Master's Thesis

MASTER'S THESIS

Mineral Chemistry and Texture Paragenesis of Alteration Minerals in the Pahtohavare Cu-Au Deposit, Sweden

Valentin Alain 2014

Master of Science (120 credits) Exploration and Environmental Geosciences

Luleå University of Technology Department of Civil, Environmental and Natural Resources Engineering Mineral chemistry and texture paragenesis of alteration minerals in the Pahtohavare Cu-Au deposit, Sweden

Valentin Alain

Master of Science

Exploration and Environmental Geosciences

Luleå University of Technology

Department of Civil, Environmental and Natural Resources Engineering

To my parents Jean-Michel and Anne-Lise Alain who gave me the chance to study.

Abstract

The Proterozoic Pahtohavare Cu-Au deposit in the northernmost part of Sweden within the Fennoscandian shield consists of a syngenetic stratiform sulphide-magnetite mineralisation (East Ore) which is uneconomic and three stratabound to discordant epigenetic Cu-Au mineralisations (Central, South-East and South Ores) hosted by the Viscaria formation. These epigenetic deposits are hosted by fine-grained albite felsite formed by alteration of graphitic schist while the East Ore is hosted by tuffite. The black graphitic schist have acted as a chemical trap for the mineralising fluids explaining the decomposition of the graphite within the schist proximal to mineralised zones and altering it into albite felsite. The past tectonic events made the Kiruna area having a favorable permeability for epigenetic solutions like saline hydrothermal fluids. This favourable permeability is one of the main important characteristic which explains the formation of Pahtohavare ores.

A scapolite-biotite alteration is enveloping the albite-altered mineralised zone and occurs in all stratigraphic units. One albite alteration of the tuffite is related to the intrusion of the footwall mafic sill and the other one is an additional ore-related mineralised albitization which is distinguishable by the lack of spatial relationship with the mafic sill and the occurrence of disseminated Ferro-dolomite. Chlorite has been formed by replacement of biotite and amphibole. A negative correlation between Mg and Cl contents of amphiboles is distinguishable which indicates that Mg-Cl avoidance mechanisms can control the incorporation of halogen in the amphibole structure. Scapolite from scapolite-biotite alteration surrounding the ore-bearing albite felsites and ore veins have a dominantly marialitic composition which indicates that the alteration must have been due to highly saline fluids. The occurrence of dipyre in Pahtohavare can be explained by the fact that the formation of the deposit happened in a Na-Cl rich environment. The main ore minerals are chalcopyrite and pyrite occurring disseminated, as veinlet, or filling breccias, and they are often associated with quartz and carbonate. Pyrrhotite is locally significant. Accessory minerals such as sphalerite, galena, millerite, native gold, tellurobismuthite, altaite, molybdenite, tellurides, and native gold in epigenetic ores occur as inclusions in sulphides and quartz.

Alteration zones surrounding the Pahtohavare ores have chemical and mineralogical zonations similar to Rakkurijärvi. The Mg-content of biotites decreases toward the ores of the South, East and South East zone. Addition of potassium and depletion of calcium and manganese are characteristic of the biotite-scapolite alteration zone. The ore-bearing albite carbonate alteration zone shows a depletion of K2O and an addition of Na2O, CaO and MnO. The relation between the depletion of Na and scapolitisation-albitisation is close as it is likely due to Na-Ca exchange reactions. Co-variation diagrams are good geochemical discriminants which can be used as exploration tool. The alteration characteristics of the Pahothavare deposit share similar features with other iron oxide and sulphide deposits such as e.g. Bidjovagge, Norway. The sodic alteration is the most important one because of its association to the mineralisation.

There are two generations of ore-forming fluids at Pahtohavare. The main physicochemical parameters that controlled hydrothermal alteration and gold mineralisation are pH, ƒO2 and temperature. The decrease of ƒO2 triggered the replacement of pyrite by pyrrhotite and its occurrence is spatially related to the mineralisation. The magnetite-pyrite and hematite-pyrite assemblages may have buffered the pH increase and ƒO2 decrease of the ore fluids. The chloride complexes of copper and gold are the most important one concerning the transport. The destabilization of gold chloride complexes is the main mechanism of gold deposition. This destabilization is due to an increase of pH from CO2 loss, cooling and dilution of the solution. The high salinity of the fluid can be explained by the metasomatic hydration of biotite and amphibole formation. Salinity is an important factor which determines the precipitation of metals from chloride complexes. Pahtohavare is considered as a copper deposit because of the low concentrations of gold due to the low initial concentrations of gases in the ore fluid and the fluids have not reach the native gold solubility 103 ppb limit for Cl complexes but has crossed the copper 100 ppm limit for Cl complexes. The copper content of the hypersaline brines at Pahtohavare have a range of 100-500 ppm which is comparable to saline magmatic fluids of the Cloncurry district in Australia.

Table of Contents

Introduction ...... 1

Geological settings ...... 2 2.1. Regional geology ...... 2 2.2. Local geology ...... 5 2.3. Geology of the Pahtohavare deposit ...... 9

Methodology ...... 12

Results ...... 13 4.1 Geochemistry ...... 13 4.2 Microscopic study ...... 17 4.3 Mineral chemistry ...... 23 4.3.1 Silicates ...... 23 4.3.2 Iron oxides ...... 30 4.3.3 Sulphides ...... 31 4.3.4 Carbonates ...... 33

Discussion ...... 36

Conclusion ...... 42

Acknowledgments ...... 42

References ...... 43

Appendix...... 46

Introduction

The main purpose of this thesis is to study the mineral chemistry variations, the texture and paragenesis of alteration minerals in rocks within and surrounding the ores of the Pahtohavare deposit to be able to determine if any correlations between the gold-copper occurrence and those variations exist.

The first aim of this thesis is to identify the different mineral chemistry variations occurring in the different ores to be able to deduce the mechanisms and sources of those variations. The second objective is to make simplified paragenetic sequences and detailed descriptions of specific paragenesis of alteration minerals of each ore in order to identify any differences between the ores. When these objectives are completed, it would be possible to determine if any zonation of alteration can be used as exploration tools pointing toward the mineralization

The Proterozoic Pahtohavare deposit is located 8km southwest of Kiruna and about 10 km south of the Viscaria deposit, in a volcanoclastic unit of the Kiruna greenstones. The discovery of this deposit is the result of intensive gold exploration in Norrbotten by the Swedish Government since 1982.

In 1984, NSG initiated an exploration program at Pahtohavare with the intention to find ore of Viscaria type using geological, geophysical, geochemical work and diamond drilling. As very little number of outcrops was found, geophysics, geochemistry and drilling have been mainly used (Carlson, 1988). The past exploration activities four different ores was identified: South East Pahtohavare, East Pahtohavare, South Pahtohavare, and Central Pahtohavare. At the end of the 1987 exploration program, 108 diamond drill holes and 22000 metres of drilling had been completed.

Pahtohavare has been mined minor contributions from 1990-1997. The majority of the production came from the main Southern orebody with the South-East ore. The Central ore have not been mined mainly because it consists of secondary Cu-minerals which is a problem in a metallurgical point of view. Due to the results of a recent EM survey, the Central ore is now the main subject of interests. As a large untested conductor located in a down-dip position of the Central oxide ore body has been identified. This thesis has been sponsored by Kiruna Iron AB.

Geological settings

2.1. Regional geology

The Pahtohavare Cu-Au deposit is located in the northern part of the Norrbotten County which is an important mining region within the Fennoscandian shield. The apatite irons ores (Kiruna and Malmberget) are economically the most important deposits for this province however it also hosts the Aitik deposit which is the Europe’s largest Cu mine. Gold is a minor element in some Cu-deposits like Pahtohavare (Fig.1.).

Fig.1. Simplified bedrock map of the northern art of Norrbotten County with epigenetic deposits occurrences (Bergman, Kübler, & Martinsson, 2001).

The bedrock in the northern Sweden is a part of the Baltic Shield which has been formed during three consecutive major orogenic events: Lopian orogeny (2.9-2.6 Ga), Svecofennian 2

orogeny (2.0-1.7 Ga) and Gothian orogeny (1.75-1.50 Ga). As showed in Fig.2, the study area is located in a transition zone between the Archean domain of the Baltic Shield in the northeast and the Svecofennian terrains on the southwest. The Archean domain has been affected by a rift event during the Lopian orogeny which has produced rift related greenstones. At the same time, a westward subduction of ocean crust has generated calcalkaline volcanic rocks. It ended with a collision envent with the Belomorian belt which is outlining the suture (Gaál & Gorbatschev, 1987; Martinsson, 1997).

Fig.2. Major geological units in the Fennoscandian Shield and surrounding areas. (Bergman, Kübler, & Martinsson, 2001). KADZ= Karesuando-Arjeplog deformation zone, PSZ= Pajala shear zone.

The basement of the Norrbotten Region is an Archean granitoid-gneiss basement consisting of c. 2.8 Ga tonalite-granodiorite intrusions with some mafic-intermediate volcanic rocks, clastic sediments and undeformed red c. 2.7 Ga granites (Bergman et al., 2001). Several generations of 2.1 Ga mafic dyke swarms have intruded these rocks and are related to the continental breakup (Martinsson, 1997). The deformed-metamorphosed Archean basement is unconformably overlain by Paleoproterozoic greenstones, porphyries and sediments (Martinsson O. , 2004). In the Kiruna area, the Kovo group (c. 2.5-2.3 Ga) consists of clastic sediments and basaltic-andesitic volcanic rocks formed during a rifting event. During a second rifting event at c. 2.1 Ga, the Kiruna Greenstones were formed. This rifting ended with 3

the opening of a SE-NW-directed ocean. MORB-type pillow lavas in the upper part of this sequence represents a deeper marine facies within a NNE-directed failed rift arm while the lower part of the greenstones have been deposited in a shallow water environment. The Haparanda and Perthite suites (1.89-1.87 Ga) are synorogenic intrusions and have a gabbroic to granitic range of composition (Martinsson, 2004). The extensive subduction (1.9 Ga) which had generated island arc magmatism and a basin closure has created a crustal accretion in Svecofennian time. The collisional orogeny and Svecofennian porphyries (1.83-1.77 Ga) have followed (Martinsson, 1997).

Fig.3. Simplified diagram with schematic illustration of main rock types and units of the northern Norrbotten region (Bergman et al., 2001).

2.2. Local geology

The Pahtohavare deposit is situated in the Kiruna area which consists of Paleoproterozoic rocks as greenstones, porphyries and clastic sediments lying unconformably on a deformed Archean basement.

Fig.4. A. Simplified geological map of the Baltic Shield outlining the major tectonic units. B. Generalized geology of the Kiruna area with location of the Viscaria deposit (Martinsson, 1997).

The stratigraphic succession of the Kiruna area can be described according to the following subdivisions. The Kovo Group (2.4-2.3 Ga) which consists of clastic metasedimentary and mafic-intermediate metavolcanic rocks unconformably overly the Archean basement (Bergman et al., 2001). This stratigraphically lowest unit of the Karelian rocks consists of basal conglomerate, tholeiitic lava, volcanoclastic sediments and calcalkaline mafic to intermediate volcanic rocks (Martinsson, 1997). The following unit is called the Kiruna Greenstone Group which is deposited during a rift-related event based on a combination of lithological and geochemical criteria divided into six formations (Martinsson O. , 1997). The Såkevaratjah Formation consists of amygdaloidal basalt with intercalations of conglomerate in the lower part. It is followed by the Ädnamvaara Formation which is an ultramafic unit with a komatiitic composition. Next is the Pikse Formation, another unit of tholeiitic basalt flows with some intercalations of chemical sediment. On top of it follows the Viscaria Formation which is a tuffitic unit with minor black schists, magnetite-sulfide ores, carbonate rocks hosting the Viscaria and Pahtohavare deposits. An upper basaltic pillow lava 5

unit with some intercalations of mafic tuff, tuffite and iron-rich sediments is called the Peuravaaara Formation. The top of the Kiruna Greenstone consists of volcanoclastic rocks of pyroclastic origin, the Linkaluoppal Formation. In the central Kiruna area, it has been lost by erosion. The Såkevaratjah, Pikse and Viscaria formation have been intruded by mafic sills, probably related to the same magmatic event forming the Peuravaaara Formation (Martinsson, 1997). Then, the Kurravara Conglomerate overlay unconformably the Peuravaara Formation, followed by the Kirunavara Group and Hauki Quartzite (Martinsson, 2004). Both Kurravara Conglomerate and Kirunavara Group have an approximate age of 1.89-1.91 Ga. This volcano- sedimentary sequence deposited on the Archean basement has a total thickness of approximately 8-10 km.

Fig.5. Stratigraphy and chronology of Paleoproterozoic greenstones in the northern part of the Baltic Shield (Martinsson, 1997).

The Kiruna area has been affected by several types of alterations, some related to ore formation and others have a more regional character. Scapolitisation for example is rather widespread and particularly intense in the north of the Norrbotten County. Intense scapolitisation is believed to be mainly linked to shear zones, contact of intrusive rocks or mineral deposits. The strong scapolite alteration of the lowest part of the Greenstone group is possibly due to the metamorphism of evaporate beds (Martinsson, 1997). According to Lindblom et al (1995) and Bergman et al (2001), regional scapolite replaces plagioclase in gabbroic rocks and in mafic sills which has also been observed from core logs study. A second important type of alteration in Kiruna area is a locally intense albitization of

greenstones producing Na-rich felsic rocks along the contact with mafic sills in the Viscaria Formation and associated to epigenetic copper-gold mineralisations. The albitization of tuffite has an extension 1-15m from the contact of the mafic sills and has been initiated from the reaction between hot basaltic intrusions and unconsolidated volcanoclastic rocks with saline interstitial water (Martinsson, 1997).

Metamorphism & Deformation

The Pahtohavare deposit is located within the Kiruna area where the metamorphosed rocks may contain zoisite and chlorite. It is characterised as a low-grade metamorphic area. In this area hornblende, epidote, plagioclase, chlorite, actinolite and albite are the minerals present in the mafic metavolcanic rocks which indicates those rocks have undergone an upper greenschist to lower amphibolite metamorphic facies.

As a part of the Norrbotten County, the Kiruna area went through several ductile and brittle deformation events. This E domain has a strong North-South structural orientation (Bergman et al., 2001). Four different deformation events has been identified in the Kiruna area: an early westward thrusting linked to the formation of mineral lineation, folding, a formation of thrust ramps and last, the formation of open folds and shear zones (Bergman et al., 2001). The major ductile shear zones affecting the north of Sweden as KADZ, KNDZ, NDZ and PSZ (Fig.7) have been active at ca. 1.8 Ga. It has been noticed that the crustal-scale shear zones have a close relationship with metamorphic grade changes which indicate that the shear zones have been active after the peak of regional metamorphism. Many epigenetic gold and copper-gold deposits have a close spatial relationship with crustal-scale shear zones, however it appears that their local control depend of second-fourth-order faults and shear-zones (Billström et al., 2010).

Today, it is possible to say that the Kiruna area has been affected by one major compressional deformation episode and correspond to eastern limb of an anticline by studying the bedding-cleavage relationships and fold symmetries. The Kiruna Greenstone Group dipping toward southeast is part of this anticline steeply. The asymmetric folds dipping toward south are Z form (Vollmer, Wright, & Hudleston, 1984). In the Pahtohavare area, it is possible to identify a local anticline. This anticlinal structure has been partly overturned and truncated by a major WNW shear zone and then, secondary shear zones have been formed mainly at the fold hinge and limbs (Martinsson O. , 1997).

Fig.6. Metamorphic map of the northern part of Norrbotten County. Examples of localities where boundaries between medium-and high-grade metamorphism are controlled by deformation zones are marked by A. KADZ= Karesuando-Arjeplog deformation zone. KNDZ= Kiruna-Naimakka deformation zone, NDZ= Nautanen deformation zone, PSZ= Pajala shear zone (Bergman et al , 2001).

Fig.7. Map with generalised structural trends from magnetic connexions and form lines of tectonic foliations. KADZ= Karesuando-Arjeplog deformation zone. KNDZ= Kiruna-Naimakka deformation zone, NDZ= Nautanen deformation zone, PSZ= Pajala shear zone (Bergman et al, 2001).

2.3. Geology of the Pahtohavare deposit

In 1984, the NSG (The State Mining Property Commission) start to explore for Viscaria-type deposits in the Pahtohavare area where resulting it the discovery of a syngenetic stratiform sulphide-magnetite mineralisation genetically similar to the Viscaria deposit, the East Pahtohavare deposit. The mineralisation consists of thin intercalations of magnetite, chalcopyrite, pyrrhotite, pyrite situated in the middle part of the Viscaria Formation between two black schist formations. However, it is considered has an uneconomic deposit due to its small size and low grade. After few drilling operations 1985-1988 the South, South-East and Central deposits was discovered. Those three stratabound to discordant epigenetic Cu-Au mineralisations are hosted by the Viscaria formation in an anticlinal structure dipping to the south-east with an over-turned south limb which makes the axial plane dipping approximately sixty degrees to the north-east. The epigenetic deposits are hosted by fine grained albite felsite which has been formed by alteration of the graphitic schists while the Eastern deposit is hosted by tuffite (Martinsson, 1997). The black graphitic schists have probably acted as

chemical trap for the mineralising fluids explaining the decomposition of the graphite within the schists proximal to mineralised zones and altering it into albite felsite.

Fig.8. Geological map of the Pahtohavare area. All rocks belong to the Greenstone group except the metaconglomerate (Svecofennian metasediment) (Bergman et al, 2001).

The host rocks are highly altered by regional and local alteration occurring within the Pahtohavare area. The scapolite-biotite alteration is enveloping the albite altered mineralised zone and occurs in all stratigraphic units. There are two types of albite alteration occurring in Pahtohavare, one is related to the intrusion of the footwall mafic sill as mentioned previously and one is an additional ore-related mineralised albitisation which is distinguishable by the lack of spatial relationship with the mafic sill and the occurrence of disseminated Ferro- dolomite.

The main ore minerals are chalcopyrite and pyrite occurring disseminated, as veinlet or filling breccias and often associated with quartz and carbonate. Pyrrhotite is locally significant. Accessory minerals as sphalerite, galena, millerite, tellurobismuthite, altaite, molybdenite, tellurides and native gold in epigenetic ores occur as inclusions in sulphides and quartz (Lindblom et al., 1995). Copper and gold have probably precipitated at the same time according to their similar distribution patterns (Martinsson et al., 1997). The gangue minerals are Ferro-dolomite, quartz and minor marialitic scapolite, biotite and albite. Moreover, the host rock age and timing of the mineralisation is c. 2.1 Ga. In addition to Au and Cu, the components enriched are Co, U, S and Te (Martinsson et al., 1997).

Only the South and South-East deposits have been mined starting as open pits respectively from 1990 to 1992. Both ores have been developed for underground mining in

1993 until their closure in 1997. Totally 1.68 Mt of ore with 1.89% Cu, 0.88ppm Au has been produced (Martinsson et al., 1997). The Central deposit has not been mined mainly because of its small size and the extensive supergene oxidation which has replaced the primary sulphides by oxides as malachite, chrysocolla, limonite-goethite and Cu-oxides.

Pahtohavare deposit have an analogue at Bidjovagge (Norway) which also is a copper- gold deposit occuring in albitized rocks comprising graphitic schist and tuffite in the Proterozoic Kautokeino Greestone Belt. They occur similar to Pahtohavare in antiforms close to shear zones. In the Bidjovagge case, the poor correlation between gold and copper indicate that the precipitation of the metals was controlled by different factors while Pahothavare has a coeval precipitation of Cu and Au shown by their distribution patterns and as gold inclusions occur in chalcopyrite. Albitisation is the most common alteration at Bidjovagge and is often associated with carbonatization. The alteration may have been due to seawater circulation or a sodium-rich brine of seawater. Scapolite is formed at the expense of albite. Biotite is present in restricted zones with albite, amphibole and carbonate (Bjørlykke et al., 1997).

Fig.9. The six mineralised zones of Pahtohavare (Wild, 2012).

Methodology

There are four main methods which have been used to get enough information to be able to complete the objectives of this thesis.

Core logging

Thirteen drill cores from the SGU drill core archives in Malå have been selected by Olof Martinsson. These cores (Appendix 1) have been previously logged by Leif Carlson and some by Heikki Markkula, Stina Danielson and Bose Gustafsson. The author has logged these cores during spring 2013. There are two from the East, three from the Central, five from the South and three from the South-East ore. They have been drilled from 1984 to 1988.

Geochemistry

Nineteen samples from the three drill cores of the South-East ore have been sent to ALS laboratory in Piteå for wholerock analysis using the XRF method (Appendix 2). The samples have been preferentially selected from less altered units which are representative precursors of the altered ones.

Microscopy

Fifty-three samples have been taken from the thirteen logged drill cores and sent to Vancouver Petrographics, Canada. The thin sections were analysed by optical microscope in order to define and identify the texture paragenesis of alteration minerals. Alterations zone, mineralisations and veins have been preferentially selected. The microscopic observation of thin sections is necessary to be able to collect enough information about the mineralogy and in order to select the minerals for microprobe analysis.

Microprobe

The microprobe analyses have been preferentially done on silicates, carbonates, sulphides and oxides in order to determine any changes in composition of those minerals. The JEOL JXA-733 electron microprobe analyser of the Oulu University (Finland) is believed to be the best one according to the quality of the past results. A total of 22 analyses were performed on biotite, 22 were acquired on chlorite, 12 on titanium minerals, 7 on scapolite, 5 on feldspars, 7 on iron oxides and 6 on amphiboles. An additional 22 analyses were made on carbonates and phosphates and 54 on sulphides.

Results

4.1 Geochemistry

Classification of magma

The use of the cation plot from Jensen (1976) makes it possible to get the general character of the volcanic rocks as the main elements reflects the mineralogy of the rocks. From the Jensen plot, it is possible to identify three major rock types: tholeiites, komatiites and calcalkalines rocks. The analysed volcanic rock samples have a Fe-tholeiitic character. The only sample near to the calc-alkaline area is believed to be a highly altered albite felsite.

Fig 10. Cation plot for volcanic rock from the Kiruna Greenstone Group at South-East Pahtohavare (Jensen, 1976).

Alterations

As the sampled rocks have been more or less affected by several types of alterations as albitization, scapolitisation, chloritisation and biotite alteration in accordance to the logging description, it is necessary to plot the data in order to find the least altered sample (Fig.11)

Fig 11. Igneous spectrum plot for the Kiruna greenstone group rocks of South-East Pahtohavare (Hughes, 1973).

The Alteration Index (AI=100.K2O+MgO/K2O+MgO+CaO+MgO) have also been calculated for each mafic volcanic samples (Appendix 2). The least altered sample have been selected because it has an AI<50, K2O< 2%, Na2O< 3% and plot within the igneous spectrum. Understand the geochemical discrimination between altered and least altered volcanic rocks is very important in order to identify the alterations. From Fig.12, it is possible to say that the volcanic rocks that have been exposed to biotite-scapolite alteration exhibit addition of potassium and the depletion of calcium and for some sample manganese as well. Barium has also been added, this addition can also be due to the biotite-scapolite alteration or/and by the presence of some small barite veins. L.O.I. is mostly increased compared to the least altered sample which could be explained by the presence of dolomite and calcite in altered rocks. According to Martinsson (1997), in the South-eastern ore the surrounding biotite-scapolite alteration can be identified by the enrichment of K, Ba and a depletion of Mn. Plotting geochemical compositions of samples from different ores (Fig.13) has been decided in order to identify the relationship between alterations and several ores of Pahtohavare. The results from these graphs confirm the previous observations that the closer we get to the ore-bearing albite carbonate alteration zone, K2O got depleted and Na2O, CaO and MnO are enriched which reflects the destruction of biotite-scapolite and amphibole during albitization (Martinsson, 1997). The samples showing a %Cu >0.5% are mostly at the left side of the graphs. It is also possible to notice from these graphs that the samples from the surrounding biotite-scapolite alteration which caused an enrichment of K and a depletion of Mn are on the right side. Moreover, it is possible to say that the Cu occurrence is related to albitization even if some samples from the albite alteration zone do not show a Cu enrichment.

1.5 Log WR88057E/ Least altered 1.5 Log WR88034C/ Least altered

1 1

0.5 0.5

0 0

-0.5 -0.5

Log WR85115A/ Least altered Log WR88057I/ Least altered 1.5 1.5

1 1

0.5 0.5

0 0

-0.5 -0.5

Log WR88057B/ Least 1.5

0.5

-0.5

Fig. 12. Chemical changes in mafic volcanic wall rocks at the South-eastern ore. Normalized to the least altered rock.

%Cu 7 6 88057 5 Albite alteration Biotite-scapolite alteration 85115 88034 4 87119 3 87104 2 85108 1 84004 0 %K2O 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00

%Cu 7 6 88057 Albite alteration 5 85115 88034 4 87119 3 87104 2 85108 1 84004 0 0 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 K20/K2O+Na2O %

%Cu 7 6 88057 Albite alteration Biotite-scapolite alteration 85115 5 4 88034

87119 3 87104 2 85108 1 84004 0 0 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 K2O/CaO+Na2O+K2O %

Fig. 13. Figures showing the correlation between copper and depleted/enriched elements in ore and wall rocks. Blue: South-eastern ore; Red: Central ore; Green: Eastern ore.

4.2 Microscopic study

Biotite-Scapolite alteration

Two types of biotite-scapolite alterations have been identified during the core logging study, one has regional character and one is ore-related. In a petrographic view, the scapolitisation close to the South-East ore (Fig.14 A) consist of 0.5-1.0 mm subhedral porphyroblasts of scapolite in a matrix of 20-50 µm euhedral biotites. This is the result of the change of mafic sill into a fine grained biotite rock with large scapolite due to the replacement of amphibole by biotite and scapolite replacing plagioclase (Martinsson, 1997). It is also possible to observe some few 0.75-0.50 mm euhedral pyrites mainly in the matrix but some rare and small pyrite grains can be present in scapolites. A biotite-scapolite ore-related alteration from the Central ore (Fig.14 B) shows 250-500 µm anhedral porphyroblasts of scapolite in a matrix of 20-50 µm subhedral biotites. Minor quartz and plagioclase grains are also present. It is also possible to see that amount and the size of the scapolite grains are different between the two samples. Some scapolite grains are sericitized along cleavages in sample B while none have been observed in sample A. The A and B biotite-scapolite altered rocks are believed to be the result of the replacement of amphibole by biotite which is also believed to come from the alteration of plagioclase and pyroxene. Pyrite is the only sulphide which has been observed into the biotite-scapolite alteration zone. Subhedral magnetites are mostly present and carbonates are often very rare.

Albitization

There is two different albite alterations one is regional formed during the basaltic intrusion in volcanoclastic rocks containing saline interstitial water and another one which is ore-related. The ore-related one is distinguishable by the fact that it is associated with Ferro-dolomite. Albite is formed from replacement of biotite and scapolite. Figure 14 E shows the mineral assemblage which consists of biotite-scapolite alteration with albite, containing disseminated magnetite, pyrite associated with albite veining and mm scale carbonate grains. Figure 14 F also shows the minerals assemblage from the transition zone between biotite-scapolite and albite alteration. The hand specimen shows a “zebra texture”. Sericitisation of scapolite, albite and other feldspar is quiet common but weak compared to carbonatisation (Fig.14 B, D). Albite grains usually occur as patches with carbonate and biotite grains while albite veins have ~100µm elongate grains rather orientated rather approximately parallel to the vein orientation if it had not been deformed by folding and shearing.

Chloritisation

It is possible to differentiate two types of chloritisation, one concerning amphibole grains by the size and shape of the primary amphibole (Fig.20E), the second one A B

C D

E F

Fig 14. Microscopic pictures; A: Biotite-scapolite alteration of mafic sill South-East Pahtohavare, B: Biotite- scapolite alteration of gabbroic wallrock Central Pahtohavare, C: Chloritisation Central , D: Albite vein in a gabbroic wallrock South Pahtohavare, E Scapolite-biotite/albitization transition zone South Pahtohavare, F Scapolite-biotite/albitization transition zone South-East Pahtohavare. 18

related to the replacement of biotite which form small scattered grains particularly in potassic alteration zones. Two main events of chloritisation have been deduced from microscopy study: before and after the formation of sulphides. The chloritisation zone is widespread and is most important in mafic gabbroic units. Chlorite is mainly related to amphibole alteration in mineralised samples.

Paragenesis sequences

East

Minerogenetic periods and Time stages Early Late SILICATES Pyroxene Amphibole Albite Quartz Chlorite ? ? Biotite Scapolite CARBONATES Dolomite Calcite OXIDES Magnetite Illmenite SULPHIDES Pyrite Chalcopyrite Pyrrhotite Sphalerite Main phase Weak phase The microscopic study of the Eastern ore has been done on a thin section showing the mineralisation in veinlets and wallrock which consists of disseminated magnetite, chalcopyrite and pyrite but only pyrite and chalcopyrite in the veinlet. The amount of pyrite is much more important than chalcopyrite while pyrrhotite is minor compared to chalcopyrite. Chalcopyrite is anheudral, bordering the pyrite and showing open-space filling texture. Vermicular chalcopyrite in quartz has also been observed. As it is possible to see from Figure 20 C, quartz grains are rather anheudral and contain sulphides and a few chlorite grains. Rounded chlorite aggregates have a size of 350 to 50 µm in the veinlet while in the wallrock chlorites show a complete different texture. Quarts grains are much smaller and feldspars have not been seen. Carbonatisation occurs as veins of mm to µm scale grains. It is possible to 19

notice a halo of reaction between chlorite and carbonates which give information for the paragenesis sequence Figure 20 E. Hematite is rather less abundant than magnetite and is associated with pyrite while magnetite is disseminated. Quartz occurs as interstitial µm scale grains or as veinlets. Few 100-300 µm rounded garnets have been identified in carbonate veining network in a volcano sedimentary unit.

South

Minerogenetic periods and Time

stages Early Late SILICATES Pyroxene Amphibole Albite Quartz Chlorite Sericite Biotite Scapolite CARBONATES Dolomite Calcite

OXIDES Hematite Magnetite Rutile SULPHIDES Pyrite Chalcopyrite Pyrrhotite

Samples from the Southern ore gave some additional information in and completed the rest of the paragenesis sequence. The studied thin section shows a porphyroblastic texture composed of subhedral 100µm-1mm dolomite porphyroblasts in a matrice of pyrite, chalcopyrite and pyrrhotite (increasing proportion order). Pyrite and pyrrhotite are sometimes vermicular through carbonate grains but rather euheudral to subheudral. Chalcopyrite is disseminated, anheudral and filling cracks carbonates and shows an interstitial, free space filling texture. Carbonates have been observed in cracks of albite phenocrysts. Weak sericite alteration is also identifiable. Quartz mostly occurs to be related to veining events which post- date the carbonate one. It is possible to distinguish the original porphyroblastic texture from a biotite-scapolite altered sample from the albtisation zone. Scapolite and biotite have been 20

replaced to albite. The matrice is composed of small elongated 100-200 µm grains which show a very low extinction angle from the Carlsbad twins.

Central Minerogenetic Time periods and stages Early Late SILICATES Pyroxene Amphibole Albite Quartz Chlorite Sericite Biotite Scapolite CARBONATES Dolomite Calcite OXIDES Hematite Magnetite Illmenite Rutile SULPHIDES Pyrite Chalcopyrite Pyrrhotite

The amount of magnetite in the Central ore thin section is much more abundant than sulphides. Pyrite is more abundant than chalcopyrite. Chalcocite has been observed associated with chalcopyrite which may be due to supergene oxidation. Chalcopyrite and pyrite can be within magnetite grains but in the matrix as well. Chalcopyrite has not been seen in pyrite. Pyrite shows an open space filling and jointing texture. Quartz occurs mainly between the oxides and sulphides grains but few times inside magnetite. Hematite is also occurring mainly at the contact with pyrite and along magnetite. Pyrite and pyrrhotite occur rather sporadically which means that these phases are subordinate. Some cuprite, tenorite, malachite, hematite and azurite have been identified in previous microscopic studies of the ore (Hålenius, 1988). 10µm grains of gold occur with oxides and carbonates but mainly in the quartz-rich parts of the mineralisation.

South-East

Minerogenetic Time periods and stages Early Late SILICATES Pyroxene Amphibole Albite Quartz Chlorite Sericite Biotite Scapolite CARBONATES Dolomite Calcite OXIDES Hematite Magnetite Illmenite Rutiles SULPHIDES Pyrite Chalcopyrite Pyrrhotite PHOSPHATES Apatite

The thin section from South-East ore studied shows 100-300 µm carbonate grains close to the intense carbonatisation while grain size decrease when carbonates proportion decrease. Magnetite grains have a size from 0,1 to 2mm and are rather euheudral. Magnetite and pyrite 10-100 µm grains are subheudral to anheudral in the fine grained part. Chalcopyrite is often on the border of pyrite and magnetite grains. It is also possible to see pyrite and chalcopyrite inclusions in magnetite while magnetite inclusions in pyrite are rare. Albite and other feldspars have not been identified which is probably due to the intense carbonatisation. The abundance of magnetite is much more important than pyrite which occurs in a higher proportion than chalcopyrite. Two generations of chlorite have been identified, one occurring as fine grained matrix (biotite replacement) or phenocrysts (previously amphibole) and one weaker consisting of chlorites in late quartz veins crosscutting albite veins.

4.3 Mineral chemistry

4.3.1 Silicates Biotites

In order to identify any chemical changes and zonation of the biotite alteration, analysed biotites come from the biotite-scapolite alteration of both gabbroic and volcanosedimentary units and from mineralised albite felsite. The #Mg (Mg/Mg+Fe) has been calculated for each biotite. Most of biotites are phlogopites but annites have been identified from the east mineralisation in graphitic banded volcanosedimentary unit (Appendix 3, No1, 50) and also from a biotite-

Table 1. Representative electron microprobe analyses of biotites.

Zone South East Central South East Sample 88219C CHL 88218D2 BIOT84004Fbiot 85108F BIOT 87104J1 BIOT 87127E BIOT 85115J BIOT 88057A BIOT No. 57 101 8 50 36 67 74 120 Na2O 0,171 0,113 0,163 0,217 0,163 0,118 0,134 0,178 FeO 14,184 19,816 19,706 23,996 26,499 18,686 21,462 18,008 Cr2O3 0 0 0 0,021 0,03 0,087 0,069 0,016 Cl 0,523 0,681 0,467 0,603 0,764 0,819 0,458 0,645 MgO 17,783 12,834 11,136 8,134 9,731 13,363 12,128 13,506 MnO 0,057 0,129 0,576 0,202 0,149 0,069 0,167 0,055 K2O 7,506 8,883 9,8 8,965 6,3 6,714 5,834 10,072 Al2O3 15,03 15,04 16,639 16,337 15,967 14,87 17,716 14,865 NiO 0,067 0,007 0 0,059 0,087 0,035 0,012 0,013 CaO 0,05 0,058 0,021 0 0,066 0,141 0,194 0,003 SiO2 35,44 36,079 36,07 34,7 32,379 34,789 32,796 37,282 TiO2 0,357 1,589 1,304 1,636 1,454 1,479 1,101 1,788 Total 91,05 95,075 95,777 94,734 93,417 90,985 91,968 96,285

Number of cations on the basis of 11O Si 2,757 2,779 2,765 2,745 2,614 2,766 2,598 2,821 Al 1,378 1,366 1,503 1,523 1,519 1,393 1,654 1,325 Ti 0,021 0,092 0,075 0,097 0,088 0,088 0,066 0,102 Cr 0,000 0,000 0,000 0,001 0,002 0,005 0,004 0,001 Mg 2,062 1,474 1,272 0,959 1,171 1,584 1,432 1,523 Fe2+ 0,923 1,277 1,263 1,587 1,789 1,243 1,422 1,139 Mn 0,004 0,008 0,037 0,014 0,010 0,005 0,011 0,004 Ni 0,004 0,000 0,000 0,004 0,006 0,002 0,001 0,001 Na 0,026 0,017 0,024 0,033 0,026 0,018 0,021 0,026 K 0,745 0,873 0,958 0,905 0,649 0,681 0,589 0,972 Ca 0,004 0,005 0,002 0,000 0,006 0,012 0,016 0,000 Cl 0,069 0,089 0,061 0,081 0,105 0,110 0,061 0,083 OH 1,931 1,911 1,939 1,919 1,895 1,890 1,939 1,917 #Mg 0,69 0,536 0,50 0,38 0,40 0,56 0,502 0,572

scapolite altered gabbroic unit situated between two significant mineralisation (Appendix 3, No36, 41) at the South zone. Concerning the East zone, the analysed biotite of a sample following the mineralisation has a higher #Mg (Appendix 3, No 8) than the ones of the mineralisation. The Central zone biotite analyses show a different pattern. The biotites from the mineralised albite felsite have a high #Mg (Appendix 3, No 19 24) while biotites from gabbroic unit surrounding the albite felsite have a lower #Mg. The South and South East zone 23

biotites show a similar pattern as the ones from the East zone. The biotites of the samples taken in a gabbroic units and albite felsite prior to the mineralisation show a #Mg>0,59 while biotites from samples close and within the mineralisation have a #Mg≤ 0,57 (Appendix 3 No106, 110, 74, 88, 95, 120).

Chlorites

The only chlorite which show a low #Mg have been found from the same samples where annites (low #Mg) have been previously identified (samples 85108F and 87104J). However, Mg rich chlorites are the most common ones and are also present with Fe-rich chlorites and biotites. Using the classification of Hey (1954) and Melka (1965), chlorites plot as delessite, pennine and corundophilite. It is not possible to distinghish the chlorites using optical microscope. However, chlorites replacing amphibole all plot in the corundophilite field.

Table 2. Representative electron microprobe analyses of chlorites.

Fig 15. Classification diagram of chlorites (Melka, 1965)

Fig 16. Classification diagram of chlorites (Hey, 1954)

Amphiboles

Concerning the chemical analysis of a hornblende from a carbonate altered mafic gabbroic unit in the South zone (Fig 17A, 88218D1), pyrite grains have been observed into it. An undefined amphibole has been studied from a quartz-chlorite vein with chalcopyrite, pyrite and Cr rich magnetite in a volcanosedimentary unit at the Central zone. The amphibole has been named as a ferro-tschermakite and occurs as an early mineral in the paragenesis sequence of the vein. The majority of amphiboles occur to have actinolite compositions. From Fig. 17 B, we can see a similar relationship between pyrite and the amphibole. We can now have an idea that the generation of amphibole and pyrite are close in the time scale and pyrite first generation rather post-date the amphibole generation. Actinolite may have been formed by alteration of albitic felsite by the ore-forming solution.

Table 3. Representative electron microprobe analyses of amphiboles.

Zone South East Central Sample 88218D1 HBL 88219B FELDS84004Mamph 87104J1 HBL 87119C ACT Name Actinolitic Hbl Actinolitic HblFerro-Hbl Actinolitic HblActinolite SiO2 52,342 52,928 42,789 50,271 55,192 TiO2 0,140 0,143 0,145 0,128 0,037 Cr2O3 0,000 3,026 0,047 0,031 0,000 Al2O3 3,736 3,026 11,131 4,470 1,932 FeO 12,420 9,824 20,026 16,446 7,982 MnO 0,301 0,129 0,494 0,338 0,153 NiO 0,000 0,000 0,000 0,000 0,027 MgO 15,778 17,423 6,538 12,331 19,105 CaO 11,826 12,502 11,672 12,139 12,633 Na2O 0,477 0,526 1,198 0,569 0,438 K2O 0,043 0,083 0,634 0,244 0,014 H2O 0,000 0,000 0,000 0,000 0,000 F 0,000 0,000 0,000 0,000 0,000 Cl 0,055 0,000 0,943 0,273 0,045 Total 97,063 99,610 94,674 96,967 97,513

Number of cations on the basis of 23 O Si 7,477 7,376 6,705 7,420 7,732 Ti 0,015 0,015 0,017 0,014 0,004 Cr 0,000 0,333 0,006 0,004 0,000 Al 0,629 0,497 2,056 0,778 0,319 Fe 1,484 1,145 2,624 2,030 0,935 Mn 0,036 0,015 0,066 0,042 0,018 Ni 0,000 0,000 0,000 0,000 0,003 Mg 3,359 3,619 1,527 2,713 3,989 Ca 1,810 1,866 1,959 1,919 1,896 Na 0,132 0,142 0,364 0,163 0,119 K 0,008 0,015 0,127 0,046 0,003 H 0,000 0,000 0,000 0,000 0,000 F 0,000 0,000 0,000 0,000 0,000 Cl 0,013 0,000 0,250 0,068 0,011

#Mg 0,694 0,760 0,368 0,572 0,810

Fig. 17 A: 88218 Hornblende with its pyrite from South albite-carbonate mineralised sample; B: 87119, Central mineralisation.

Fig 18. Calcic amphiboles with diagram parameters: CaB≥1.5; (Na+K)A≤0.5; CaA≤0.5, according to (Leake, 2013)

Due to a very low Si value, an amphibole from Central zone could be named as Mg-Gedrite or Cummingtonite because it is magnesium rich and calcium, sodium and potassium concentrations are low. Another possibility explaining the low Si value is that the amphibole has been replaced by chlorite partially conserving the initial shape and cleavage as the sample has been taken within chloritisation alteration zone.

Feldspars and scapolites

Scapolite have been analysed in order to determine their nature which is mainly marialitic in composition. From Fig.14F, it has been possible to see scapolites occurring in sample from an albitization zone. The analyse of scapolite in sample 85115N1 show a marialitic scapolite closer to the albite field on the ternary classification diagram compared with other scapolites from samples outside the albite alteration zone. The two anorthites have been found from both gabbroic and volcanosedimentary units few meters above and below the mineralisation respectively. Plagioclase has also been found mainly in potassic alteration zone but also in albite felsite.

Fig 19. Plot of compositions of feldspars and scapolites in Ab-An-Or ternary classification diagram.

Table 4. Representative electron microprobe analyses of feldspars and scapolites.( Ab=Na/Na+K+Ca; An=Ca/Na+K+Ca; Or=K/Na+K+Ca)

Zone South Central South East Sample 88218C FELDS88093D FELDS88221A SCP 87104J1 SCP 87104J2 SCP 87104J2 FELDS87127E SCP 85115N1 SCP88057A FELDS Anorthoclase Anorthoclase Anorthoclase Scapolite Scapoilte Albite Scapolite Albite Albite SiO2 55,672 56,646 55,552 55,100 55,598 69,585 55,599 67,200 67,690 TiO2 0,000 0,003 0,000 0,000 0,000 0,012 0,000 0,000 0,000 Al2O3 23,070 22,409 22,586 24,167 24,084 20,345 23,286 19,340 19,904 Cr2O3 0,000 0,004 0,000 0,000 0,023 0,000 0,004 0,000 0,000 FeO 0,173 0,089 0,049 0,015 0,065 0,179 0,000 0,566 0,099 MnO 0,044 0,000 0,000 0,065 0,024 0,053 0,000 0,024 0,010 MgO 0,000 0,000 0,000 0,002 0,000 0,000 0,000 0,147 0,000 CaO 7,947 6,319 7,300 9,506 7,696 0,404 7,614 0,476 0,295 Na2O 9,815 10,297 9,655 8,497 8,571 11,363 10,007 10,278 11,759 K2O 0,325 0,675 0,668 0,387 0,395 0,070 0,376 2,133 0,034 NiO 0,000 0,037 0,000 0,000 0,000 0,018 0,000 0,000 0,005 Cl 3,020 3,397 3,169 2,563 2,737 0,409 3,196 0,059 0,000 Total 97,046 96,479 95,810 97,739 96,456 102,029 96,886 100,164 99,796

Number of ions on the basis of 32 O

Si 10,446 10,652 10,539 10,271 10,424 11,918 10,437 11,872 11,876 Al 5,102 4,966 5,050 5,309 5,322 4,107 5,152 4,027 4,116 Ti 0,000 0,000 0,000 0,000 0,000 0,002 0,000 0,000 0,000 Cr 0,000 0,001 0,000 0,000 0,003 0,000 0,001 0,000 0,000 Mg 0,000 0,000 0,000 0,001 0,000 0,000 0,000 0,039 0,000 Fe2+ 0,027 0,014 0,008 0,002 0,010 0,026 0,000 0,084 0,015 Mn 0,007 0,000 0,000 0,010 0,004 0,008 0,000 0,004 0,001 Ni 0,000 0,006 0,000 0,000 0,000 0,002 0,000 0,000 0,001 Na 3,571 3,754 3,551 3,071 3,116 3,773 3,642 3,520 4,000 K 0,078 0,162 0,162 0,092 0,094 0,015 0,090 0,481 0,008 Ca 1,598 1,273 1,484 1,899 1,546 0,074 1,531 0,090 0,055

Alb 0,68 0,72 0,68 0,61 0,66 0,98 0,69 0,86 0,98 An 0,30 0,25 0,29 0,38 0,33 0,02 0,29 0,02 0,01 K 0,01 0,03 0,03 0,02 0,02 0,00 0,02 0,12 0,00 29

Titanium minerals

Rutile occurs with two different shapes. No. 113 is euheudral associated with quartz and carbonate grains in a sample from silicified part of a volcanosedimentary unit at the South zone close to the ore. The second rutile shows an elongated shape. Rutiles are present in a none negligible amount in a of graphitic volcano-sedimentarty unit situated close to the ore at the South East zone. Ilmenite grains are rather small (<50µm) subheudral to anheudral, filling disseminated cracks. The only ilmenite with a size over than 50µm has been observed in a sample of gabbroic unit from the Central zone.

Table 5. Representative electron microprobe analyses of Ti-minerals.

Zone South East Central SouthEast Sample 88221B MG 84004MMg 85108G MG 87104J1 PO SIL85115J MG 85115N2 ILL 88057Nb mg No. 113 4 54 35 72 83 93 Rutile Ilmenite Ilmenite Ilmenite Rutile Ilmenite Ilmenite Na2O 0,023 0,045 0,031 0,046 0,135 0,025 0,02 FeO 0,048 41,75 41,588 45,099 4,023 41,774 40,34 Cr2O3 0,474 0,01 0,009 0,009 0,034 0,005 0,021 Cl 0 0,012 0,021 0,014 0,013 0 0 MgO 0,066 0,688 0,01 0,061 0,042 0,014 0,009 MnO 0,014 4,13 5,285 2,485 0,683 3,068 7,578 K2O 0 0,02 0 0,011 0,179 0,023 0 Al2O3 0,014 1,002 0 0,039 0,233 0,578 0,021 NiO 0 0,068 0 0,013 0,037 0,04 0 CaO 0,039 0,025 1,459 0 0,604 2,844 0 SiO2 0,108 1,996 0,012 0 3,102 3,174 0,012 TiO2 102,227 51,34 53,087 54,236 93,211 51,333 55,238 Total 103,013 101,083 101,497 102,01 102,293 102,878 103,239 Number of cations on the basis of 2O 3O 3O 3O 2O 3O 3O Si 0,001 0,049 0,000 0,000 0,041 0,076 0,000 Al 0,000 0,029 0,000 0,001 0,004 0,016 0,001 Ti 0,993 0,946 0,992 1,006 0,924 0,925 1,010 Cr 0,005 0,000 0,000 0,000 0,000 0,000 0,000 Mg 0,001 0,025 0,000 0,002 0,001 0,000 0,000 Fe2+ 0,001 0,855 0,864 0,930 0,044 0,837 0,820 Mn 0,000 0,086 0,111 0,052 0,008 0,062 0,156 Ni 0,000 0,001 0,000 0,000 0,000 0,001 0,000 Na 0,001 0,002 0,001 0,002 0,003 0,001 0,001 K 0,000 0,001 0,000 0,000 0,003 0,001 0,000 Ca 0,001 0,001 0,039 0,000 0,009 0,073 0,000 Cl 0,000 0,000 0,001 0,001 0,000 0,000 0,000 4.3.2 Iron oxides The magnetite having a size less than 50µm usually occur as disseminated subheudral grains in gabbroic, mafic volcanic and volcanosedimentary wallrock. It also occurs as euheudral 200-500 µm grains in wallrock (sample 88219B) or in quartz vein as (sample 87104DMg). As mentioned before, the magnetite of this quartz vein which also contains pyrite and 30

chalcopyrite is enriched in chromium. In contrary, the analyses of magnetite present within the mineralisation show a rather pure magnetite composition (sample 87104H).

Table 6. Representative electron microprobe analyses of magnetite.

Zone South Central Sample 88209F MG 88219B MG 87104D MG 87104D MG2 87104H MG1 87104H MG2 87119B2 Mg SiO2 0,394 0 0 0,003 0 0 0,19 TiO2 0,117 0,017 0,035 0,001 0,009 0 0,305 Al2O3 0,205 0,028 0,1 0,053 0,035 0,038 0,122 Cr2O3 0 0,141 1,254 0,314 0,007 0 0,556 FeO 90,682 90,61 91,461 89,722 90,962 92,857 91,298 MnO 0 0,016 0,084 0 0,042 0,063 0,068 MgO 0,284 0,01 0,015 0 0,01 0,008 0 CaO 0 0 0 0,003 0 0 0 Na2O 0,01 0,083 0,035 0,073 0,028 0,059 0,017 K2O 0,13 0 0,009 0 0,001 0 0,008 Total 91,822 90,911 93,043 90,171 91,129 93,025 92,564

Number of cations on the basis of 4 O Si 0,015 0,000 0,000 0,000 0,000 0,000 0,007 Ti 0,003 0,001 0,001 0,000 0,000 0,000 0,009 Cr 0,000 0,004 0,038 0,010 0,000 0,000 0,017 Al 0,009 0,001 0,005 0,002 0,002 0,002 0,006 Fe3+ 1,960 2,000 1,958 1,993 2,000 2,003 1,947 Fe2+ 0,988 0,987 0,990 0,989 0,993 0,989 1,011 Mn 0,000 0,001 0,003 0,000 0,001 0,002 0,002 Ni 0,000 0,000 0,002 0,000 0,001 0,000 0,000 Mg 0,016 0,001 0,001 0,000 0,001 0,000 0,000 Ca 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Na 0,001 0,006 0,003 0,006 0,002 0,004 0,001 K 0,006 0,000 0,000 0,000 0,000 0,000 0,000

4.3.3 Sulphides Pyrite

Table 7. Representative results of electron microprobe analyses of pyrites.

Zone South Central East South East Sample 88209I PY 88219G PY 87104D PY 87119BPY 84004FPy 84004QPy 85115O PY1 88057A PY Name py py py py py py py py No. 23 32 13 10 7 8 36 52 Fe 46,957 45,982 46,559 44,95 45,505 46,643 45,826 42,609 Mn 0 0,052 0,019 0,027 0,021 0,003 0 0 Au 0,009 0 0 0,014 0,025 0,046 0,024 0 S 52,301 53,693 53,399 52,692 52,721 53,172 53,164 52,288 Cu 0,026 0 0,045 0,036 0 0,033 0,046 0 Ag 0 0,014 0,025 0,018 0,013 0 0 0 Zn 0 0,092 0 0,062 0,09 0,043 0,026 0,013 Ti 0 0 0,019 0,019 0 0 0,014 0 Total 99,293 99,833 100,066 97,818 98,375 99,94 99,1 94,91 31

The samples have been taken prior to, within and following the mineralisation for each zone. For example, 88209I and 88219G samples have been taken within the mineralisation. Microscopically, 88219G pyrite is a unique grain whiles the other pyrite as a pore-filling texture. Cu, Au, Ag and Zn values are very low and below the detection limit (0,1% wt.) (Tab.6). The hornblende has been formed before pyrite grains which probably come from a first pyrite generation. The other pyrite grains out of the actinolitic hornblende shows similar composition values as the first generation pyrites (see Annexe 3 analyses 43-44, Fig. 17 A).

Pyrrhotite

Table 8. Representative results of electron microprobe analyses of pyrrhotite.

Zone South East South East Sample 88209I PO 84004FPo 85108F PY 85108G PO 88034A PO Name po po po po po No. 22 6 25 27 48 Fe 59,078 59,451 57,959 60,463 57,93 Mn 0 0 0 0 0,021 Au 0 0 0,063 0,009 0,037 S 39,359 38,526 38,94 39,009 39,063 Cu 0,038 0,047 0,051 0 0 Ag 0,012 0 0 0 0 Zn 0 0 0,006 0 0 Ti 0,006 0,004 0 0 0,036 Total 98,493 98,028 97,019 99,481 97,087 Pyrrhotite has been found in vein far from the mineralisation with significant amount of chalcopyrite. From thin section observation of sample 88034A, pyrrhotite is replaced by pyrite (South-East paragenesis sequence). Few samples show low values of Cu and Au below the detection limit (0,1% wt.) (Tab.8).

Chalcopyrite

Table 9. Representative results of electron microprobe analyses of chalcopyrite.

Zone South Central East South-East Sample 88209I CPY 88218c cpy 87104D CPY GOLD87104H CPY 84004MCPy 85108G CPY 85115O CPY2 88034A CPY Name cpy cpy cpy cpy cpy cpy cpy cpy No. 21 41 15 17 3 28 35 47 Fe 30,167 30,669 29,831 29,691 30,419 30,572 30,436 30,052 Mn 0 0 0 0,012 0,006 0,02 0,008 0 Au 0 0 0 0 0,044 0 0,004 0 S 34,317 34,741 34,214 34,729 35,024 34,783 34,609 34,784 Cu 34,019 33,987 34,119 34,628 34,104 33,726 33,833 33,798 Ag 0 0,013 0,002 0 0 0,013 0 0,016 Zn 0,105 0,127 0,044 0,112 0,159 0,095 0,121 0,109 Ti 0,021 0,008 0,007 0 0,003 0 0,007 0 Total 98,629 99,545 98,217 99,172 99,759 99,209 99,018 98,759 32

Zinc values are below the detection limit (0,1% wt.). The average iron content in chalcopyrite is 30,11wt. % and the average copper content is 34,43wt. %. Few samples show low values of Ag and Au over the detection limit (0,1% wt.) (Tab.9).

Others

Table 10. Representative results of electron microprobe analyses of sphalerites.

Zone East Sample 84004MHem sulphid84004FHem sul85108F HEM as85108G sulf MG SULPH Name Sph Sph Sph Sph No. 1 4 26 29 Fe 6,629 5,351 5,356 6,668 Mn 0,093 0,031 0 0,03 Au 0 0 0,004 0 S 32,991 33,305 33,131 33,709 Cu 0,023 0,086 0,239 1,654 Ag 0 0,001 0 0 Zn 60,309 62,808 59,336 60,494 Ti 0,019 0 0,034 0 Total 100,064 101,582 98,1 102,555 Sphalerites have only been observed in the East zone (Fig.19 C). They all are associated with pyrite or/and chalcopyrite. It consists of sub to anheudral 200-500 µm grains. Sphalerites contain low values of Mn and an iron content between 5-6 wt. % and one has a significant Cu value of 1.654 wt.% (Tab.10). All samples have been taken from a volcanosedimentary unit which host the mineralisation and these samples are spatially close to the mineralisation.

4.3.4 Carbonates Table 11. Representative results of electron microprobe analyses of calcites and Ferro-dolomites.

Zone SOUTH EAST SOUTH EAST CENTRAL Sample 88209I CARB88219C CARB84004Mcarb 85108G CARB85115O CARB88057A CARB87119B2 Carb87119B1 Carb Name Fe-Dol Calc Calc Calc Calc Fe-Dol Calc Calc FeO 7,741 0,209 1,171 1,77 0,971 8,104 0,383 0,864 MnO 0,422 0,309 1,111 1,644 1,206 0,597 0,314 0,364 NiO 0 0 0 0 0 0 0 0 MgO 16,028 0,076 0,505 0,666 0,932 15,213 0,446 0,947 CaO 28,136 52,052 51,224 49,266 49,564 27,844 50,465 51,038 CO2 47,673 47,354 45,988 46,655 47,327 48,242 48,392 46,788 Total 100 100 99,999 100,001 100 100 100 100,001

Fe2+ 0,106 0,003 0,017 0,026 0,014 0,113 0,006 0,013 Mn 0,006 0,005 0,016 0,025 0,018 0,008 0,005 0,005 Ni 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Mg 0,393 0,002 0,013 0,018 0,025 0,379 0,012 0,025 Ca 0,495 0,990 0,954 0,932 0,943 0,499 0,977 0,957 Na 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 #Mg 0,787 0,393 0,435 0,401 0,631 0,770 0,675 0,661 CaCO3 0,495 0,990 0,954 0,932 0,943 0,499 0,977 0,957 FeCO3 0,106 0,003 0,017 0,026 0,014 0,113 0,006 0,013 MnCO3 0,006 0,005 0,016 0,025 0,018 0,008 0,005 0,005 MgCO3 0,393 0,002 0,013 0,018 0,025 0,379 0,012 0,025

The amount of Fe ~8 % in dolomite indicate that it consist of Ferro-dolomite. The both Ferro- dolomites have been taken from albite felsite part of the mineralisation from the south and south east zone (Tab.11).

Minor amount of 200-300µm subheudral apatite grains have only been observed and analysed in quartz veins from mafic volcanic to volcano-sedimetary unit only at the south east zone (Tab.12).

Table 12. Representative results of electron microprobe analyses of apatites.

Zone South-East Sample 85115N2 APATITE88057O AP1 88057O AP2 No. 82 87 91 Na2O 0,037 0 0 FeO 0,079 0,138 0,1 Cr2O3 0,016 0,035 0 Cl 1,271 1,253 1,689 MgO 0 0,015 0,014 MnO 0,095 0,22 0,138 K2O 0,016 0,013 0 Al2O3 0,016 0,06 0 NiO 0,015 0 0,021 CaO 53,327 53,542 54,09 SiO2 0 0 0 TiO2 0 0 0 Total 54,585 54,993 55,671

A B

C D

E F

Fig. 20 A: Ilmenite grains from Central sample of gabbroic unit; B: Ilmenites in a biotite-scapolite altered volcano-sedimentary unit; C: Mineralised sample from volcano-sedimentary unit of East zones; D: Graphitic volcanosediment from South-East zone with albite veins; E: Amphibole replaced by chlorite which has been carbonate altered from East zone; F: Carbonate-albite hosted South mineralisation.

Discussion

Alteration zones surrounding the Pahtohavare ore bodies show chemical and mineralogical zonation (Martinsson et al, 1997). The alteration characteristics of the Pahothavare deposit share similar features with other iron oxide and sulphide deposits of the Fennoscandian shield such as e.g. Bidjovagge (Bjørlykke et al, 1987; Bjørlykke et al, 1993) and Rakkurijärvi (Smith et al, 2007).

Similar to Pahtohavare, the alteration associated to the Bidjovagge copper-gold mineralisation includes carbonatisation, scapolitisation, sodic and potassic alteration. The sodic alteration is in both cases the most important one because of its association to mineralisation. The Ernest Henry deposit in Australia shares identical chemical and temporal progression from sodic- to potassic-dominant alteration. This transition may have occurred during the interaction between rock and fluid which evolved via alkali exchange (Mark et al, 2006). The occurrence of sphalerite as anhedral inclusions in chalcopyrite (Figs. 20A and B), subhedral ilmenite grains from mineralised volcano-sedimentary unit surrounding the albite felsite (Fig. 20C), and disseminated rutile in graphitic felsite (Fig. 20D) enhances the similarity between the two deposits (Bjørlykke et al, 1987).

Biotite from Pahtohavare show similar depletion of Al and K as biotite from Rakkurijärvi, a nearby IOCG deposit. These depletions comforts the deduction that chloritisation of biotite is widespread (Smith et al, 2007). Enrichment in Ti has also been noticed from Rakkurijärvi biotite. Few chlorites of the East and Central zone samples from mineralisation within volcanosedimentary and gabbroic units of the Kiruna Greenstone Group show Fe enrichment compared to chlorite from the surrounding alteration. A similar feature has been observed at Rakkurijärvi and Smith et al. (2007) have deduced that the composition of secondary chlorite of the surrounding alteration indicates temperatures from ~300° to 250°C, and chlorites replacing biotite suggest temperatures from ~175° to 100°C. The presence of Fe-rich chlorite support the hypothesis that chlorite have been formed by replacement of biotite and amphibole.

Amphibole showing the richest Cl content (Table 3) is also from the sample which has Fe-rich chlorite and biotite (Table 1-2, Appendix 3). The Cl content of amphibole and biotite is at a similar low range (<0.6 wt %) as the ones from Tjårrojåkka (Edfelt et al, 2005). Another explication of this content could be that the analyses have been done in the Fe-rich rims of actinolite from the Kurravaara conglomerate (Smith et al, 2007). An increase of Cl content in amphibole requires an increase of Fe2+, K and Al content according to Oberti et al. (1993) which is relevant with the tendency of the amphiboles from Pahtohavare (Table 3). If we do not take in consideration the 87104D amphibole due to the zero values, a negative correlation between Mg and Cl contents is distinguishable which probably indicates that Mg- Cl avoidance mechanisms can control the incorporation of halogen in the amphibole structure (Monteiro, et al., 2008). Amphibole comes from samples of least altered units or from the ore 36

in the case of 87119C. It is possible that the generation of amphibole and pyrite are temporally close and that first generation pyrite rather post-date the amphibole generation. The fact that the amount of amphibole and plagioclase decrease towards the alteration zones makes it possible to conclude that the biotite-scapolite alteration has been formed by the decomposition of plagioclase and amphibole in accordance with Martinsson (1997).

Scapolite from scapolite-biotite alteration surrounding the ore-bearing albite felsites and ore veins have a dominant marialitic composition which indicates that the alteration must have been due to highly saline fluids (Pan, 1998). The analyse of scapolite in sample 85115N1 show a marialitic scapolite closer to the albite field on the ternary classification diagram compared with other scapolite grains from samples outside the albite alteration zone. It supports the previous microscopic observations that albite is formed by replacement of scapolite and biotite. The fact that it has been possible to identify albites in a mafic volcanic unit far below the mineralisation indicates that the albite alteration zone is wide spread but strong albitisation is mainly localised at the mineralisation and around vein network. No clear spatial relationship between albite/plagioclase occurrence and mineralisation has been identified. This might be due to the fact that not enough feldspar have been analysed. The An (=Me) content of scapolite is intermediate (0,29-0,42) which is in accordance with what have been agreed in the past (Frietsch et al, 1997). Dipyre seems to be a more accurate name to chemistry of scapolite. The occurrence of dipyre in Pahtohavare can be explained by the fact that the formation of the deposit happened in a Na-Cl rich environment (Frietsch et al, 1997). Moreover, a reddened and silicified part of the metavolcanic unit has been described in core log (Appendix 1, page 72, sample 88218D). There are similar observations from drill cores of Rakkurijärvi. Apatite also occurs as an accessory mineral in the Rakkurijärvi deposit (Smith et al, 2007).

Fluid evolution

The past tectonic events made the Kiruna area having a favorable permeability for epigenetic solutions like saline hydrothermal fluids. This favourable permeability is one of the main important characteristic which explains the formation of Pahtohavare ores. There are two generations of ore-forming fluids at Pahtohavare. The first is a high temperature supersaline fluid which has also deposited iron oxides and most of the carbonate. The second one is a CO2-bearing saline solution. This solution was very reactive with the volcanic rocks of the Pahtohavare area mainly because these rocks were already albitised (Lindblom et al, 1995).

The main physicochemical parameters that controlled hydrothermal alteration and gold mineralisation at Bidjovagge were pH, ƒO2 and temperature (Ettner et al, 1993; Frietsch et al, 1997). The main stage of co-deposition of chalcopyrite-gold at Pahtohavare is characterized by the second generation of ore-forming fluids, aqueous fluids with a salinity up to 30 eq. wt.% NaCl, a temperature below 350°C and a pressure of 1-2 kbar (Lindblom et al, 1995). The high salinity of the fluid can be explained by the metasomatic hydration of biotite 37

and amphibole formation. It is an important factor which determines the precipitation of metals from chloride complexes (Ettner et al, 1993). The destabilisation of gold chloride complexes is the main mechanism of gold deposition. This destabilisation is due to an increase of pH from CO2 loss, cooling and dilution of the solution (Lindblom et al, 1995). Pahtohavare is a copper deposit because of the low concentrations of gold due to the low initial concentrations of gases in the ore fluid. The presence of graphitic schist is essential because it was a redox trap to the hydrothermal solutions which made it as an essential host- rock for mineralisation (Martinsson & Söderholm, 1994). It is possible to say that the chloride complexes of copper and gold are the most important one concerning the transport, but gold- bisulfide complexes could also have been of some importance.

Few hematite grains have been identified. Hematite is often associated with a magnetite-pyrite assemblage. Magnetite is the main oxide mineral as it occurs in much bigger amount than hematite. It is possible to make the hypothesis that the ore-forming solution was within the stability field of hematite rather close to the magnetite-hematite buffering limit resulting in a low capacity for gold transport and a high Cu/Au ratio (Martinsson et al, 1992) (Fig. 20). This is also the case for the Bidjovagge deposit (Bjørlykke et al, 1987). It has been noticed that pyrrhotite is often associated with pyrite which can be explained by a decrease of

ƒO2 triggering the replacement of pyrite by pyrrhotite (Grondin & Williams-Jones, 2004). It is possible to say that pyrrhotite occurrence is spatially related to the mineralisation because it has only been found in samples close or within the mineralisation. The magnetite-pyrite and hematite-pyrite assemblages may have buffered the pH increase and ƒO2 decrease (Ettner et al, 1993). The occurrence of dolomite limits the lower pH boundary to a pH value above 5.2. The pH value of 4.7 indicates the occurrence of albite whereas the absence of K-feldspar and the formation of sericite is limited by the lowest 6.3 pH value (Grondin & Williams-Jones, 2004). The sericitisation and intense carbonatisation can indicate that pH increased (Grondin & Williams-Jones, 2004). Sericitisation is relatively unusual but had been observed and it can indicate that the pH changed to higher values as does the intense carbonatisation (Grondin & Williams-Jones, 2004). From the previous paragenetic sequence obtained from a microscopic study, sericite has been placed at a late stage as it occurs as alteration of feldspar which is in accordance with Figure 20 showing the fluid evolution arrow crossing the sericite limit at the end. Dolomite-forming stages have been placed before and/or after the formation of sulphides and biotite-scapolite. These observations confirm the fluid evolution arrow on Figure 21 which is in the dolomite insolubility field before and after the mineralisation event. Quartz have been mostly positioned at the end of the paragenetic sequence because it has open space and crack filling texture or/and occurs as veins crosscutting albite, carbonate veins. The formation of quartz might be due to a drop in temperature of the fluids which has promoted silica precipitation. The fact that all analysed pyrrhotites (Table 8) come from samples where chalcopyrites have also been identified as in Figure 20 F, makes it possible to end the second arrow in the Po+Cpy field. As it is possible to see from Figure 20 A, B and D, the ilmenite and rutile generation stages can be placed earlier than the scapolite-biotite one in the paragenesis sequence of Central zone. 38

Several types of veins have been identified. Albite and quartz veins seem to be formed in a later stage than the large carbonate mineralised veins. Carbonate-magnetite-pyrite ± chalcopyrite are more common in the large chalcopyrite-carbonate veins which confirm that the fluids had CO2 as a minor phase (Ettner et al, 1993; Lindblom et al, 1995). Chloritisation in veins is often associated with amphibole.

Pahtohavare is considered as a copper deposit rather than a gold deposit (Lindblom et al, 1995). An explanation to this might be that the fluids have not reached the native gold solubility 103 ppb limit for Cl complexes but has crossed the copper 100 ppm limit for Cl complexes. The copper content of the hypersaline brines at Pahtohavare have a range of 100- 500 ppm which is comparable to saline magmatic fluids of the Cloncurry district in Australia (Baker, et al., 2008).

Fluid generation First Second Biotite Scapolite

Magnetite Hematite Ilmenite Rutile Albite Chlorite Apatite Amphibole Carbonates Pyrite Chalcopyrite Pyrrhotite Sphalerite

Mineral paragenesis Sericite Quartz

Potassic biotite-scapolite alteration Sodic albite alteration Sulphide mineralisation Weathering/Supergene Fig.21 Paragenetic sequence and spatial distribution of pre- and syn-ore alteration.

Fig. 22 Phase diagram showing the stability fields of ore and selected alteration minerals at pressure-temperature conditions estimated for the Kiruna area. Ab=albite, Bn= bornite, Ccp= chalcopyrite, Hem= hematite, Kfs= K- feldspar, Mag= magnetite, Ms= muscovite, Pg= paragonite, Po= pyrrhotite, Py= pyrite (Grondin & Williams- Jones, 2004).

Several possible exploration tools

The geochemical discrimination diagrams (Fig.12) allow us to see that addition of potassium and the depletion of calcium and manganese are characteristic of the biotite- scapolite alteration zone. The ore-bearing albite carbonate alteration zone shows the following chemical changes: K2O is depleted and Na2O, CaO and MnO are enriched. The Tjårrojåkka deposit whole-rock geochemistry indicates the same features (Edfelt et al, 2005). The relation between the depletion of Na and alteration such as scapolitisation and albitisation is close as it is likely due to Na-Ca exchange reactions (Smith et al, 2012). It is also possible to say that a single element is not a reliable geochemical discriminant. However, co-variation diagrams as the one presented in Fig.13 are possible geochemical discriminants which can be used as an exploration tool in order to locate Cu mineralisation. Bjørlykke et al (1993) suggested that the low to medium metamorphic boundary could be used as an exploration criteria for mesothermal Au-Cu deposits in the Svecokarelian unit. The importance of CH4 as a 40

geochemical tracer to gold mineralisation still need to be clearly determined for Pahtohavare (Ettner, Bjørlykke, & Andersen, 1993). The rather low Pb and Zn concentration (Appendix 2) in the ore may be evidence for them being soluble in the ore fluid as they also have higher solubility compared to Cu. The Ernest Henry deposit also shows this characteristic (Mark et al, 2006). The Mg variation of biotites decrease toward the ores of the South, East and South east zone while it is the contrary in the Central zone which has also been noticed from Tjårrojåkka where biotites from Cu-mineralised samples are generally more Mg-rich (Edfelt et al, 2005). Due to the low number of biotite analyses, further studies are recommended in order to confirm the reliability of this exploration tool.

Fig.22 Biotite #Mg variation diagram against distance in meters and generalised schema of alteration sequences and chemical changes toward the ore. Ores have been defined from geochemical values ≥0,2 wt. % of Cu. 41

Conclusion

Pahtohavare is considered as a copper deposit rather than a gold one due to the small concentration of gold explained by the ore forming fluid evolution. A first hypersaline solution is believed to have prepared the deposition of sulphides from the second fluid, which is has lower salinity and temperature. The early titanium oxides, biotite-scapolite alteration, albitisation and the destruction of graphite are believed to be the trace of this early solution. The resulting chemical reactions are the main important factors promoting the ore deposition by decreasing ƒO2 and increasing pH. The study of thin sections made the creation of mineral paragenesis sequence possible and supports the hypothesis concerning the evolution of the ore forming fluids. Mineral paragenesis sequences of each ores have been made and despite small differences on mineral generations, they are rather similar. These differences can be explain by the fact that Central ores seem to have been more affected by supergene oxidation and weathering than others, and East ores are syngenetic Viscaria type.

Depletion and addition of elements are noticeable from geochemical analyses and can give great information associated to core logging descriptions in order to locate a potentially ore. Mineral chemistry can also be used as an exploration tool. Moreover, the results give important informations for the understanding of fluid evolution. The #Mg variation of biotite toward mineralisation is one particular factor that needs to be further studied.

Finally, Pahtohavare shares several similar characteristics with other deposits as Tjårrojåkka, Rakkurijärvi and Bidjovagge. Any new publications on these deposits can be very useful in order to increase our knowledge of the Pahtohavare deposit.

Acknowledgments

I would like to thank all members of the Hannans Reward team which consist of Damian Hicks, Lewis Wild, Jörgen Lindsköld and Jan Ehrenborg. A special thanks to Christina Lundmark and Amanda Scott for their assistance, patience and great help. I am very grateful to the SGU for the access to the drillcores and facilities. The author is also thankful to Olof Martinsson and Christina Wanhainen who provided very valuable corrections and advices. Zimer Sarlus has as well spent much time to help the author to get great quality pictures. Thanks are also due to Francisco Javier Morales Blasco who has supported the author in many ways. Then, I would like to finish by a great thank you to LTU and Hannans Reward for their financing.

References

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Appendix

Appendix 1: Core logs p 47-74

Appendix 2: Geochemical analyses p 74-76

Appendix 3: Microprobe analyses p 76-80

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -55˚ 85108 E 700N 800W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =216,15m Grain size Alteration Sulphide (%)

2 4 6 8 Depth unitRock Description

Fine Medium Coarse Weak Moderate Strong Legends 0 m 0.00-6.75m: Overbudden po py As Sl Cp

Visible Gold

6.75-12.75m: Mafic volcano-sedimentary rock Grey massive. With graphitic fragments Albitisation

10m Carbonitization biotite silicification (chert)

12.75-14.20m: Graphitic silt-shale Magnetite Scapolitisation Chloritisation

14.20-17.00m: Mafic volcanic rock Green massive. 15.30m: chert inclusion Abbreviations 17.70-19.90m: Mafic volcano-sedimentary rock Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy Carbonate as patches, vein or filling cracks. = Chalcopyrite, Cb= Carbonate,dol=dolomite,Ab=albite,scp=scapolite, 20m 19.90-30.00m: Graphitic silt-shale Phl=phlogopite, tlc=talc Banded parallel to CA. Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

Chert 30m 30.00-56.35m: Mafic gabbroic rock Diffused contact, greenish-grey, brecciated and altered Graphitic silt-shale

Mafic-intermediate volcanic rock

40m

Sulphides filling cracks

50m

56.35-70.00m: Mafic volcanic rock Grey-bluish massive, cracked.

60m 60.15-70.00m: Banded

47 70m 70.00-80.45m: Mafic volcano-sedimentary rock 70.00-80.45m: Carbonate bands

74.00-91.60m: Graphitic bands subperpendicular to CA

80m

80.45-95.25m: Graphitic tuffite 80.45-91.60m: crosscutted by carbonate vein containing fragment of graphitic tuffite.

90m

95.25-99.65m: Banded graphitic shale-silt

100 m 99.65-103.95m: Chert

103.95-109.20m: Mafic volcano-sedimentary rock

109.20-116.95m: Graphitic shale-silt 110m

116.95-204.75m: Mafic volcano-sedimentary rock

120m 120.10-129.80m: Carbonate banded tuffite

130m 129.80-132.45m: Graphitic tuffite

136.40-147.20m: banded

140m

142.50-142.80m: graphitic band with cp and po.

146.15-147.20m: graphitic band with cp and po. 85108E: 146.50m

150m At 151.30 and 151.80m: carbonate band 48

158.00-158.60m: Cp impregnations 160m

170m

179.15-184.75m: graphitic band sub perpendicular to CA 180m

190m 85108F: 190.00m

85108G: 193.60m

200m

204.75-216.15m: Mafic gabbroic rock, probably hornblendite

210m

E.O.H: 216.15m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 84004 E 889N 819W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =230,91m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-2.77m: Overbudden po py As Sl Cp 2.77-42.60m: Mafic volcanic rock Massive, composition variations between (+)biotite (+)hornblende Carbonate filling thin veins, cracks (mm) Visible Gold Foliated and weakly sheared

Albitisation

10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation 84004C: 14.80m

Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m From 20.30m: start to be Qz-Alb(?) veined and figures of ductile deformation , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Banded graphitic tuffite

30m

Graphitic silt-shale

Mafic volcanic rock

40m

42.60-58.60m: Mafic volcano-sedimentary rock Weakly sheared

50m

54.25-55.65m: graphitic silt, diffused contact, foliated/deformed. 84004D: 54.75m

58.60-61.50m: Graphitic silt-shale 60m 61.50-63.65m: Mafic volcano-sedimentary rock Generally, carbonate increase near contacts.

63.65-65.50m: Graphitic silt-shale 65.50-67.35m: Mafic volcano-sedimentary rock

67.35-69.50m: Graphitic silt-shale

69.50-72.10m: Mafic volcano-sedimentary rock 50 70m

72.10-76.25m: Graphitic silt-shale

At 74.20m: oxidized 10cm semi-massive Cp (?)

76.25-81.45m: Banded graphitic tuffite 84004F: 77.60m Strongly altered Band 70-80° to CA 80m

Contact 45° to CA 81.45-84.30m: Graphitic silt-shale Sulfides as veintlets/vein. Figures of mixing. 84.30-91.15m: Banded graphitic tuffite Bands 80° subperpendicular to CA

84004I: 87.80m

90m

91.15-94.45m: Graphitic silt-shale Net contact (80° to CA), Po as patches, veintlets or disseminated. 94.45-147.10m: Banded Mafic volcano-sedimentary rock

84004K: 96.90m

100 m 99.00-110.00m: greenish color rock

106.70-107.30m: Graphitic silt-shale

110m 110.60-111.40m: Graphitic silt-shale

120m

130m

140m

84004M: 142.90m 143.10-147.10: banded (scp+biot bands)

147.10-151.10m: Banded graphitic tuffite 51 150m

151.10-230.91m: Banded Mafic volcano-sedimentary rock 153.50-154.50m: magnetite bands sub perpendicular to CA

160m 161.00-162.00m: Quartz-Carbonate breccia with massive Po.

Po in cracks, vein and associated with carb and Qz vein (30° to CA) at 165.50m.

170m

180m

190m

200m 201.50-202.10m: thin veins of Qz+biot+trace Py+(Chl) sub parallel to CA

210m

84004Q: 212.65m

220m

222.36-230.91m: strongly veined ( thin, carb-alb(?))

230m E.O.H: 230.91m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 87104 C 1305 N 1770 W Starting date = Completion date = Core diameter = 76mm Length (EHO) =224.10m Grain size Alteration Sulphide (%)

Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Edited from Log Jan Ehrenborg 2013 Legends 0 m 0.00-3.50m: Overbudden The upper part of the core is often rather-very rusty, weathered and broken-crushed. It is often difficult to be certain about the po py As Sl Cp origin of the fragments (or if they really exist). The term agglomerate has been used consistently through out this log by the earlier logging geologist. The word breccia would be much more descriptive and also non-genetic while agglomerate always indicate both volcanic material and processes. I have interpreted the upper 3,20-18,38m interval as most likely a primary volcanic breccia (or Visible Gold possibly a combination with sedimentary processes to give e.g. some kind of slump-deposit(?). Other breccias in the core could be formed by a number of processes, except primary volcanic fragmentation. Different processes could have been active in different places, such as deformation and hydrothermal activity, or a combination of two or three of these processes.It must also be pointed Albitisation out that some intervals in this core seems to be made up of banded-laminated rather than fragmented lithologies indicating a coarse banding between breccias and layered sediments. Difficult to observe deformation marked by folding and foliation has 10m thereafter overprinted the lithologies and made observations much more problematic. Carbonitization biotite silicification 3.50-55.50m: Mafic volcanic rock (chert) 9,47-12,29m: Mafic matrix-supported breccia (=slump-deposit?). Fragments rarely >0,5cm in size. Py-impregnated, some chl. Lowest part of this interval rusty + crushed. Magnetite Scapolitisation Chloritisation 12.29-18,38m: Mafic matrix-supported breccia (=slump-deposit?). Fragments bigger than above, <10cm in size. Py-impregnated, some chl. Foliation sub parallell with drill core= weak ductile-shear-zone. At approx 16,00 - 18,38m the angle between core and foliation-fragment orientation = 40-60 degrees to core. Px-porphyroblasts. Few cb-veinlets. Trace of ep + a red mineral. Abbreviations 18.38-20.40m: Dark grey, vf, laminated layering (undulating sub parallell with core), mafic rock (tuffite?). Some mt-impregn. Py- Cb= carbonate, Py = Pyrite, Po = Pyrrhotite, impregnated after qz-vein infiltration. Qz-veins which have been broken + fragment-rotated indicating movements along foliation- Px=pyroxene, Cp = Chalcopyrite, Bn= bornite planes which might be sub parallell with layering. Some chlorite. 20m 20.40-21.77m: Mafic rock, totally chrushed. Some py-impregnation. 21.77-25.44m: Mafic rock mostly totally crushed. Some rust indicating py-impregnation. Qz-veins which have been broken + fragment-rotated indicating movements along foliation-planes. Semi-flat core-pieces indicate lamination= layering or Overburden 25.44-26.25m: Grey (with rusty spots-schlieren), vf, eg, laminated (layering-foliation?), mafic tuffitic rock. Some py. Lamination ondulates sub parallell with core. Qz-fragments from broken qz-veins, later qz-fragments rotated indicating Mafic Volcano-sedimentary rock movements along lamination-planes. Lamination undulations = small-scale. Small-scale undulation-folds = NO axial-plane 26.25-30.32m: Strongly weathered, greenish-rust brown, eg, laminated (layering-foliation?), mafic tuffitic rock. Some py+mt Graphitic silt impregn. Lamination undulates sub parallell with core. Qz-fragments from broken qz-veins, later qz-fragments rotated indicating movements along lamination-planes. Lamination undulations = small-scale. Small-scale undulation-folds = NO 30m axial-plane foliation. When the lamination is broken the reason is probably deformation NOT primary fragments. Mafic volcanic rock 30.32-31.70m: Rusty, strongly weathered, crushed, possibly the same as above= mafic tuffite(?). Small qz-peaces. Some mt. 31.70-35.68m: Weathered, mostly crushed, rusty, mafic volcanite. Locally banded, laminated (=layering?), semi-massive. Some mt. Mafic gabbroic rock 35.68-42.95m:Looks banded to fragmented. When banded= alternating green and grey vf bands. Uncertain if fragments are primary or secondary= tectonic e.g. through folding+faulting or both primary and folding+faulting. It is thus not unlikely that the rock Breccia contains both primary and secondary fragments. Mafic-intermediate volcanite-breccia/tuffite. Elongated schlieren-like mt- fragments in breccia. Hard "fragments" possible chert at 37,50m, also mt-band close. Mt-groundmass = 12-18%. Some py. Rich in py Massive chert + trace of bn close to lower contact (42.45-42,95m). Cherty tuffite

Magnetite ore 40m

42.95-47.73m: Somewhat weathered, greyish green, brecciated - massive, mafic (-intermed) volcanite. Locally laminated - foliated. Generally some py and py-rich in interval 43,30-43,80m. Not as soily and loose as mullmalm (=weathered soily ore). Mt occur but generally in low/very low concentration = NOT even weak ore. Locally hard core might be cherty rock. Chlorite as spots and fracture coatings. Locally foliated sub parallell core and 37 degrees to core.

47.73-50.98m: Rust-green, breccia, mafic rock. The material is proabably volcanic but the breccia is possibly hydrothermal. The breccia in interval 3,20-18,38m is a primary mostly matrix supported breccia while the breccia in interval 47,73-50,98m is something between a breccia and a fractured rock. Some py and very little mt. 50m

50.98-54.70m: The core loss = 3,30m is 89% of this interval and the rest of the core pieces are just sub rounded gravel to small stones in size. Rust-grey, mafic rock. Some mt. 54.70-55.50m: The core loss = 0,55m is 67% of this interval and the few core pieces left are stone-size. Rust-green mafic rock. Very small amount of mt and a few small qz-patches= proabably fragments from broken qz-veins. Foliation-surfaces, also cutting, indicate movements/rotations along these planes. 55.50-59.55m: Weathered, rusty-greenish-grey, banded-laminated, mafic volcanite (tuffite?). Py as spots and schlieren sub parallell banding-lamination. Very little mt. The banding-lamination (25-40 degrees to core) looks partly primary and partly secondary (=foliation-part of shear zone?). The primary appearance of the banding-lamination indicate a possible tuffite. The lower contact looks like it is cutting this banded volcanite and both rocks are cut by foliation and tectonically disturbed. Contact= 22 degrees to core, foliation cutting contact= 30 degrees to core.NOT enough chlorite to call the rock chlorite schist. 60m 59.55-63.55m: Grey, vf-fg, eg, semi-massive, mafic rock, probably a dyke (indicated by the semi-massive appearance + probable cutting upper contact). Somewhat magnetic with very low amount of mt. Seem to be rich in px. The rock is rather fractured to locally in situ brecciated but no true fragments have been observed. Fractures + in-situ-breccc-matrix often rusty. 63.55-64.61m: Weathered, rusty-greenish-grey, vf, diffusely banded, mafic volcanite (tuffite?). Some py and locally very little mt. Banding looks primary + tectonically modified. No primary fragments have been observed = can´t be an agglomerate. 64.61-70.20m: Greenish, foliated, breccia, mafic volcanite. Banding in some core pieces looks foliated/sheared and even if it 53 originally is some kind of primary banding it now looks secondary, foliated. The breccia carries small elongated mt-fragments (sub parallell with foliation) to mt-schlieren. Weak very small-grained py-impregn. Only secondary sheared fragments? indicating part of shear zone. Some vf py-impregn + fewer py-schlieren. 70.20-75.45m: Mafic tuffite 70m 70.20-70.90m: Greenish grey, vf, banded, mafic tuffite. With mt-rich bands. Towards upper part folded bands + rotated py-"lumps" showing that py was introduced before a folding event. 70.90-75.30m: Greenish grey, vf, eg, banded (probably layering), mafic tuffite. Black sub-mm dots= chl or chl-altered px. Locally some scp. Banding 50 degrees to core. Vf-py as thin fracture fillings and impregn. At 72,55-72,65m= 1 cm thick mt-carrying shear zone (12 degrees to core) in undeformed tuffite. 88104D=71.85m 75.30-75.45m: Greenish grey, vf-silty, eg, banded (1-6mm) 48 degrees to core, mafic tuffite. Py (not uncommon) mostly along banding + fractures. Few possible scp-porphyroblasts. 75.45-76.05m: Grey, vf, eg, semi-massive, mafic volcanite. Thin shear-zone with py sub parallell with core. Py also along fractures. Few scattered black px-porphyroblasts <1mm.

76.05-79.80m: Greenish grey, vf-silty, eg, banded (1-6mm) 52degrees to core, mafic tuffite. Py (not uncommon) mostly along 80m banding + fractures. Few bands with scp (porphyroblasts)-bt. Also very few bands with px-porphyroblasts. 79.80-81.55m: Light grey, vf-silty, eg, diffusely-banded to semi-massive, cherty tuffite. Py occur in greenish fractures (very rarely solitary grains in the groundmass. 81.55-81.90m: Greenish grey, vf, eg, massive, mafic volc. Some py along fractures and trace of bornite also along fractures. 81.90-83.90m: Greenish grey, dissordered-breccia,slump(?)-deposit.The slump-matrix is rather rich in py.This and other similar deposits in this core is interpreted as primary breccias (=slump deposit) wich might have a tectonic origin e.g. earthquakes. It is NOT likely to be a tectonic breccia becuase of lack of tectonic structures and fractures in the wall-rock. Light grey fragments are rather hard indicating chert, why the chert silica is older than the slump-deposit = from the time of deposition and NOT from a younger tectonic event. 83.90-85.20m: Greenish-brownish-grey, vf, semi-massive, mafic volcanite. Locally hard indicating cherty. The brownish colour is 90m from the lower part of the section which probably is bt-rich and holds scattered px-porphyroblasts. Py as very few and small scattered grains or bigger patches. 85.20-86.20m: Greenish grey, vf, banded, banded-slumped cherty mafic, scattered py rather much (probably mostly in fractuers and slump-matrix). Trace of very small bornite grains on fracture. 86.20-89.80m: Grey, vf, banded-semi massive, chert. Py on chloritic- and on skarn-fractures. 89.80-95.50m: Brownish-greenish-grey, vf, porphyroblastic, banded cherty tuffite. Banding 48 degrees to core. The cherty tuffite is banded with greenish (amp-px(?)-rich bands) alternating with greyish chert-rich bands. Interstratified occur rather frequently occurring brownish bt-scp (porphyroblasts) bands. Locally thin skarn-fractures and also very local black px-porphyroblasts. A 1 cm thick mt-py-band with cb (=carbonate, white or red) at 88,24m marks a more general occurrence of py (especially along and within fractures) and scattered fractures + patches and of carbonate towards greater depths. Trace of cp-bn. Mt occur locally (rarely) as 100m patches. Mt-cb-cp-bn-py seems often to occur together. Cp-bn occur with cb and in fractures. Cp-bn occur with carbonate especially at 89,15m, at 91,00m in fractures in vf bt-band and 93,68m within cb-skarn-schliere. 87104G: 93.55m 95.50-100.20m: Alternating between grey-banded to semi massive-cherty tuffite and greenish grey dissordered mafic slump- deposits partly with cherty fragments. Greenish slump-matrix is rather rich in py in patches-bands- scattered grains and also carry trace of bn as solitary very small grains. 100.20-101.60m: Greenish grey, Mafic slump-deposit. Partly cherty fragments. Carbonate in patches. Slump-matrix chloritic and relatively rich in py as patches and scattered grains. 101.60-102.00m: Grey, massive-disturbed semi-banded, chert. Py as fracture filling esepecially when greenish skarn occurs. 102.00-102.85m: Grey, semi-massive, chert. Some py in fractures. 102.85-102.98m: Greenish grey, slump-deposit/dissordered rock, chert. Slump/dissordered rock - matrix holds rather much py. 110m 102.98-104.50m: Grey, massive (also banded) chert. Some py in fractures and scattered individual grains. 104.50-105.13m: Greenish grey, mafic slump/disordered-deposit. Some py in matrix and fractures. 105.13-105.57m: Grey, massive, chert, some little py in fractures. 105.57-105.87m: Greenish grey, mafic slump-deposit, with some chl and py in slump-matrix. Fragments partly cherty. 105.85-107.05m: Grey, semi-massive, tuffite, (15-cm thick chert-section), py mainly in irregular fractures. 107.05-108.78m: Alternating between grey semi massive-cherty tuffite deposits and greenish grey dissordered mafic slump- deposits with cherty-tuffitic fragments. Greenish slump-matrix is rather rich in py occurring in patches-bands- and as scattered grains. Some py bin fractures in the chert. 108.78-110.11m: Greenish grey, mafic slump-deposit, mainly with chert-fragments. Slump-matrix with chl and py. 110.11-112.12m: Grey semi-massive, cherty tuffite. Py especially in fractures, very little cp at 111,12m. 120m 112.12-112.89m: Greenish grey, mafic slump-deposit, few scattered solitary py-grains in slump-matrix. 112.89-113.53m: Grey, massive, tuffite (possibly somewhat cherty), few thin carbonate-fractures. 113.53-113.86m: Brownish-greenish-grey, vf, px-porphyroblastic, massive, mafic tuffite. Very little py in fractures and as scattered solitary crystals. Rather frequent with mm-cm-thick carbonate-skarn fractures. Cb-py-skarn occur together and px-porphyroblasts grow mostly in the groundmass but also in cb-veins. Mt might occur but nothing is felt with the magnet. 113.86-114.05m: Greyish white, carbonate vein rather rich in solitary py-crystals and sparsely dotted with black px-porphyroblasts. 114.05-118.00m: Greyish green, vf, massive (locally very diffuse lamination), mafic volcanite-tuffite. Occassionally thin cb-fractures. 118.00-118.27m: Brownish grey, chert 118.27-118.33m: Greenish grey, massive, mafic volcanite, 5mm thick py-band. 118.33-118.38m: Carbonate vein, brecciating the mafic volcanite (tuffite), rich in wall-rock fragments. 130m 118.38-118.67m: Grey, massive-banded/laminated, chert. Some laminations = py. Py also occur in in-situ breccia-fractures. 118.67-121.40m: Greyish green, vf, massive-laminated, mafic volcanite-tuffite. With a cb-patch. Lamination(-banding) occur at 119,30-119,60m. It partly looks as fractures BUT it also looks like graded bedding indicating a primary layering + later fractures sub- parallell with the layering. Layering = 16 degrees to core. 118.67-121.80m: Compact mt rich in py and with patches of cb. 87104H: 121.45m 121.80-124.12m: Greyish green, vf, massive, mafic volcanite. Locally chl-amp-fractures with some cb and very rare py. 124.12-124.52m: Greyish green, vf, layered, mafic tuffite. Probably graded bedding, showing up towards depth (= overturned layering). Layering= 47 degrees to core. A 6mm high normal fault along a slump-structure, with intact layering above and below, also show up towards depth (= overturned layering). 124.52-128.51m: Greenish grey, vf, massive, volcanite (tuffite?),sparsely occurring thin cb-fractures, few <1cm thick irregular 140m disturbances/slump(?)-bands.

128.51-128.75m: Greenish grey, massive-fragment oriented slump-deposit, some py in slump-matrix, some chl in slump-matrix. 128.75-131.29m: Greenish grey, vf, massive- mineral lineated, volcanite. Few thin cb-fractures, maf-vein sub parallell with core and with cb-fractures along vein-contacts, px-porphyroblasts in fracture-borders, some very small scp-porphyroblasts. 131.29-132.79m: Greenish grey, mineral/fragment oriented slump-deposit, some py in slump-matrix, some chl in slump-matrix. 132.79-133.70m: Grey, vf, banded, mineral lineated, somewhat disordered tuffite, few thin chl-bands, some px-porphyroblasts. 133.70-143.49m:Greenish grey, porphyroblastic, massive,mafic volcanite.Scp frequent as porphyroblasts<2mm(commonly 1mm) and as mm-cm-thick bands.Very thin, sparsely occurring cb-veinlets.Lower contact=18° 87104J: 143.30m 143.49-144.04m: Greenish grey, mg, eg, massive, gabbroic rock. 54 144.04-144.58m: Greenish grey, vf, porphyroblastic, massive, mafic volcanite. Porphyroblasts= small, scars, scattered= scp + px. 150m 144.58-144.69: Greenish grey, eg, massive, gabbroic rock. On one side of the core, on the other vf mafic volcanite. The gabbroic rock undulates in and out of the core, sub parallell with core(?). 144.69-145.35m: Greenish grey, vf, porphyroblastic, massive volcanite. Porphyroblasts = <1mm big scp. 145.35-147.60m: Greenish grey, mg, pl-phyric (?), massive, gabbroic rock. Probably the beginning of a rather thick gabbroic- porphyritic dyke. Scp especially close to upper contact. Upper contact = 31 degrees to core. 147.60-147.80m: Dark greenish grey, vf, pl-phyric, massive porphyrite dyke. Fine grained chilled margins. 147.80-150.19m: Greenish grey, sem-massive, gabbroic rock, (scp?). Continuation of gabbroic dyke in interval 145,35-147,60. 150.19-153.90m: Greenish grey, massive, gabbroic rock. Coarser part of the gabbroic dyke in intervals 145,35-150,19m. 153.90-155.00m: Greenish grey, mg, pl-phyric (2-4mm), massive, mafic-gabbroic rock. Mt=scattered weak. 155.00-155.96m: Greenish grey, vf-fg, pl-phyric (1-2mm), massive, mafic-gabbroic rock. 160m 155.96-157.50m: Greenish grey, mg, eg, massive, gabbroic rock. Grain seiz smaller downwards in hole. Trace of py on chl-fracture.

157.50-157.88m: Greenish grey, vf-fg, pl-phyric (1-2mm), massive, mafic-gabbroic rock. 157.88-165.35m: Greenish grey,vf-fg,massive, mafic-gabbroic rock.Locally scp-porphyroblasts.Chl coated fractures with trace of py. 165.35-166.40m: Greenish grey, vf-fg, eg, massive, mafic-gabbroic rock. Weak cb-schlieren/veins with trace of py and cp. 166.40-177.37m: Greenish grey, vf-fg, eg, massive, mafic-gabbroic rock. Very few cb-schlieren/veins with trace of py and cp (almost less than trace), mostly on factures.

170m

177.37-178.31m: Greenish grey, vf-fg, eg, massive, mafic-gabbroic rock. Rich in cb-schlieren/veins with some cpmostly in cb-veins. 178.31-178.47m: Carbonate vein, with some qz, rathyer good in cp + more brownish Cu-mineral. Lower contact = 18 degrees to core. 178.47-184.00m: Greenish grey, vf-fg, eg, massive, mafic-gabbroic rock. Irregularily distributed areas with scp-porphyroblasts. Poor in cb-(qz)-veinlets. 180m

184.00-187.20m: Greenish grey, fine mg, eg, massive, mafic-gabbroic rock. With very few cb-qz-veins.

187,20-194,20m: Greenish grey, fine mg, eg, massive, mafic-gabbroic rock. With very few cb-qz-veins.

190m

194.20-198.67m: Greenish grey, fine mg, eg, massive, mafic-gabbroic rock. More cb-qz-veinlets than above (not much). The rock looks more heterogeneous than above with parts with with less of the light mineral (=pl/scp). This might be the result of thin shear zones which e.g. following cb-qz-veins, very rich in bt and rather poor in the light mineral compared to the rest. At 195,23-195,27m a 1cm thick qz-vein (29 degrees to core) is surrounded by a bt-rich + light-mineral-poor shear zone. Also few chl-coated fractures.There might be a relation between closeness to the lower contact + more cb-qz-veinlets + thin shear zones + cp-trace. 198.67-198.74m: Magnetite-ore-band (24 degrees to core), dark grey, vf, compact, 1-1.5cm thick, with small cb-schlieren. Both the 200m magnetite and the surrounding gabbroic rock is a patchy-net work distribution of cp. 198.74-201.72m: Brownish (greenish)-grey, vf, leipido-grano blastic, foliated-semi massive, mafic rock-schist. Might partly be a ductile shear zone sub parallell with the core. Rich in chl/bt or both at least in the foliated parts. There is also a diffuse banding sub parallell with the core. CB-qz-veins/schlieren often sub parallell with core. Rather rich in cp which seem to be related first of all to the cb-qz-veins but also to the foliation. The primary rock can NOT be identified. Start wondering if there might be several dykes from 198,74 and down-wards and not (so much) mafic volcanite. 201.72-202.31m: Compact, vf, magnetite-ore-band, rich in cb-schlieren and cp. The biggest cp-patch irregular and >5cm long. 202.31-203.75m: Grey, vf-fg, eg, massive- semi massive, mafic rock. Few chl-coated fractures, somewhat heterogeneous, poor in cb- schlieren/veinlets which holds trace of cp close to contacts. A dyke cutting the vf mafic rock? 203.75-205.92m: Broken to locally crushed, brownish-greenish-grey, vf, porphyroblastic-scp, heterogeneous, semi-massive, mafic 210m rock. Chl/(bt?) and locally a greesy feeling = talc (?). Possibly some thin foliation-zones at low angle to core. Few cb-schlieren. Some cp and trace of bn especially together with cb. 205.92-206.17m: Carbonate-vein + some mafic rock. Rich in scattered cp-patches. 206.17-209.94m: Grey, vf-fg, eg, massive, mafic rock. Locally a fragmented appearance. Poor in cb-schlieren/veinlets which holds trace of cp, more cp in interval 207,87-208,10m. A dyke cutting the vf mafic rock? 299.94-210.23m: Grey, vf-fg, eg, massive, mafic rock. A dyke cutting the vf mafic rock? Cut by cb-veins rather rich in cp and bn. 210.23-210.35m: Carbonate-vein, rather rich in multi-coloured Cu-minberals like cp and bn. 210.35-210.42m: Brownish grey, vf, porphyroblastic-scp, mafic rock. Proabably rich in bt/chl. 210.42-210.72m: Carbonate-vein, scattered px- or amp- crystals. 210.72-210.81m: Carbonate-vein, with cp + bn + mt (lower contact of carbonate-vein above). 220m 210.81-211.70m: Greenish grey, vf, eg, massive, mafic rock. Some scp. Poor in cb-veins with trace of cp. 211.70-216.38m: Greenish grey, vf, porphyroblastic-scp, massive, mafic rock. Very poor in cb-veinlets. 216.38-222.50m: Greenish grey, vf, porphyroblastic-scp, massive, mafic rock. Some cb-veinlets. Trace of bn. 222.50-224.10m: Greenish grey, fine mg, eg, massive, gabbroic rock. E.O.H: 224.10m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -45˚ 87119 C 1247 N 1900 W Starting date = Completion date = Core diameter = 76 mm Length (EHO) =142.24m Grain size Alteration Sulphide (%)

Rock

Depth unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-3.50m: Overbudden po py As Sl Ccp

3.50-42.95m: Mafic-intermediate Volcanosedimentary rock, probably tuffite. Massive fine grained grey matrice with some darker probably basaltic intercalations. Visible Gold 97119A: 5.75m

At 9.00m: scapolite seems to be more present in some beds. 10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation At 14.30m: quartz fillling cracks+Chl+oxidized Py(?).

Abbreviations Strong scapolitisation : matrice becoming dark (biotite?) As = Arsenopyrite, Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Gl= galena Plf = Phyllosilicate lined fractures 20m

Overburden At 23.35m: 10cm talc+ graphite (?)+magnetite Mafic volcano-sedimentary rock

Graphitic Silt 27.10-27.50m: Brecciated tuffite 29.30-29.45m: oxidized altered tuffite+magnetite-graphite and oxidized sulpfides. Friable (tectonised?) Cherted-silicified tuffite 30m

Chert breccia

Gabbroic rock At 34.35m: well preserved tuffite 35.75m: Carb+Chl+Qz vein 30° to CA Mafic volcanic rock 36.20m: irregular contact with a 10cm quartz vein. 38.40-38.60m: clasts of quartz. 87119B: 37.25m

40m

87119C: 42.80m 42.95-88.45m: Mafic volcanic rock, probably basaltic. Sharp irregular contact. Fine grained massive dark rock. 45.50-45.70m: carbonate filling cracks with Py and chl?

50m

60m

Oxidation in cracks and redish scapolite

(?) 70m

74.30-75.30m: brecciated basaltic volcanite

80m

88.45-88.80m: Breccia 80.80-90.10m: Cherted tuffite and Fe oxides. 90m 90.10-92.80m: Oxidized mafic volcanic rock.

92.80-95.35m: Graphitic silt.

95.35-99.35m: Mafic-Intermediate Volcanosedimendary, probably tuffite. Massive fine grained. Talc in cracks and pieces of altered graphitic silt (98.00-99.35m)

99.35-103.80m: Graphitic silt 100 m net contact 40° to CA

103.80-112.50m: Mafic volcanic rock, probably basaltic. Talc in cracks At 106.30m: thin vein of felspar (?) perpendicular to CA.

110m

112.50-120.70m: Mafic-Intermediate Volcanosedimendary, probably tuffite. Diffused contact Greyish fine grained. Talc filling cracks (113.20-113.50)

120m

120.70-122.50m: Chert breccia OR strong silicification 121.00: Cpy in graphitic clast or between clasts 122.50-133.40m: Cherted mafic-intermediate volcanosedimentary, probably tuffite. Silicified Bands perpendicular to CA.

130m

133.40-142.24m: Basic gabbroic rock, probably hornblendite Massive, compact.

140m

E.O.H: 142.24m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 87127 C 1230N 1988W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =149.35m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-3.50m: Overbudden po py As Sl Cp

3.50-50.10m: Mafic volcano-sedimentary rock, probably tuffite. Visible Gold Grey blueish compact Banded Albitisation

10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation

Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

Cherty breccia 30m

Graphitic silt-shale

40m

50m 50.40-55.40m: Graphitic silt

87127C: 53.60m

55.40m-58.50m: Graphitic mafic volcanosedimentary, tuffite

58.50-74.30m: Graphitic silt 60m

70m

74.30-105.40m: Mafic volcanosedimentary, probably tuffite

80m

90m

87127F: 92.10m 93.70-96.00m: Cherty breccia, banded.

96.00-105.40m: Tuffitic banded breccia

100 m

105.40-149.35m: Mafic gabbroic rock. 105.40-132.20m: porphyritic texture with small cherty part. Amphibolgabbro 110m 87127E: 111.00m

120m

130m

132.20-135.40m: Cherty breccia highly altered/oxidised

140m

E.O.H: 149.35m 150m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 88034 SE 354N 1160W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =136.10m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-8.05m: Overbudden po py As Sl Cp

Visible Gold

Albitisation 8.05-26.50m: Mafic gabbroic rock Massive, compact + biotite matrice 10m 10.30-26.50m: gabroic-dioritic rock. Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation

Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, 88034A: 18.50m Cpy = Chalcopyrite, Cb= 19.40m: thin vein filled with Qz+Cp parallel to CA Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock 26.50-29.20m: Graphitic silt Diffused contacts 29.20-53.00m: Mafic volcanic rock probably basaltic. Cherty breccia 30m Greyish massive. Graphitic silt-shale

Mafic volcanic rock

40m

50m

53.00-86.70m: Mafic gabbroic rock Diffused contact

60m

63.50-64.80m: Albite(?)+carb+Qz+magnetite thin spines <5cm vein parallel to CA 88034E: 64.80m

70m

77.80-84.90m: Chl-Biot gabbro Thin quartz veined (1mm-cm)

80m

84.90-86.70m: Biotite gabbro Chert clasts

86.70-93.20m: Mafic volcanosedimentary probably tuffite

90m

93.20-105.30m: Chert Conatin graphitic silt inclusions.

100 m

105.30-111.00m: Cherty tuffite

110m

111.00-118.45m: Graphitic silt

118.45-122.35m: Cherty tuffite 120m

122.35-126.00m: Graphitic tuffite

126.00-132.55m: Graphitic silt

130m

132.55-136.20m: Graphitic tuffite

EOH: 136.10m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 88057 SE 501N 1214W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =160.75m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-9.30m: Overbudden po py As Sl Cp

Visible Gold

Albitisation

9.30-10.55m: Dark massive mafic volacnosedimentary (?)-volcanic(?) rock 10m Carbonate veined Carbonitization biotite silicification 10.55-14.25m: Intermediate-felsic volcanosedimentary rock, probably albite-felsite. (chert) Banded 88057A: 11.65m Magnetite Scapolitisation Chloritisation

14.25-101.85m: Mafic grabbroic rock, variation of composition between amphibolgabbro-hornblendite Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

Intermediate volcano sedimentary 30m

Graphitic silt-shale

40m

50m

60m

88057H: 66.20m

62 70m

71.10-73.60m: weakly foliated 73.60-92.75m: carbonate veined

80m

90m

100 m

101.85-107.90m: Mafic volcanosedimentary, probably tuffite. More grey-bluish color, banded.

107.90-114.90m: Graphitic silt-shale. 110m

114.90-117.15m: Mafic volcanosedimentary, probably tuffite.

117.15-121.00m: Graphitic silt-shale. Foliated 120m

121.00-122.20m: Mafic volcanosedimentary, probably tuffite. 122.20-123.90m: Graphitic silt-shale. Carbonate-albite veined 123.90-126.70m: Mafic volcanosedimentary, probably tuffite.

126.70-130.50m: Graphitic silt-shale.

130m 130.50-133.45m: Mafic volcanosedimentary, probably tuffite. 130.50-140.55m: Carbonate brecciated tuffite.

132.50-133.45m: Graphitic.

140m

142.40-143.75m: Weakly foliated 50° to CA graphit band. 88057Nb: 142.40m

88057O: 146.20m

150m 63

158.40-158.80m: graphitic inclusion foliated 160m

E.O.H: 160.75m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -55˚ 85115 SE 450N 1300W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =248,29m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-6.30m: Overbudden po py As Sl Cp

Visible Gold

6.30-45.70m: Mafic volcanic rock Greyish massive rock. Possibly mafic volcanosedimentary-volcanite rocks succession. Albitisation

10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation

Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

30m

Graphitic silt-shale

33.27-34.13m: shear zone 50° to CA Mafic-intermediate volcanic rock

39.55-41.58m: graffitic bands 40m

45.70-102.40m: Mafic gabbroic rock, probably hornblendite

50m

51.70-57.50m: Quartz-Albite veined

60m

64.30m: 85115F

64 70m

74.30m: 85115G

80m

90m Impregnated sulphides in quartz-albite vein and associated with quartz 91.20-107.40m: succession of gabbroic-fine grained texture

100 m

107.40-115.50m: Mafic volcanic rock

110m

115.50-144.20m: Mafic volcanosedimentary, probably tuffite. Tuffite with ductile deformed graphitic inclusions and graphitic bands. 115.50-119.32m: few carbonate veins/patches

120m

130m

133.20-140.80m: Graphitic layers/bands sub perpendicular to CA more or less altered and fragmented. Thin "line" of Alb(?) between layers

140m

144.20-152.37m: Graphitic silt-shale 145.50m: 85115J

150m 65

152.37-163.77m: Mafic volcanosedimentary rock, probably tuffite

156.00-159.00m: "Zebrazone" (biotite/carb) brecciated structur.

159.00-162.30m: weakly deformed and ductile deformation figures. 160m

163.77-177.30m: Mafic volcanic rock

170m

173.70-177.30m: Py associated with alb, Qz and carb.

177.30-186.92m: Mafic gabbroic rock, probably hornblendite

180m Cp associated with Alb+Qz+Carb+Chl

186.92-248.29m: Mafic-intermediate volcanic rock 192.00-199.00m: Volcanoclastic texture 190m

200m

210m

212.05m: 85115M

218.20m: 85115N

220m

230m

232.30-242.20m: possibly more volcanosedimentary, tuffite (?)

66 240m

245.20m: 85115O

E.O.H: 248.29m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 88093 S 600N 1600W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =162.80m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-16.10m: Overbudden po py As Sl Cp

Visible Gold

Albitisation

10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation

16.10-18.55m: Mafic volcanosedimentary, probaby tuffite. Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= 18.55-20.90m: Altered graphitic shale Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m Peperitic texture , Phl=phlogopite, tlc=talc 20.90-31.00m: Chert Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

Intermediate volcano sedimentary 30m

31.00-75.40m: Mafic vocanosedimentary, probably tuffite. Graphitic silt-shale 31.00-39.05m: Highly altered Chert

88093D: 36.20m

40m

44.00-75.40m: weakly to moderate sheared 60-90° to CA

50m

51.00-52.00m: scapolites are deformed

60m

70m

75.40-76.70m: Graphitic silt-shale 76.70-162.80m: Andesitic-intermediate volcanosedimentary rock. Massive grey blueish

80m

81.10-81.40m: Graphitic shale

90m

100 m

108.70-108.90m: Strongly oxidized+albite vein 110m

117.80-117.95m: Quartz-carb-Alb-Ch vein with a net contact 60° to CA and a diffused second contact 118.15-118.65m: euhedral white-grey altered mineral(?) 120m

130m

140m

143.40-162.80m: trace of sulphides filling cracks

150m

160m

E.O.H: 162.80m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 88218 S 700N 1900W Starting date = Completion date = Core diameter = 46 mm Length (EHO) =130.15m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00-7.50m: Overbudden po py As Sl Cp

Visible Gold

7.50-97.05: Mafic grabroic rock, green, massive. Albitisation

10m Carbonitization biotite silicification (chert)

Magnetite Scapolitisation Chloritisation

Abbreviations Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Cb= 19.45-19.75m: Shear zone Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m , Phl=phlogopite, tlc=talc

Overburden

Mafic volcano-sedimentary rock

Mafic gabbroic rock

Intermediate volcano sedimentary 30m

32.65-33.60m: Black graphitic silt(?). Red color quartz veined. Diffused contact. 33.30m: 88218A

40m

50m 50.40m: 88218B

55.45m: 88218C

58.40m: 88218D 60m

Small variations of grain size 69 70m

80m

90m

97.05-126.50m: Intermediate felsic volcanosedimentary, probably albite-felsite. Massive, contact not preserved 100 m

110m At 110.70m: 1cm semi massive Py. 10cm cherty

116.35-117.35m: banded 118.80-118.95m: semi massive Py. 118.70-119.20m: darker matrix (graphitic?more basic?) 120m

122.45m: 88218I 122.35-123.50: Alteration dolomite-caronate, weakly reactive to acid. Whiter and more friable. Some foliation and preserved bands. 123.50-128.80m: Probably tuffitic sediment, bandings parallel to CA

126.50-128.80m: mafic volcanosedimentary, probably tuffite

128.80-130.15m: Graphitic silt-shale Diffused altered contact. Tectonised with 70° to CA bands 130m E.O.H: 130.15m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -˚ 88219 S Starting date = Completion date = Core diameter = 76 mm Length (EHO) =168,3m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Edited from Log Jan Ehrenborg 2013 Legends 0 m 0.00-8.50m: Overbudden General comments to PAH88219: A first glance at PAH88219 indicate that it is a "copy" of PAH88209 meaning that the same po py As Sl Cp lithologic units, deformations and alterations will be found in the same order in both drill cores, eventually with approximately the same thicknesses. Interpretations for the first hole logged, PAH88219, will thus most likely be more or less the same for PAH88209. Distorted= slightly/weakly deformed rock, through minor normal faults, very weak folding often together with/and along the Visible Gold normal faults + leuco-schlieren.

Albitisation

8.50-27.50m : Mafic volcano-sedimentary rock, probably mafic-intermediate tuffite 10m Grey, eg-porphyroblastic, layered= laminated-banded.The tuffite is in general weakly magnetic and thin-mt-laminae occur Carbonitization biotite silicification (frequently?). Mt-enrichment occur locally= rather strongly magnetic. Lamination=0-15 degrees to core. Porphyroblastic bands = (chert) recrystallized layering = scp or alb. Some bands scp-bt-altered. Several very small scale (displacement mm-cm) normal faults. 19.40-23.20m: Green, laminated-distorted, mafic tuffite. Lamination= 0-30 degrees to core. Carbonate (=dol?)-schlieren-veins Magnetite Scapolitisation Chloritisation located in accordance to the somewhat stronger deformation than in the tuffite above. Extremely weakly (min-lineation NOT foliation-planes). 23.20-25.10m: Grey,porphyroblastic, layered= laminated-banded. Lamination=0-15 degrees to core. The small-scale normal fault Abbreviations deformation more rare. Py = Pyrite, Po = Pyrrhotite, Sl = Sphalerite, 25.10-25.80m: laminated-distorted. Lamination= generally 0-15 degrees to core but the tuffite is rather plastically distorted (caotic) Cpy = Chalcopyrite, Cb= with small-scale overturned folds (without ax-pl-foliation) why angle to core varies a great deal. A large amount of carbonate Carbonate,dol=dolomite,Ab=albite,scp=scapolite 20m (=dol?)-schlieren-veins located in accordance to the somewhat stronger deformation than in the tuffite above. , Phl=phlogopite, tlc=talc 25.80-26.20m: laminated with broken up 5-10mm thick bands of mt. This sequence is strongly carbonate (dol?) brecciated. Rock= mafic tuffite breccia with dol-matrix. Lower contact= 18 degrees to core= follows tuffite-layering. Overburden 26.20-26.60m: Carbonate rock (soft + no respons on acid = dol?) richly spotted by mafic minerals + mt (probably from the wall rock mafic tuffite + mt). Lower contact= 22 degrees to core= follows underlying tuffite layering. Mafic volcano-sedimentary rock 26,60-26,70m: Dark grey, laminated. Lamination= 22 degrees to core parallell with the upper contact. Cut by underlying ab-fels- alteration in tuffite. Mafic gabbroic rock 26.70-27.50m: Ab-fels-altered tuffite. greyish red, laminated. Upper irreegularcontact, sharp and at approx 60 degrees to core. This interval holds irregular fractures at 45-70 degrees to core filled with mafic mineral (perhaps related to the mafic-gabbroic body below). These mafic fractures are sometimes developed to small irregular in-situ-breccia-bands. Intermediate volcano sedimentary 30m 27.50-106.30m: Mafic-gabbroic rock 27.50-28.60m: Scp-bt-altered mafic-gabbroic-rock . Reddish spotted towards upper contact (=the ab-felsite-alt from the ab-fels- tuffite interval above?). Weakly foliated/min-lineated. Few small carbonate (dol?)-veins-schlieren. Phl in dol along vein borders. Lower contact cut irregularily + sharply by underlying carbonate rock(soft + no respons on acid = dol?). 29.20-32.50m: Dark grey, foliated-mineral lineated, scp-bt-altered, Rich in carbonate-ab-fels-schlieren, often sub parallell with foliation-mineral lineation. Locally rather magnetic= mt. Trace of py + cpy in cb-ab-schlieren. Foliation= 57 degrees to core.

32.50-36.75m: Bt-scp-alt rock , rather much cb-schlieren with py-trace. Weak foliation-mineral lineation= 40-50 degrees to core. 36.75-41.20m: Dark brownish-greenish-grey, vf, porphyroblastic, massive, amp-bt-scp-altered . Dark vf bt-groundmass rich in <1mm big scp-porphyroblasts + amp, + up to 1cm big amp-megacrystals. Sparsely occurring carbonate-schlieren. 41.20-42.00m: Dark brownish-greenish-grey, vf, porphyroblastic, weakly foliated-mineral lineated, amp-bt-scp-altered . Dark vf bt- 40m groundmass rich in <1mm big scp-porphyroblasts + amp, + up to 1cm big amp-megacrystals. Carbonate-schlieren with some py and trace of cp. 42.00-43.60m: Bt-scp-amp-tlc-chl-rock, semi-massiv , cb-schlieren with py + cp-trace. 43.60-44.70m: Crushed somewhat clay-altered semi-massive st-scp-amp-chl-altered. 44.70-51.30m: Semi-massive st-scp-amp-altered. Red spots from weak ab-alt.

50m 51.30-88.30m: Dark grey semi-massive . Bt-scp-amp-(chl)-altered, cb-schlieren with some py + cp-trace. Weakly magnetic.

60m

71 70m

80m

88.30-90.60m: Dark green, massive, amp-gabbro , weakly bt-scp-(chl)-alt. In general it shows a rather well preserved gabbroic texture (massive, cmg) , few cb(=dol?)-schlieren with py + cp-trace, magnetic. 90m

90.60-91.75mDark greenish grey, vy, ug, foliated-mineral lineated, mafic-gabbroic rock . Bt-scp-amp-(chl)-altered, cb-schlieren. Some py + cp-trace. Weakly magnetic. 91.75-93.15m: Dark green, massive, amp-gabbro , weakly bt-scp-(chl)-alt. In general it shows a rather well preserved gabbroic texture (massive, cmg) , few thin cb(=dol?)-schlieren with py + cp-trace, weakly magnetic. 93.15-95.15m: Dark greenish grey, vy, ug, mineral lineated, mafic-gabbroic rock . Bt-scp-amp-(chl)-altered, cb-schlieren-veins with phl-along vein borders + py + cp-trace. Weakly magnetic. 95.15-106.38m: Dark greenish grey, vy, ug, foliated (75 degrees to core), mafic-gabbroic rock . Bt-scp-amp-(chl)-altered, cb-schlieren- veins with py + cp-trace. Weakly magnetic. 88219A: 97.50m; 88219B: 96.00m 100 m

88218C: 106.10m 106.38-111.50m: Intermediate Volcanosedimentary, probably felsite, broken reddish, banded-laminated . Banding-lamination (40- 60 degrees to core) indicate possible ab-altered tuffite. Some fractures and small in-situ-breccias with trace of cp + py. 88218D: 108.30m 110m

111.50-128.30m: Mafic-gabbroic rock 111.50-114.50m: Dark grey, vf-fg, eg, foliated-mineral lineated , bt-scp(-amp)-altered mafic-gabbroic rock. Few, thin ab-cb-veins with trace of py + cp.

114.50-115.65m: Yellowish carbonate (=dol?)-vein, with ab-patches, sub-mm-thin bands of py and other bands of mt, patches rich in py-crystals, some cp.

120m

115.65-124.65m: Dark grey, vy, ug, foliated (75 degrees to core), mafic-gabbroic rock . Bt-scp-amp-(chl)-altered, cb-schlieren-veins with py + cp-trace, some mt-blobs. Weakly magnetic.

88218E: 127.05m 124.65-128.30m: Dark grey, vy, ug, foliated (75 degrees to core) - semi massive (=foliation more diffuse), mafic-gabbroic rock . Bt- scp-amp-(chl)-altered. Rather rich in cb-ab-fels-schlieren-veins with py + cp-trace, some mt-blobs. Weakly magnetic. 128.30-168.30m: Intermediate Volcanosedimentary, probably felsite. 128.30-139.00m: Whitish yellow, semi-massive, cb(dol?)-fels with patches of ab-fels + minor patches + veins of qz. Stockwork 130m (defined by 1.patches + veins of vein-qz, 2.cp + py - mineralized fractures, and 3.Very local small parts with ore-breccia). Both cp and py occur throughout this interval in neither rich or very poor amounts. The best cp-section in this interval is 134,18-135,22

139.00-140.65m: Grey, laminated-banded (70 degrees to core) ab-felsitic tuffite . Fractures and few small in-situ-breccias with cp+py. 140m 140.65-141.00m: Ab-chl-felsic tuffite . Weak stockwork of cp+py-fractures/diffuse fracture network. 141.00-141.85m: Brownish grey laminated-banded (65-70 degrees to core), ab-scp-bt-altered tuffite. Few cp+py-fractures. 141.85-142.30m: Cp-ore-stockwork-breccia , fragments= ab-alt-tuffite , matrix= cp+py-mineralization. 142.30-144.80m: Light greenish red, vf, eg, diffusely laminated-banded, ab-chl-altered, tuffite . Some parts wih cp+py fracture-fillings + impregnations. 144.80-149.00m: Light reddish grey, vf, eg, laminated-banded, ab-altered tuffite . Very poor in fractures, thin bands and patches with cp + py.

150m ? 149.00-157.25m: Reddish greenish grey, vf, eg, laminated-banded, weakly ab-altered tuffite. Weak stockwork with fractures, thin bands and patches with cp + py. Chl-alteration + amount cp+py increases from interval 146,00-149,00m to 149,00-153,45m to 153,45- 17,25m. Lower contact is an alteration contact. It is sharp because the chl-alt ends here.

157.25-157.55m: Bleached, greyish, vf, eg, laminated-banded, tuffite . Banding towards lower contact = caotic. Not ab-altered because it can be scratched with a knife. 157.55-157.70m: Broken-crushed, black, vf, eg, laminated, black shale . Sub-mm-thin qz-veinlets showing very72 small scale folding. 157.70-159.10m: Greenish grey, vf, eg, laminated-banded , locally weakly ab-altered tuffite. Weakly chl-altered and a 10 cm-thick band with scp-bt-alteration. Some schlieren/patches/fractures with cp+py. 160m 159.10-162.05m: Brown, vf-fg, eg, banded-laminated, bt-rich-tuffite (bt-bands thick and semi-massive). Weak scp-alteration, few weakly ab-altered bands, some py + trace of cp. Bleached, light grey, vf, eg, banded-laminated, tuffite . Weakly ab-altered, some cp + py. 162.05-162.40m: Broken-crushed, black, vf, eg, laminated, black shale. Sub-mm-thin qz/ab-felsite-vein/veinlets showing very small scale folding (mm-amplitudes). 162.40-163.40m: Brownish grey, vf, eg, laminated-banded (75 degrees to core), weakly ab-scp-bt-altered tuffite. Some cp + py. 163.40-168.30m: Greenish, vf, eg, banded-laminated, tuffite . Bt-amp-scp-altered, thin cb-bands with py+ cp-trace. Band (75-80 degrees to core) with mt in interval 165,85-166,28m. This band shows very nice load cast structures with right way up (=towards E.O.H: 168.30m

Location Hole ID Zone Northing Easting Azimuth = ˚ Dip = -60˚ 88221 S 625 N 1750 W Starting date = Completion date = Core diameter = 46mm Length (EHO) =75.50m Grain size Alteration Sulphide (%)

Depth Rock unit Fine Medium Coarse Weak Moderate Strong 2 4 6 8 Description Legends 0 m 0.00 – 13.00 m : Overburden po py As Sl Cpy

Visible Gold

10m Carbonitization biotite silicification (chert)

13.00-44.90m: Felsic-Intermediate volcanic rock (Felsite), probably volcano-sedimentary Tourmaline Scapolitisation Chloritisation Massive fine grained grey-white rock. 14.55-24.60: banded 45° to CA Weakly deformed Abbreviations carbonate and Py are usually associated in cracks As = Arsenopyrite, Py = Pyrite, Po = Sulphides occcur as veintlets, patches and filling cracks Pyrrhotite, Sl = Sphalerite, Cpy = Chalcopyrite, Gl= galena Plf = Phyllosilicate lined fractures 20m

Overburden

Intermediate Volcanic rock 88221A: 25.80m Graphitic silt 27,05-28,50m : Bands 50° to CA

88221B: 29.50m 30m

33.60-37.80m: Brown carbonate possibly ferro-dolomite.

39.10-44.80m: bands 50-60° to CA 40m

88221C: 43.00m

44.80-47,60m: Graphitic silt Massive, very fine grained and no schistosity.

47.60-48.60m: Felsic-Intermediate volcanic rock (Felsite), probably volcano-sedimentary Bands 70° to CA 48.60-49.70m: Graphitic silt, with some carbonate in cracks. 50m 49.70-55.00m: Felsic-Intermediate volcanic rock (Felsite), probably volcano-sedimentary 88221E: 51.50m 49.70-51.30m: bands 60° to CA

55.00-55.60m: Graphitic silt 55.60-71.40m: Felsic-Intermediate volcanic rock (Felsite), probably volcano-sedimentary

60m

70m

71.40-72.40m: Graphitic silt 72.40-75.50m: Felsic-Intermediate volcanic rock (Felsite), probably volcano-sedimentary bands 40° to CA

E.O.H: 75.50m

98,5

100,1

98,51

99,16

98,69

99,86

98,53

99,12

99,58

99,29

98,89

99,61

98,56

98,49

99,59

99,82

100,1

100,3

100,05

Total

ME-XRF06

2,4

3,2

0,9

3,76

5,28

2,77

8,79

2,45

15,3

4,48

1,25

5,14

2,76

1,93

1,13

2,43

0,66

2,06

18,35

LOI

ME-XRF06

0,13

0,04

0,02

0,04

0,02

0,01

0,03

0,01

0,03

0,02

0,08

0,01

0,02

<0.01

BaO

ME-XRF06

0,01

0,03

0,01

0,02

0,01

<0.01

SrO

ME-XRF06

0,18

0,06

0,05

0,06

0,037

0,005

0,058

0,131

0,063

0,097

0,045

0,035

0,078

0,061

0,052

0,061

0,066

0,075

<0.001

P2O5

ME-XRF06

0,1

0,23

0,08

0,03

0,09

0,12

0,18

0,04

0,01

0,18

0,29

0,42

0,24

0,23

0,07

0,43

0,25

0,31

MnO

ME-XRF06

1,66

0,74

1,07

0,75

0,78

0,95

0,92

0,88

0,71

0,66

0,94

1,06

0,64

0,81

0,67

1,01

TiO2

ME-XRF06

0,02

0,04

0,01

0,03

0,01

0,02

0,01

0,02

0,04

0,02

0,03

0,02

0,04

0,06

0,04

Cr2O3

ME-XRF06

1,6

0,31

2,71

5,91

3,31

4,47

2,41

1,24

2,15

0,69

1,84

1,89

0,59

0,47

2,79

0,61

0,64

1,06

K2O

ME-XRF06

2,5

2,7

1,03

1,78

1,42

6,21

3,72

2,35

3,16

3,49

2,47

3,88

3,32

1,89

2,23

2,13

4,76

1,67

3,28

Na2O

ME-XRF06

2,8

6,8

8,07

9,99

1,24

7,78

8,25

8,29

7,17

3,71

0,89

10,1

2,26

9,56

7,77

3,62

6,62

7,73

8,27

MgO

ME-XRF06

4,7

4,21

3,26

2,91

5,96

6,16

4,47

8,72

10,8

2,91

3,87

9,45

4,18

3,03

10,1

9,03

5,47

10,85

24,75

CaO

ME-XRF06

2,6

9,54

2,97

8,36

6,65

13,8

6,37

17,49

16,38

11,91

17,47

13,32

11,74

15,15

12,69

15,45

14,03

13,45

Fe2O3

ME-XRF06

17,1

9,05

13,5

9,22

15,1

14,01

12,13

13,52

13,83

13,85

12,89

11,59

14,29

14,36

15,03

12,53

14,08

14,02

Al2O3

ME-XRF06

49,14

44,97

60,98

43,38

44,07

45,76

63,05

73,79

44,52

47,33

33,32

45,66

51,09

66,72

47,21

51,83

SiO2

ME-XRF06

0,4

0,5

0,6

0,5

0,7

0,5

0,1

0,95

0,65

0,45

0,95

0,15

0,11

length

72,4

66,7

47,5

23,7

64,8

37,2

26,8

18,2

30,9

160,3

119,8

36,45

11,65

124,7

107,9

146,4

147,7

112,8

66,3

23,2

64,3

26,1

17,7

159,9

35,85

124,2

36,25

146,3

147,6

112,7

59,85

30,79

118,85

107,45

From

WR88057P

WR88057L

WR88057I

WR88057H

WR88057E

WR88057C

WR88057B

WR88057A

WR88034G

WR88034F

WR88034E

WR88034C

WR88034B

WR88034A

WR85115E

WR85115D

WR85115C

WR85115B

WR85115A

DESCRIPTION

SAMPLE

PO :NUMBER

CERTIFICATE COMMENTS : Project: Kiruna Iron: Pahtohavare. : COMMENTS Project:Pahtohavare. Iron: Kiruna CERTIFICATE

PROJECT : Pahtohavare PROJECT

DATE RECEIVED : 2013-04-22 DATE FINALIZED : 2013-05-04 FINALIZED DATE :RECEIVED DATE 2013-04-22

# of Samples # of : 19 CLIENT : NORIIK - Kiruna Iron AB Iron - Kiruna : NORIIK CLIENT PI13072878 - Finalized PI13072878 74

Core 88057

DEPTH m AL203 % FE203 % MNO % TI02 % MGO % CAO % K20 % NA20 % P205 % BA ppm CO ppm CR ppm CU ppm 10.55-14.25 10,40 10,80 0,21 0,66 6,17 8,30 2,07 3,53 0,06 115 103 70 18175 14.25-16.15 13,10 12,60 0,10 0,64 7,31 4,34 5,53 1,39 0,06 257 51 155 222 33.50-38.45 13,70 14,70 0,10 0,72 7,18 5,20 4,87 2,81 0,06 259 61 224 1555 38.45-42.15 6,45 14,80 0,30 0,38 7,09 14,00 1,25 2,10 0,08 56 144 104 23176 42.15-47.20 12,50 10,80 0,15 0,58 6,31 8,56 3,33 3,46 0,06 139 41 183 1998 47.20-51.35 13,30 10,70 0,12 0,51 6,52 6,54 3,59 3,43 0,06 147 44 162 1745 51.35-56.90 14,60 10,80 0,10 0,62 6,50 5,51 4,46 3,94 0,05 188 41 149 691 56.90-60.65 12,40 11,50 0,12 0,70 7,15 5,98 4,78 2,94 0,06 188 36 161 700 60.65-62.20 2,63 31,50 0,28 0,15 5,39 11,20 0,56 0,90 0,10 27 272 40 63248 62.20-63.40 12,70 11,40 0,15 0,64 6,57 7,63 4,27 3,51 0,06 171 38 126 1328 63.40-65.75 13,70 12,70 0,08 0,11 6,91 4,63 5,94 2,98 0,06 240 42 201 220 65.75-67.15 11,90 11,20 0,07 0,40 1,70 5,41 1,23 4,13 0,04 61 207 85 10054 67.15-71.10 13,90 11,70 0,09 0,67 6,31 5,09 5,49 2,89 0,05 254 34 199 756 92.75-96.70 15,00 10,90 0,11 0,64 6,49 5,48 5,36 2,88 0,06 242 28 143 1397 117.10-121.00 12,10 10,90 0,11 0,51 2,89 3,19 3,57 1,66 0,04 792 62 126 1125 126.70-130.50 10,70 14,80 0,22 0,51 3,03 7,47 3,61 0,95 0,05 336 124 147 3960

Core 85115

DEPTH m NA20 MGO % AL203 % SI02 % P205 % S % K20 % CAO % TI02 % V ppm CR ppm MNO % FE203 % CO ppm NI ppm CU ppm 34.15-39.55 2,6169 7,4852 13,8299 49,3473 0,0893 0,4288 1,4334 8,1524 1,0173 0,0275 0,0292 0,3634 16,579 0,0173 0,011 285 90.65-91.20 3,6476 8,2576 13,4335 48,6487 0,4436 1,355 0,3274 10,4454 0,7062 0,0231 0,0251 0,1729 13,7233 0,0207 0,0527 1869 173.70-177.30 2,0008 7,5806 11,5927 46,0853 0,118 2,1349 2,8756 8,9368 1,5226 0,0328 0,0121 0,1783 17,8106 0,0237 0,0219 1293 192-194.75 4,6479 7,1592 12,389 51,7918 0,097 1,3956 2,2416 4,8657 1,0375 0,029 0,0121 0,1 15,4434 0,0263 0,0104 541 206.20-209.25 2,9686 9,1206 12,7289 53,3968 0,0941 0,3865 2,7717 5,4947 1,1322 0,031 0,016 0,1086 13,2331 0,0145 0,0118 1331 209.25-212.65 3,2435 8,8082 11,492 45,8021 0,1079 2,0388 2,6052 5,8189 0,909 0,0229 0,0204 0,1571 15,9351 0,0432 0,0112 185

Core 88034

Depth m AL203 % FE203 % MNO % TI02 % MGO % CAO % K20 % NA20 % P205 % AS ppm BA ppm BE ppm CO ppm CR ppm CU ppm 5540-5780 14,7 13,2 0,214 0,692 7,05 8,47 1,22 3,17 1,68 4,6 132 0,09 43 205 496 8670-8740 12,2 12,4 0,12 0,664 7,51 5,32 5,82 1,76 1,45 4,9 323 0,1 42 193 2428 9005-9310 14,8 9,83 0,084 0,752 3,46 4,92 2,37 5,79 0,841 4,6 133 0,09 61 227 2579 9310-9650 18,1 6,55 0,039 0,746 1,16 2,34 1,06 8,6 0,671 4,6 90 0,92 18 167 2089 9650-9900 18,6 5,66 0,036 0,692 0,373 1,94 0,737 9,12 0,53 12 96 2 12 198 2187 9900-9970 11,7 24,1 0,031 0,633 0,415 1,08 0,297 6,11 0,684 0,684 8,3 0,1 110 559 27300 9970-10280 16,3 13,2 0,036 0,682 0,427 3,31 0,851 7,11 0,733 4,6 74 3 68 304 5344 10280-10550 13,6 4,02 0,011 0,087 0,417 3,66 1,05 5,25 0,41 4,6 75 2,5 78 59 2268 10550-11100 14 3,93 0,027 0,218 2,76 3,71 2,51 3,82 1,02 4,8 174 1,4 35 156 562 11100-11550 9,85 9,69 0,025 0,08 1,57 3,49 1,47 2,61 1,05 4,7 105 0,09 182 54 3417 11550-11845 10,9 14,2 0,028 0,129 2,46 2,39 2,9 2,22 1,19 4,8 255 0,1 281 104 5237 11845-12150 12,2 7,4 0,086 0,416 4,65 6,34 3,51 1,95 0,85 4,8 524 0,1 52 447 305 12150- 12235 13 14,1 0,072 0,246 5,09 7,1 2,81 2,31 1,24 4,7 223 0,09 159 253 29208 12235-12590 13,5 4,42 0,037 0,256 3,01 2,38 3,89 2,14 0,627 4,7 448 0,49 31 142 232 12590-12970 11,6 6,79 0,046 0,366 3 2,47 3,31 1,85 0,745 5 283 0,1 55 197 515 12970-13255 11,3 9,54 0,055 0,366 3,17 2,57 3,08 1,93 0,942 4,9 313 0,1 73 156 691

Core 87119

Depth m AL203 % FE203 % MNO % TI02 % MGO % CAO % K20 % NA20 % BA ppm CU ppm 25.85-30 .70 13,2 17,8 0,084 1,01 6,9 3,15 1,77 3,2 147 80 30.70-34.35 12,3 21,7 0,067 1,12 6,04 2,16 1,14 4,29 71 20 34.35-38.00 11,9 21,3 0,074 1,08 6,43 2,99 2,4 3,86 107 19 38 .00 -42.95 9,79 21,8 0,057 0,68 8 0,675 1,69 2 75 17 42.95-46.60 13 35 0,105 0,857 9 3,88 1,23 3,88 110 495 46.60 -49.05 14,7 11,3 0,123 0,886 9,85 2,24 2,12 3,99 198 248 89 .80 -92 .80 14,7 11 0,091 0,982 10,3 0,623 2,23 0,855 186 265 118 .60 -122.00 14,5 10,1 0,044 0,695 6,08 0,37 2,07 3,89 220 613 122.00-124.67 14,9 7,16 0,024 0,625 3,86 0,33 2,34 4,46 281 428

Core 87104

Depth m NA20 % MGO % AL203 % SI02 % S % K20 % CAO % TI02 % MNO % FE203 % CU ppm 3.20-7.32 1,8781 16,9002 15,2333 49,0511 0,2573 0,7731 1,4362 1,0348 0,1311 14,4856 568 7.32-9.47 1,6702 18,5047 14,8294 47,4292 0,8152 0,6417 1,123 0,9242 0,1382 14,8135 672 9.47-12.29 1,5751 18,9335 14,6635 47,8426 0,9126 0,2952 1,1192 0,8818 0,1362 14,3473 809 12.29-15.36 2,0393 17,974 15,0718 47,5877 0,7047 0,5909 1,3968 0,9191 0,1452 15,4795 394 15.36-18.38 1,0586 19,3612 14,0902 44,1626 0,7687 1,9905 1,7331 0,9637 0,1489 16,7683 266 171.70-176.55 3,4883 7,898 12,2257 49,0617 0,1979 0,8589 7,2051 1,953 0,1888 17,6296 553 176.55-179.10 2,5961 7,9881 11,6607 47,0409 0,2788 1,7447 9,7031 1,9401 0,198 17,0063 2084 184.20-187.20 2,9673 7,3174 12,6622 49,6515 0,1445 1,2336 8,3796 1,6412 0,2007 16,4299 454 194.20-198.65 1,2559 11,1067 13,7066 47,0102 0,1347 3,1767 5,4274 1,0972 0,1355 17,4566 1095 198.65-202.60 0,7462 11,3476 11,2871 44,0623 1,5181 1,9372 3,75 1,6121 0,1279 23,3424 14519 202.60-205.85 0,4795 15,3144 14,2451 43,8233 0,4081 2,1316 3,0457 1,2249 0,1357 19,75 4579 205.85-209.60 2,0439 7,9736 10,4858 39,5442 0,5663 0,7243 14,7985 1,5474 0,2189 14,638 3911 209.60-212.25 2,3679 9,1831 9,5617 35,5719 1,6477 0,553 19,3851 1,4372 0,3353 18,3331 15517 212.25-216.10 1,5184 10,9792 13,1136 49,4102 0,2359 1,3055 4,7052 2,1035 0,1184 17,363 1112 216.10-219.15 1,0968 11,9886 12,8207 48,5984 0,2101 1,1966 4,6009 2,061 0,119 18,1035 1312

Core 85108

Depth m NA20 % MGO % AL203 % SI02 % P205 % S % K20 % CAO % TI02 % MNO % FE203 % CU ppm 99.65-103.95 1,4897 4,2183 10,6106 48,799 0,126 5,1519 2,3899 10,3769 0,8136 0,6046 14,2151 21758 187.50-191.30 0,4142 7,1697 12,445 45,8133 0,1223 1,6757 4,2367 2,9954 1,244 0,3387 24,9079 4797

Core 84004

Depth m NA20 % MGO % AL203 % SI02 % P205 % S % K20 % CAO % TI02 % MNO % FE203 % CU ppm 77.70-79.10 0,5126 5,5366 8,0713 34,4249 0,1482 5,1892 1,6346 15,9193 0,4376 0,5564 28,8053 3272 153.50-154.50 1,9674 3,8541 7,0327 29,2251 0,1108 11,4246 0,4607 10,6083 0,6142 0,2337 36,6624 5506

BIOTITE ANALYSES

Zone SOUTH EAST Sample 88209F PHL 88219C CHL 88219B BIOT 88218D2CHL BIOT88218I MBIOT88218C BIOT 88093D BIOT 88221A BIOT 84004Mbiot 84004Fbiot 85108F BIOT No. 55 57 59 101 104 106 110 118 1 8 50 Na2O 0,159 0,171 0,165 0,113 0,074 0,136 0,09 0,15 0,141 0,163 0,217 FeO 15,272 14,184 16,559 19,816 17,017 20,184 19,071 15,342 22,426 19,706 23,996 Cr2O3 0,092 0 0,052 0 0,022 0,027 0,018 0,087 0,028 0 0,021 Cl 0,628 0,523 0,784 0,681 0,243 0,624 0,655 0,568 0,49 0,467 0,603 MgO 15,729 17,783 13,43 12,834 17,987 13,102 12,885 14,333 9,576 11,136 8,134 MnO 0,04 0,057 0,006 0,129 0,036 0,096 0,039 0,066 0,223 0,576 0,202 K2O 10,229 7,506 10,527 8,883 5,717 8,441 9,996 10,681 9,708 9,8 8,965 Al2O3 13,86 15,03 14,886 15,04 15,303 15,147 14,407 16,938 16,593 16,639 16,337 NiO 0,007 0,067 0,109 0,007 0,06 0,01 0,062 0,039 0,005 0 0,059 CaO 0 0,05 0,028 0,058 0,126 0,025 0 0,01 0 0,021 0 SiO2 37,734 35,44 36,601 36,079 36,599 35,529 36,874 37,036 35,617 36,07 34,7 TiO2 1,944 0,357 2,661 1,589 0,936 1,534 1,797 1,594 1,809 1,304 1,636 Total 95,552 91,05 95,631 95,075 94,065 94,714 95,746 96,716 96,505 95,777 94,734

Number of cations on the basis of 11O Si 2,844 2,757 2,789 2,779 2,746 2,748 2,825 2,758 2,742 2,765 2,745 Al 1,231 1,378 1,337 1,366 1,353 1,381 1,301 1,486 1,506 1,503 1,523 Ti 0,110 0,021 0,153 0,092 0,053 0,089 0,104 0,089 0,105 0,075 0,097 Cr 0,005 0,000 0,003 0,000 0,001 0,002 0,001 0,005 0,105 0,000 0,001 Mg 1,767 2,062 1,526 1,474 2,012 1,511 1,471 1,591 1,099 1,272 0,959 Fe2+ 0,963 0,923 1,055 1,277 1,068 1,306 1,222 0,955 1,444 1,263 1,587 Mn 0,003 0,004 0,000 0,008 0,002 0,006 0,003 0,004 0,015 0,037 0,014 Ni 0,000 0,004 0,007 0,000 0,004 0,001 0,004 0,002 0,000 0,000 0,004 Na 0,023 0,026 0,024 0,017 0,011 0,020 0,013 0,022 0,021 0,024 0,033 K 0,984 0,745 1,023 0,873 0,547 0,833 0,977 1,015 0,954 0,958 0,905 Ca 0,000 0,004 0,002 0,005 0,000 0,002 0,000 0,001 0,000 0,002 0,000 Cl 0,002 0,069 0,101 0,089 0,031 0,082 0,085 0,072 0,064 0,061 0,081 OH 1,998 1,931 1,899 1,911 1,969 1,918 1,915 1,928 1,936 1,939 1,919 #Mg 0,647 0,69 0,591 0,536 0,653 0,54 0,55 0,62 0,43 0,50 0,38

CHLORITES ANALYSES

FELDSPARS AND SCAPOLITE ANALYSES

ANALYSES OF APATITE

Zone South East Sample 85115N2 APATITE88057O APATITE88057O APA No. 82 87 91 Na2O 0,037 0 0 FeO 0,079 0,138 0,1 Cr2O3 0,016 0,035 0 Cl 1,271 1,253 1,689 MgO 0 0,015 0,014 MnO 0,095 0,22 0,138 K2O 0,016 0,013 0 Al2O3 0,016 0,06 0 NiO 0,015 0 0,021 CaO 53,327 53,542 54,09 SiO2 0 0 0 TiO2 0 0 0 Total 54,585 54,993 55,671 78

AMPHIBOLE ANALYSIS