape Town, South Africa, Extended Abstracts.

Fipke, C.E., Gurney, J.J. and Moore, R.O. (1995): Diamond exploration techniques emphasizing indicator

mineral geochemistry and Canadian examples; Geological Survey of Canada, Bulletin 423, 86 p. Garanin, V.K., Kudryavtseva, G.P., Janse, A.J.A. (1993). Vertical, horizontal zoning of kimberlites; in

Proceedings of the Eighth Quadrennial IAGOD Symposium, Ottawa 1990, Maurice, Y.T., Editor, Schweizerbart'sche Verlagsbuchhandlung, Stuttgart, p. 435-443.

Geological Survey of Canada (1989): The development of advanced technology to distinguish between

productive diamondiferous and barren diatremes; Geological Survey of Canada, Open File 2124, 1183 p.


Godwin, Colin I. and Price, Barry J. (1986). Geology of the Mountain Diatreme Kimberlite, Northwest Territories; in Geology of Mineral Deposits in the Northern Canadian Cordillera, Canadian Institute Mining Metallurgy, Special Volume.

Gurney, J.J. (1989): Diamonds; in Proceedings of the Fourth International Kimberlite Conference,

Kimberlites and Related Rocks, Their Mantle/crust Setting, Diamonds and Diamond Exploration, Ross, J., Editor, Geological Society of Australia, Special Publication 14, v.2, p. 935-965.

Harris, J.W. (1992): Diamond geology; in Physical Properties of Natural, Synthetic Diamonds, p. 345-392. Hawthorne, J.B. (1975): Model of a kimberlite pipe; Physical Chemical Earth, v. 9, p.1-15. Jacques, A.L., Ferguson, J. and Smith, C.B. (1984): Kimberlites in Australia; in Kimberlite Occurrence and

Origin: A Basis for Conceptual Models in Exploration, Glover, J.E. and Harris, P.G., Editors, Department of Geology and University Extension, University of Western Australia, Publication No. 8, p. 227-274.

Janse, A.J.A., Sheahan, P. (1995): Catalogue of worldwide diamond, kimberlite occurrences: a selective,

annotative approach; in Diamond Exploration: Into the 21st Century, Griffin, W.L., Editor, Journal of Geochemical Exploration, v. 53, p. 73-111.

Jennings, C.M.H. (1990): Exploration for diamondiferous kimberlites, lamproites; in Beck,L.S. and Harper

, C.T., Editors, Modern Exploration Techniques, Saskatchewan Geological Society, Special Publication No. 10, Regina, p. 1192-1203.

Jennings, C.M.H. (1995): The Exploration Context for Diamonds; Journal of Geochemical Exploration, v.

53, p. 113-124. Kingston, M.J. (1989): Spectral reflectance properties of kimberlites, carbonatites: implications for remote

sensing for exploration; in Kimberlites, Related Rocks, Ross, J., Editor, Blackwell, Melbourne, p. 1135-1145.

Kjarsgaard, B.A. (1994): Potassic magmatism in the Milk River area, southern Alberta: petrology and

economic potential; Geological Survey of Canada, Current Research 1994-B, p. 59-68. Lehnert-Thiel, K., Loewer, R., Orr, R., Robertshaw, P. (1992): Diamond-bearing kimberlites in

Saskatchewan, Canada: the Fort a la Corne case history. Exploration and Mining Geology,1; 4, p. 391-403.

Lorenz, V. (1973): Formation of maar-diatreme volcanoes and its relevance to kimberlite pipes. -

Int.Conference on Kimberlites, Cape Town, South Africa, Ext. Abstracts, p. 203-205. Lorenz, V. (1985): Maars, diatremes of phreatomagmatic origin: a review. Trans. Geol. Soc. S Afr., 88, p.

459-470. Lorenz, V. (1986): On the growth of maars, diatremes, its relevance to the formation of tuff rings. Bull.

Volcanol., 48: 265274. Lorenz, V., Zimanowski, B., Buettner, R., and Kurszlaukis, S., 1999: Formation of Kimberlite Diatremes by

Explosive Interaction of Kimberlite Magma with Groundwater: Field and Experimental Aspects. - Proc. 7th Int.Kimberlite Conf., Cape Town, South Africa, 1998, in press.

Meyer, H.O.A., 1976. Kimberlites of the continental United States. A review. J. Geol., 84: 377-403.

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Michalski, T.C. and Modreski, P.J. (1991) Descriptive Model of Diamond-bearing Kimberlite Pipes; in Some Industrial Mineral Deposit Models: Descriptive Deposit Models, editors, Orris, G.J and Bliss, J.D., U.S. Geological Survey, Open-File Report 91-11a, pages 1-4.

Mitchell R.H. 1986. Kimberlites- Mineralogy, geochemistry, and petrology. Plenum, New York, 442 pp. Mitchell R.H. 1995. Kimberlites, orangeites, and related rocks. Plenum, New York, 410 pp. Mitchell R.H. 1997. Kimberlites, Orangeites, Lamproites, Melilitites, and Minettes: A Petrographic Atlas.

Almaz Press Inc, 243 pp. Mitchell R.H. & Bergman S.C. 1991. Petrology of lamproites. Plenum, New York, 447 pp. Pieters, C.M. and Mustard, J.F., (1985). Spectroscopy of Moses Rock Kimberlite Diatreme, Proc. Airborne

Imaging Spectrometer Data Analysis Workshop (G. Vane and A. Goetz Eds.), JPL publication 85-41, p. 106-110.

Scott Smith B.H., Orr R.G., Robertshaw P. & Avery R.W. 1994. Geology of the Fort a la Corne

Kimberlites, Saskatchewan. The Sixteenth CIM District 6 Annual General Meeting, Vancouver, British Columbia.

Scott Smith B.H., Orr R.G., Robertshaw P. & Avery R.W. 1998. Geology of the Fort a la Corne

Kimberlites, Saskatchewan. Extended Abstract of the Seventh International Kimberlite Conference, Cape Town, South Africa, 1998

Skelton, D., and Bursey, T. 1998. Assessment Report: Buffalo Head Hills Property (AL01), Ashton Mining

of Canada Inc. Assessment File 19980015, Alberta Geological Survey, 19 p. Skinner, E.W.S. 1989. Contrasting Group I and Group II kimberlite petrology: towards a genetic model for

kimberlites. In Ross, J. et al., eds., Kimberlites and related Rocks, Vol. 1. Geol. Soc. Australia Spec. Pub. 14, pp. 528-544.

Smith C.B., Gurney J.J., Skinner E.M.W., Clement C.R., Ebrahim N. 1985. Geochemical character of

southern African kimberlites: a new approach based on isotopic constraints. Trans. Geol. Soc. S. Afr. 88, pp. 267-280.

Sobolev, N.V., 1971. Mineralogical criteria for diamond prospecting in kimberlites. Geol. Geofiz., 3: 70 -79

(in Russian). Wood, B.D., Scott Smith, B.H., and de Gasparis, S. 1998. The Mountain Lake kimberlitic pipes of NW

Alberta: Exploration, geology and emplacement model. In Extended Abstracts, Seventh International Kimberlite Conference, Cape Town, South Africa.

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APPENDIX A

ASHTON MINING OF CANADA INC. DIAMOND DRILL HOLE SUMMARY LOGS

(modified from Skelton and Bursey, 1998).


Ashton Mining of Canada Inc. Diamond Drill Hole Summary Log

DDH#: 1A-1 Start Date: July 5, 1997 End Date: July 7, 1997 Elevation: 732.50 Hole Length: 160.20 Anomaly #: 1A Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6284752.82 Core Size: HQ Easting: 569562.34 Measure Units: m FROM TO DESCRIPTION

0.00

20.42

99.00

103.20

20.42

99.00

103.20

160.20

OVERBURDEN KIMBERLITE - Crystal (olivine) lapilli tuff. - Grey green, fine grained, composed of rounded and angular olivine (25%-35%) that has Altered to serpentine and carbonate, up to 0.75 x to 0.75cm. Some olivine alters to a brown. Colour; there may be two populations of olivine: one <3.0mm and the other >0.3mm. - Matrix (30%-40%) is granular in appearance and fine grained. - Xenoliths: Angular serpentinized fragments .5cm (20%), angular shale fragments with embayed olivine and well rounded limestone up to 2.5 x 3.0cm. - Lapilli range in size from 0.2 x 3.5mm with the kernels being olivine, other lapilli, and/or shale; several of them are concentric in nature. MUDSTONE & KIMBERLITE - Grey black in colour. - Soft unconsolidated material with kimberlite clasts intermittent throughout. MUDSTONE - With minor sand blebs and interlayered sandstone units. - Mudstone is grey in colour and unconsolidated. - Bedding is 60°to core axis. - 103.20-103.50m is a limestone occurrence, locally vuggy, grey, massive, coral? EOH @ 160.20m.



DDH#: 1B-2 Start Date: July 9, 1997 End Date: July 14, 1997 Elevation: 740.20 Hole Length: 77.42 Anomaly #: 14 Azimuth at Collar: 360.00 UTM Zone: 11 Incline at Collar: -58.00 Northing: 6284586.07 Core Size: HQ Easting: 568989.34 Measure Units: m FROM TO DESCRIPTION

0.00

18.89

66.26

18.89

66.26

77.42

OVERBURDEN KIMBERLITE - Olivine lapilli tuff, grey-green, fine grained, granular in appearance. Matrix comprises 50-60% of the rock. Light grey-yellow lapilli comprise <2%, to 3cm, with irregular and rounded margins. Peridotite nodules present, <1%. Olivine macrocrysts are altered to serpentine with a trace of pyrite. Also present in trace amounts are chrome diopside, pyrope, orange garnet, white mica and wood fragments. Black and green shale xenoliths comprise ~3%. Bedding may be present at 62.00m where a 2cm wide zone shows a change in grain size. The kimberlite-mudstone contact is not well-defined and consists of a zone 30cm wide with intermixed kimberlite and mudstone. MUDSTONE - Grey-brown grading to black-brown downhole, bedding at 68% TCA, with soft sediment deformation features. EOH @ 77.42m.



DDH#: 2-1 Start Date: July 24, 1997 End Date: July 27, 1997 Elevation: 757.45 Hole Length: 227.77 Anomaly #: 2 Azimuth at Collar: 180.00 UTM Zone: 11 Incline at Collar: -60.00 Northing: 6287827.42 Core Size: HQ Easting: 571565.78 Measure Units: M FROM TO DESCRIPTION

0.00

2.72

225.77

2.72

225.77

227.77

OVERBURDEN KIMBERLITE - Very weathered and/or altered volcaniclastic kimberlite, greyish-brown to pale grey in colour, comprised macroscopically of olivine macrocrysts, basement xenoliths, cored lapilli, autoliths, wood fragments, crustal xenoliths, and sand set in a crumbly black matrix which resembles (ordinary) mud. Textures are matrix supported and the rock is generally medium grained. The matrix is moderately carbonate-rich and potentially granular. Definitive sedimentary structures and textures such as bedding planes with deformed surfaces are present. Except in the case of distinctive bedding planes, this kimberlite is poorly to moderately sorted and (within beds) internally structureless. Locally, it is possible to observe individual beds which remain traceable, but which have been disrupted. From the start of the hole to approximately 81m, macrocrysts show some breakage. Below 81m, abundant broken and shard-like olivine indicate common breakage and may suggest rapid and/or turbulent transport of this material. - Intervals of sand and mixed sand-kimberlite occur throughout this hole. From 28.65-43.89m, the kimberlite contains intervals where sand comprises up to 60% of the groundmass. From 43.89-53.13m, only sand, sandstone, shale and mudstone are present. From 55.70-75.32m, sand and sand veins are present within the kimberlite and from 80.57-88.90m a large intersection of shale and sandstone occur. - - SANDSTONE - Some deformation is present. EOH @ 227.77m.



DDH#: 4A-2 Start Date: February 16, 1997 End Date: February 18, 1997 Elevation: 767.02 Hole Length: 51.50 Anomaly #: 4A Azimuth at Collar: 180.00 UTM Zone: 11 Incline at Collar: -60.00 Northing: 6301519.04 Core Size: NQ Easting: 578380.01 Measure Units: M FROM TO DESCRIPTION

0.00

25.75

25.75

51.50

OVERBURDEN ALTERED KIMBERLITE Rock is medium rusty brown to light grey green. Rock is badly weathered – competent in spots. Rock is composed of 80%-90% granular fine grained matrix (carbonate?). Constituents are too small to see with binocular microscope. Remaining ~20% is made up of what remains of badly weathered olivine grains. Chromite is evident as small granular masses with pitchy luster and brown streak. Last 20cm of core exhibit 75-80% altered olivine crystals, light to medium green. Olivine crystals make up a continuous mass, in the spaces between this mass is a fine grained matrix which alternates between calcite and fine grained medium green serpentine. - Xenoliths consisting of shale, carbonate and sandstone (?) are subround to angular and range in size from 2mm to 17mm. Rock ranges from competent to quite broken up. - - EOH @ 51.50m.



DDH#: 4B-1 Start Date: February 19, 1997 End Date: February 21, 1997 Elevation: 785.96 Hole Length: 200.25 Anomaly #: 24B Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6300991.437 Core Size: NQ Easting: 578464.10 Measure Units: M FROM TO DESCRIPTION

0.00

8.50

8.50

200.25

OVERBURDEN KIMBERLITE - Kinberlite ranges in colour from medium rusty brown through light grey-green to Weathered rust brown section extends down to 19.5m. - Rock is composed of 60-70% fragmented, subangular to subrounded olivine crystals that range from 1mm to ~12mm in size and are bright olive green in colour. - At approximately the 83m mark the core begins to exhibit rounded equigranular olivine crystals many of which contain carbonate (calcite?) in their cores. The remaining 40-40% of the rock consists of a fine grained matrix. This matrix is made up mostly of carbonate (25%-30% of whole rock) and approximately 10% of serpentine. The matrix is light grey brown to white to light pale green in colour & vitreous. - Phlogopite is observed to ~1%, crystals range from 1-5mm, are green to copper colour and are subrounded to angular. - Xenoliths consist of sandstone, shale, granitic and carbonate clasts which range in size from 0.5 to 5cm, none of which were observed with reaction rims. - The core is predominately competent. EOH @ 200.25m.



DDH#: 4C-1 Start Date: February 22, 1997 End Date: February 24, 1997 Elevation: 753.12 Hole Length: 105.67 Anomaly #: 4C Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6301274.06 Core Size: NQ Easting: 578821.46 Measure Units: M FROM TO DESCRIPTION

0.00

44.00

77.70

44.00

77.70

105.67

OVERBURDEN ALTERED KIMBERLITE Light brown to greyish yellow, medium grained, highly altered matrix with variable silicification and carbonitization, locally vuggy, incompetent and crumbly. - Variable bedding at 15-70° TCA – interbedded silica and carb alt, trace pyrite with silicification, Unterbedded coarse and fine grained crater facies sequences. 5-10% shale clasts, serpentinized fragments and small lapilli. Shale clasts can reach >10cm anf occasionally display embayment features where olivines have been passed into the shale clast. - Common green mineral – chlorite-antigorite – to 35%, and up to a 15% unaltered olivine towards gradational lower contact. KIMBERLITE - Light green to greyish green, fine to coarse grained, carbonate/serpentine matrix. Generally weakly magnetic. - 35-70% olivine in duel population of phenocrysts and macrocrysts, 10-35% blue green chlorite-antigorite to .1cm. Variable crater facies textures, graded bedding at 70°-90° TCA, beds grade upwards from coarse (olivine packstone) to fine, with localized soft sediment deformation features. - 5-10% shale clasts, serpentized fragments and lapilli. Lapilli contain trace spinel, Shale clasts to >10cm, some with sulfides, can contain embayed olivine grains. - Some Fe staining, occasional tar on fractured surfaces. EOH @ 105.67m.



DDH#: 5A-2 Start Date: February 6, 1997 End Date: February 7, 1997 Elevation: 634.11 Hole Length: 139.29 Anomaly #: 5A(1) Azimuth at Collar: 270.00 UTM Zone: 11 Incline at Collar: -60.00 Northing: 6306035.83 Core Size: NQ Easting: 582687.67 Measure Units: M FROM TO DESCRIPTION

0.00

16.00

23.00

119.31

16.00

23.00

119.31

139.29

OVERBURDEN KIMBERLITE - Greenish-brown, poorly sorted, macrocrystic and lapilli-bearing volcaniclastic kimberlite which has ~10% xenoliths but >15% locally. Displays weak grain orientation @ 45° TCA but is not well-bedded. May show a general coarsening with depth. Macrocrysts comprise 30% and lapilli 10%. Microcrysts are common in the groundmass. BEDDED KIMBERLITE Greyish-green to orangish volcaniclastic kimberlite with occasional coarse breccia intervals. 23-40m: Kimberlite is fine and medium-grained and bedding is not well developed. The rock is composed of 50% olivine microcrysts (generally <2mm), and ~3% small (avg 5mm) black shale xenoliths in a carbonate and serpentine matrix. 40-49m: A very coarse breccia zone, rich in cb, where clasts of carbonate, siltstone and shale reach 40% of the rock volume and 50mm, averaging 20mm. Massive (clasts?) of magnetite are also present. Olivine macrocrysts (to 5mm) and lapilli (to 25mm) are abundant. All olivine is either oxidized or black and altered (to serpentine?). Sorting is very poor in this interval. 49-119.31m: The kimberlite is moderately sorted with much distinctive bedding, generally defined by changes in grain size. In fine-grained beds, olivines measure 2mm or less and these areas contain very little country rock xenoliths or macrocrysts. In coarser beds, (1 to 50mm thickness), country rock xenoliths comprise 40% of the bed, along with 20% olivine macrocrysts and microcrysts, and small lapilli (2%). Bedding is at ~50° TCA.

MUDSTONE -Unlithified sediment. Rock is moderately competent but crumbled, recovery is ~55%. EOH @ 139.29m.



DDH#: 6-2 Start Date: February 1, 1997 End Date: February 3, 1997 Elevation: 574.33 Hole Length: 138.70 Anomaly #: 6(2) Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6308382.71 Core Size: NQ Easting: 585550.18 Measure Units: M FROM TO DESCRIPTION

0.00

74.40

127.00

74.40

127.00

138.70

OVERBURDEN KIMBERLITE - Volcaniclastic kimberlite is dark grey green to light grey green in fresh sections and light rusty buff in the top section. Rock is composed of 65-75% olivine crystals. - Olivine crystals range from 0.5mm to 3mm but the rock is more or less equigranular. Olivines are rounded and seem to be serpentinized with magnetite in their cores. - At top section the cores of the olivine crystals are rusty brown (ankerite?). - The remaining 30-35% of the rock is composed of a fine grained serpentine matrix. However, in some sections of the core fine-grained carbonate composes 5-7% of the core. Black to bronze phlogopites to ≈ 1mm are observed. - Granitic, carbonate, shale and sandstone(?) xenoliths are observed throughout the core (but are absent from 82.9m to 94.5m). Xenoliths are rounded to subangular and reaction halo’s are absent. - Autoliths observed range from 5mm-15mm. Between 111.9m and 121m the rock’s physical appearance changes, in this section it is badly weathered. Xenoliths are still observed. - From 121m to 127m the kimberlite is fresh. MUDSTONE -Unlithified mudstone EOH @ 138.70m.



DDH#: 7A-1 Start Date: January 28, 1997 End Date: January 30, 1997 Elevation: 620.30 Hole Length: 200.25 Anomaly #: 7A Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6311235.65 Core Size: NQ Easting: 583261.72 Measure Units: M FROM TO DESCRIPTION

0.00

69.20

69.20

200.25

OVERBURDEN -Sand, gravel and clay. At 120’ there was a minor artesian flow. KIMBERLITE BRECCIA -Magnetic susceptibility is highest at the top of the DDH. The Kimberlite contains 60-70% olivine, which has been resorbed and is quite rounded. All of the grains exhibit white rims and appear to have been replaced. Magnetite has replaced some of the grain. Serpentine in material is 20-30%. Pyrite is seen throughout as replacement of olivine (especially towards the bottom of the hole) and as a component of the material. -Autoliths are common at the top of the hole, becoming more difficult to identify towards the bottom of the hole. The autoliths can contain 5-10% phlogopite, however there appears to be several generation of autoliths – some of which contain no mica. The phlogopite bearing autoliths are usually more fine grained. Fresh olivine is present in some of the coarse grained autoliths. -Xenoliths are small and are generally not common (<3cm). They appear quite angular and exhibit few alteration halos. Xenoliths are sedimentary and include mostly limestone? (greenish) EOH @ 200.25m.



DDH#: 7B-1 Start Date: January 17, 1997 End Date: January 21, 1997 Elevation: 622.59 Hole Length: 154.53 Anomaly #: 7B Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6312089.27 Core Size: NQ Easting: 583131.36 Measure Units: m FROM TO DESCRIPTION

0.00

34.70

34.70

154.53

OVERBURDEN -Light colored clay containing only a few pebbles. KIMBERLITE BRECCIA -Green to green black. Olivine rich breccia pipe –60-90% olivine with the remaining components comprising xenoliths, carbonate, serpentine and a few oxides. -Olivine grains are resorbed and many exhibit fresh surfaces, especially towards the top of the section. -The olivine grains are generally small (1-3mm) and are found throughout the hole. Py is present as blebs up to 1cm. Carbonate/zeolite replacement is common. -Xenoliths are 0.1 to 50mm in size with the majority approximately 1-2cm. Lithologies include limestone, shale, greywacke, and sandstone. These xenoliths can have reaction rims (especially the limestone). -Autoliths are also very common and can be seen containing xenoliths as well. -The rocks are heavily fractured and broken throughout, generally at 45° TCA and contain many clay seams (<6″). The clay is blue to green to light green. EOH @ 154.53m.



DDH#: 7C-1 Start Date: January 21, 1997 End Date: January 24, 1997 Elevation: 620.31 Hole Length: 92.05 Anomaly #: 7C Azimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6312455.15 Core Size: NQ Easting: 583052.93 Measure Units: m FROM TO DESCRIPTION

0.00

37.20

37.20

92.05

OVERBURDEN -Clay with few pebbles. Lots of water (artesianal flow at bedrock). KIMBERLITE -Rock is buff colored. – light grey to beige brown. -Original texture is often difficult to discern due to the high degree of alteration – rock is very bleached. -Rock is very crumbled and broken in sections while other section are quite competent. -Alteration is pervasive. Autoliths are present and country rock xenoliths are small and not common (<5cm). Both the autoliths and xenoliths have been altered. -Relict olivine is present (grains <5mm) and have been completely replaced. Olivine was approx 60-70%. -Hydrocarbons visible on some fracture surfaces as black patchy coating (never a measure thickness). No mica or oxides visible. -Core often has a sandy, grainy feel. -Below 61.60m the kimberlite is fresher than above and exhibits green-grey color. 30% fresh olivine is retained. Core is more competent is general below this depth. EOH @ 92.05m.



DDH#: 14-1 Start Date: January 24, 1997 End Date: January 27, 1997 Elevation: 620.72 Hole Length: 200.00 Anomaly #: 14 Azzimuth at Collar: UTM Zone: 11 Incline at Collar: -90.00 Northing: 6315049.84 Core Size: NQ Easting: 582882.92 Measure Units: m FROM TO DESCRIPTION

0.00

7.00

7.00

200.00

OVERBURDEN KIMBERLITE -Grey green in color – some light and dark sections; 60-70% olivine – grains are rounded and equigranular (2-3mm). -Olivine is serpentinized and may have magnetite cores. -Remaining 25-30% is a serpentine matrix. -Lapilli are common. -Xenolilths are small (<5cm) and are composed of sandstone, limestone shale. EOH @ 200.00m



DDH#: 19-3 Start Date: July 23, 1997 End Date: Jul 28, 1997 Elevation: 735.94 Hole Length: 204.51 Anomaly #: 19 Azimuth at Collar: 360.00 UTM Zone: 11 Incline at Collar: -58.00 Northing: 6289104.04 Core Size: NQ Easting: 575034.19 Measure Units: m FROM TO DESCRIPTION

0.00

3.66

3.66

204.51

OVERBURDEN KIMBERLITE -Volcaniclastic kimberlite with varying grain size (fine, medium, coarse) and varying concentrations of the constituents olivine macrocrysts, lapilli, crustal xenoliths, mica, wood and indicator minerals. From 3.66-9.83m and 27.92-28.42m the kimberlite is more highly weathered and is light grey. Lapilli are abundant overall and may comprise 30% or more. Olivine macrocysts may comprise 50% of the rock locally. Crustal xenolith concentrations of up to 50% in localized intervals constitute beccia layers. Intermittent mud and mud-sand layers occur but are generally thin and <1m. Calcite veining is common. From 142.33-166.88m sand occurs within the kimberlite as free grains within the groundmass (10-50% of the groundmass). Beneath 166.88m the kimberlite is commonly mud-rich and friable. EOH @ 204.51m.



DDH#: 91-03 Start Date: October 18, 1997 End Date: October 19, 1997 Elevation: 650.25 Hole Length: 145.38 Anomaly #: 91 Azimuth at Collar: UTM Zone: 11 Incline at Collar: 0.00 Northing: 6317052.10 Core Size: NQ Easting: 581819.70 Measure Units: m FROM TO DESCRIPTION

0.00

17.37

125.37

17.37

125.37

145.38

OVERBURDEN -Sandy beige brown clay and mud with round granite boulders up to 5cm. KIMBERLITE -Grey green to dark green. -Lapilli are the dominant textural feature of unit. Texture shows subtle differences as the sizes of lapilli and xenoliths vary. Alteration of olivine macrocysts is variable with some olivine having preserved cores. Lapilli range from 3mm to 2cm in size. Composition is generally 20% olivine phenocrysts, <5% chromite, <5% mica in an aphanitic green serpentine/cb matrix. -Xenoliths make up 10-20% of unit and although mainly black shale, limestone xenoliths were noted throughout the hole. -Trace sulfides occur as replacement in xenoliths or as isolated irregular masses <5mm. -Irregular but sharp lower contact with mudstone. MUDSTONE with KIMBERLITE HORIZONS -Grey-brown, fine-grained, poorly consolidated interbedded mud and silt, bedded at 65-70 degrees TCA, generally <5cm. Non-magnetic. 128.58 – 128.87m KIMBERLITE Olivine crystal tuff with minor lapilli(?) 134.70 – 135.80m KIMBERLITE Olivine crystal tuff, less altered, brecciated near contacts. EOH @ 145.38m.


APPENDIX B

PIMA MINERAL IDENTIFICATION LOGS


Sample ID Depth Sap Ser CO3 Apo Gyp Ver Chl Mg Amp Mineral Description ASHK01 76.7m. DDH 1A-01 08-08-089.12W5

Buffalo Hills Assmt. Report Min 9815 Grey green nodules - diff sizes, fine grd mtx/black sh?

a x tr saponite? tr chlorite? matrix b x tr saponite, tr Mg silicate matrix c silica? black nodule d x tr saponite, tr Mg silicate fract surface - whitish e x x saponite, tr chl, Mg silicate

ASHK02 49.15 DDH 4A-02 10-32-09011 Buffalo Hills Assmt. Rpt MIN 9815

a M magnesite oxidized bleached tan, v silic w/qtz trans grains b M tr magnesite, trace gypsum matrix w/quartz grains c M tr magnesite, trace gypsum large spongy area - leached? d magnesite small spongy area

ASHK03 84.23m DDH 5A-02 08-14-091-11W5 Buffalo Hills Assmt. Report Min 9815 fine grained grey-green matrix, silicified

a x serpentine matrix b x serpentine small swarm grains, lighter alt grains, more clay c x serpentine edge of core - lighter grain d x serpentine light color, elongated clast

Sample ID Depth Sap Ser CO Apo Gyp Ver Chl Mg Amp Mineral Description

ASHK04 66.15m DDH 1B-02 07-08-089-12W5 Buffalo Hills Assmt Rpt Min 9815 grey-tan mtx, small grain swarms, white diag stringers

a ? x chlorite? CO3 matrix - grey, tan, fine grained b C x CO3 - chlorite white stringers c x chlorite? CO3 darker, circular area d C x chlorite, trace calcite nodules and stringers

ASHK05 140.65m DDH 4B-01 07-32-090-11W5 very low reflectance Buffalo hills Assmt. Report 9815 different serpentine fine grey-green matrix, large mica grains - fresh?


a x ? chrysotile? chlorite matrix b x chrysotile end - mica grains c x ? chrysotile? chlorite matrix with mica grains d x ? chrysotile? chlorite end - mica grains

ASHK06 110.15m DD6-02 15-19-091-10W5 Buffalo Hills Assmt. Report 9815 very fine grey, green matrix, pervasive alt of sm grains, mica grains, black shale clasts

a x serpentine matrix b x serpentine? large white nodule/clast c x serpentine? large pale clast, side of core d x serpentine? matrix e x serpentine? large white clast

Sample ID Depth Sap Ser CO Apo Gyp Ver Chl Mg Amp Mineral Description ASHK07 59.13m DDH2-01 05-22-089-12W5

Buffalo Hills Assmt. Report 9815 uncut piece of core-gry, fi mtx w/variable sz clasts, gr

a x x saponite > silicate side of core, large plae clast b x x saponite > silicate edge of core, matrix, fine grey c x x Mg silica > saponite pale green grains, argillized, rough edge, bad angle d x x saponite > silicate edge again - altered clasts e x ? x saponite > silicate weathered surface

ASHK08 63.0m DDH 4C-01 09-32-090-11W5 Buffalo Hills Assmt. 9815 grainy, sandy - tan, white mtx, arglzd grey green grains

a x serpentine matirx b x serpentine large grey-green clast c x serpentine matrix - end of core

ASHK09 119.0 m DDH 7A-01 11-36-091-11W5 low reflectance except Buffalo Hills Assmt. 9815 for "d" medium grey, very fine grains, silic

a x serpentine fine grey matrix b x serpentine small white stringers around darker grain


c x serpentine end d x serpentine - chrysotile white clast, side of core

Sample ID Depth Sap Ser CO Apo Gyp Ver Chl Mg Amp Mineral Description

ASHK10 14.65m DDH 14-01 13-12-092 11W5 Two Phases Buffalo Hills Assmt. 9815 carbonate? grey-green mtx - multiple clasts, whitish, some zoned?

a x serpentine large white clast b x serpentine small clast xl faces, white c x serpentine end - more matrix - green, fine d x serpentine green matrix, sawn surface e x serpentine swarm of small grains, altered, whitish

ASHK11 14.65m DDH 19-03 03-25-089-12W5 Buffalo Hills Assmt. 9815 solid core - muddy brn, arglzd matrix - arglzd clasts

a x x Mg silicate > saponite muddy brown matrix c x x Mg silicate > saponite end - xls/grain swarm d x x Mg silicate > saponite altered grains

ASHK12 84.93m DDH91-03 03-23-092-11W5 Buffalo Hills Assmt. 9815 grey, green fine grained mtx, large clasts, arglzd mtx

a x serpentine matrix w/white altered b x serpentine swarm of grains in white matrix c x ? serpentine ? chlorite trace argillized white grains d x ? serpentine large grey - shale? clast e x serpentine white altered clast, side of core

Sample ID Depth Sap Ser CO3 Apo Gyp Ver Chl Mg Amp Mineral Description ASHK13 58.4m DDH 7C-01 05-01-992-11W5

Buffalo Hills Assmt. 9815 tan, orange matrix - oxidized large alt white clasts

a x smectite + ???+ CO3? matrix b x smectite + ???+ CO3? clasts - white c x smectite + ??? + CO3? swarm, small clasts


d x smectite +??? + CO3? smaller swarm ASHK 14 76.93m DDH 7B-01 04-01-092-11W5

Buffalo Hills Assmt. 9815 fi gr grey mtx w/alt sm white grains, blk shale clasts

a x x saponite, Mg silicate matrix b x saponite matrix c x x saponite, Mg silicate matrix

ASHK 15 45.0m ML 02-91 12-36-74-25W5 Mountain Lake AR Min 9404, GSC OFR 3441 grey green matrix, arglzd, silic dense, small phenos/ clasts, alt grains - some large, others obviously clay

a x Mg silicate matrix b tr x Mg silicate, tr apophyllite matrix c x x Mg silicate + apophyllite large clast, alt - side of core d x x apophyllite + Mg silicate large clast, altered, side of core (could be distorted) e x apophyllite large clast, altered, side of core (could be distorted)

Sample ID Depth Sap Ser CO3 Apo Gyp Ver Chl Mg Amp Mineral Description

ASHK 16 Hand Spl SW 18-01-08W4 Black Butte ARM 9522 green, gd mass w/brown, mica in matrix

a x amphibole + vermiculite mica flake b nontronite? nodule, brown-white c x amphibole + vermiculite large brown mica flake d x amphibole + vermiculite large brown flake e x amphibole + vermiculite large brown flake f x amphibole + vermiculite matrix - green

Alteration Mineralogy of Alberta Kimberlites: PIMATM Infrared … · 2020-03-16 · ALBERTA...

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