The Solvik Au Mineralization in South Western Sweden

UNIVERSITY OF GOTHENBURG Department of Earth Sciences Geovetarcentrum/Earth Science Centre

The Solvik Au

mineralization in south

Ulf Christensson

ISSN 1400-3821 B840 Master of Science (120 credits) thesis Göteborg 2015

Mailing address Address Telephone Telefax Geovetarcentrum Geovetarcentrum Geovetarcentrum 031-786 19 56 031-786 19 86 Göteborg University S 405 30 Göteborg Guldhedsgatan 5A S-405 30 Göteborg SWEDEN Abstract

The Gold mineralization at Märrnäset peninsula in Solvik, south western Sweden has been studied in detail in terms of siting of gold, fracture mineralisations, and wall rock alteration. Sample preparation, petrographic studies, SEM-EDS and LA-ICP-MS analysis was carried out at the University of Gothenburg. In the Solvik mineralization, Au is mainly found in electrum (AuAg), either hosted as inclusions in pyrite or along fractures inside the pyrite, associated with chalcopyrite, bismuthinite, and galena. The fault zone hosting the mineralization was brecciated by three different quartz generations, and crystallization of electrum mainly occurred during the third stage. Wall rocks of phyllite and granite show strong K enrichment and Na leaching, indicating that the fault zone controlled a significant hydrothermal system. In the nearby Harnäs mine the, electrum crystallization is reported to have occurred already in the second quartz stage, associated with pyrite only, indicating that the siting of gold may vary between different fault systems in this region.

Keywords: Solvik, Au, Pyrite, Quartz, LA-ICP-MS, SEM,

ISSN:1400-3821 B840 2014

Sammanfattning Guldmineraliseringen på Märrnäset i Solvik, södra Västsverige har studerats i detalj med avseende på lokalisering av guld, sprickmineraliseringar och omvandlingar i sidoberg. Provförberedning, petrografiska studier, SEM - EDS och LA - ICP - MS-analys utfördes på Göteborgs universitet. I Solvik mineraliseringen är Au främst kopplat till elektrum (AuAg ), antingen som inneslutningar i pyrit eller längs sprickor inuti pyrit, associerade med kopparkis , vismutglans och blyglans. Förkastningen som kontrolerar mineraliseringen blev breccierad av tre olika kvarts generationer, och kristallisation av elektrum skedde främst under den tredje generationen. Sidoberget av fyllit och granit visar kraftig K anrikning och Na lakning, vilket indikerar att förkastningen kontrollerade ett betydande hydrotermalt system. I den närbelägna Harnäs gruvan uppges elektrum ha kristalliserat redan i den andra kvarts generation i association endast med pyrit, vilket tyder på att lokaliseringen av guld kan variera mellan olika förkastningssystem i området

Nyckelord Solvik, Guld, Pyrit, Kvarts, LA-ICP-MS, SEM

ISSN:1400-3821 B840 2014

Contents Introduction ...... 5 Objectives ...... 5 Background ...... 5 Geological Background ...... 5 Regional Geology ...... 5 Harnäs mine ...... 6 Local Geology ...... 7 Rock lithologies ...... 7 Hydrotermal processes...... 8 Epithermal systems ...... 8 Au in as Nano inclusions in pyrite ...... 9 Method ...... 9 Sampling ...... 9 Whole rock ...... 9 Optical petrography...... 9 Analytical methods ...... 9 Scanning Electron Microscopy ...... 9 Laser ablation inductive coupled plasma mass spectrometer (LA-ICP-MS) ...... 9 Results ...... 10 Petrography ...... 10 Wall rock and veins in the Solvik area...... 10 Host granite ...... 12 SEM ...... 12 Whole rock ...... 13 Result LA-ICP-MS ...... 13 Time resolved pyrite analysis ...... 14 Time resolved analysis of Au grains ...... 14 Discussion ...... 14 Sitting of Au ...... 14 Sitting of the Ag ...... 17 Alteration ...... 17 Host rock alteration...... 17 The relative ages of the different quartz veins, and the relation to the Au deposition, at Solvik...... 17 Recommendations for future exploration ...... 18

Conclusions ...... 18 Acknowledgements ...... 19 References ...... 19 Appendix 1 ...... 20 Samples location...... 40 Spot positions for LA-ICP-MS ...... 42

Gothenburg Introduction

Objectives The aim of this study was to provide geological Background information about the Au mineralization at Solvik, In 1956, Larsson and Sandgren first reported to gain a better understanding of the mineralization sulphide bearing boulders in the Märrnäset area forming processes, and to provide a guide for future which later have shown to contain Au. From 1956 exploration in the area. The thesis has four main to 2011 four different companies have carried out objectives: exploration in the area, and in 2011 the claim at the Märrnäset in Solvik was sold and is now currently  Petrographic characterisation of the explored by Agnico Eagle Sweden. The area is mineralogy of the host rocks with situated 15 km northeast of Bengtsfors municipality emphasis on the altered and mineralized center, in Dalsland, south western Sweden (Fig. 1). rocks.  Characterise the sitting of the gold.  Identification and characterisation of the sulphides and oxides present and to Geological Background distinguish different pyrite generations.  Try to date the mineralization by Regional Geology describing the occurrence and The western and eastern segments are divided from characteristics of zircon and/or other datable minerals (i.e. rutile, monazite). each other by the mylonite zone (Fig. 2) The western gneissic segment consists mainly of The project includes geochemical analysis and granitic gneiss with intrusion ages of 1.66-1.60 Ga petrographic studies, and all work was carried slightly younger than the granitic genesis of eastern out at the University of Gothenburg. The Au segment 1.70-1.65 Ga. The western segment was grades are not mentioned in grams/tonnage, the deformed by the Gothian orogoney 1.75-1.55 Ga grades are stated as “non Au bearing” or “Au bearing”. The thesis is a cooperation between (Åhäll & Larson, 2000) and the Sveconorvegian Agnico Eagle LTD. and the University of

N S o w r e w d a e y n

Figure 1 Overview map of Märrenäset in Solvik. It is located 15 km to the northeast of Bengtsfors municipality, in the south western Sweden (Google 2014).

Sweconorwegian orogeny (Lindström et al., 1991). In Dalsland- Värmland region, vein mineralizations of quartz, with minor hematite and sulphides tend to have an ESE-WNW orientation. The veining follows the main structural pattern, the veining is most likely to have been formed during the deformation stages of the western domain (Tegengren, 1924).

This district is often referred to as the Mjøsa- Vänern ore district which has its northern boundary in Lake Mjøsa in southern Norway and its southern boundary in Lake Vänern in south western Sweden.

Harnäs mine In the beginning of the 90´s the Au mine at Harnäs was under operation. This mine is situated 16 km to the NW of Solvik and produced ~ 150 kg of Au Figure 2 The mylonite zone (MZ) separating the (Höglund, 2011). The Harnäs mineralization was eastern and western gneissic segments. Further to interpreted to have formed by four main stages (Fig the east the Protoginezone (PZ) is separating the 3). The first stage deposited quartz in veins, at a western and eastern segments from the TIB pressure of 1.0-1.2 kbars and ~ 200 degrees. granitoids (Andersson, Möller et al. 2002). orogeny 1.15-0.90 Ga and formed the greenschist – The fluid was CO2-rich metamorphic fluid which amphibolite facies gneiss (Lindström, Lundqvist, & possibly was mixed with metamorphic water. The Lundqvist, 1991). quartz deposition occurred under decreasing pressure, as the CO2 was boiled off. The second The older gneisses in Dalsland formed a bottom to stage of this system has been the main pyrite-gold a sedimentary sequences of sandstone, shales and stage, which is a continuation of the first stage, with spilitized basic volcanites during an extensional a lower pressure ~0.3-0.4 kbars and lower CO2 event between 1.33 and 1.03 Ga that experienced content. This stage is associated with intense wall low grade metamorphism during the rock alteration of K-feldspar into sericite. The alteration in combination with mineralogy in the vein suggests that the main sulphur in the aqueous

solution has been H2S. During the wall rock

alteration and effervescence of CO2 and H2S, the pressure dropped and coprecipitated Au and pyrite in the fractured quartz and simultaneously altered the wall rock. The coprecipitation is indicated by primary inclusions of Au in pyrite or in close proximity to the pyrite. Movements along the ore shear zone could explain the occurrence of Au in thin fractures in the pyrite by physical remobilisation. The third stage of Harnäs is known

as the galena stage. At this stage there was no CO2 left in the system. Galena, chalcopyrite and minor pyrite were deposited, filling up fractured quartz and cataclastic early pyrite, and only minor Au was present. The low temperatures might indicate that the base metals are from the cooling of stage two. But a late stage fluid cannot be excluded. A fourth late stage of crosscutting quartz- calcite veins, with pure meteoric source was also observed (Alm et al., 2003) Figure 3 Schematic model of the Harnäs development(Alm, Broman, Billström, Sundblad, & Torssander, 2003). 6

Local Geology

The bedrock at Solvik peninsula in Lake Östra- silien has been mapped by Agnico-Eagle ltd. (Fig. 4). The cataclastic fault breccia has been the main target for the drilling program. This fault has previously been classified as a third order fault system after, the main north-south stretching fault system, and after the east- west lineation and fault system (Witschard, 1989a). (Witschard) defines the fault system as a “dislocation” strike-slip -type (c.f. figure 4) that could reflect major rigid movements within the Baltic shield (Witschard, 1989b). About 6,5 kilometres to the NNW from Märrnäset in a parallel NW structure there is one silica sinter hill Figure 5 Massive quartz outcrop in Hökenäs, ~ of ~ 100x600 metres. This outcrop is located in the 100x600 meters. The hematite is seen as the darker valley of the fault zone, and consists mainly of pure veining’s in this picture. quartz with minor fractures filled with hematite (fig.5). Rock lithologies The rock lithology in the Marenäset area consists of two main units, the first are Proterozoic intrusive rocks. The Proterozoic rocks consist of two types of granitic gneiss: (1) pink to red fine - grained, aplitic, partly showing biotite-foliation, and (2) pink to brownish red medium-grained biotite-foliated, and often containing augens of k-feldspar. The former is named Kroppefjäll and the latter are from the Åmål granitic suite. These two granitic units are Märrnäset here mapped as granitic gneisses.

A Mesoproterozoic sedimentary sequence from the Dal formation is the second main unit at Märrnäset, and is postdates the proterozoic granites. In Märrnäset four different sedimentary units are present. First is quartzite, it consists of light grey to brownish grey fine-grained meta-sandstone. In some outcrops ripple marks can be observed. Busterud Second unit is the fine to medium grained limestone, which is hosted within the quartzite. Third unit is the metabasalt (mafic volcanic rock) which is dark greenish black to green, mainly foliated, it´s stratigraphically over the quartzite and below the phyllite. It sometimes holds magnetite in sufficient concentrations to locally disturb the Figure 4 Bedrock map of the peninsula and its continuation to southwest. The sinisterly dislocation compass. It is likely to be in lower amphibole facies of this system is ~ 800 meters (Höglund 2011). since amphiboles have been noted. Phyllite is the fourth unit in the Mesoproterozoic sequence at Märrnäset. It is characterized by lustrous grey to dull grey colour, distinct foliation and strong lineation. (Höglund, 2011).

Hydrotermal processes Hg, Sb, Cu, Se, Bi, U. This type of system is found A hydrothermal system is the process of hot water in sedimentary or igneous rocks, often in post circulating both vertical and lateral below the Precambrian rocks not deeply eroded since ore surface of the crust (Pirajno, 2009). These fluids formation. They are often located in fault and joints may over sufficient time transport enough metals to systems (Evans, 2009). There are two different cause an anomaly of metals in an area. Whatever types of epithermal systems. The first is called the the anomaly that give rise to an ore, is determined Acid - sulphate and second is Adularia - sericite. on location, scale, type of deposit, and other The latter type is more abundant than the former. economic parameters. But there are two things that These two types have lately been referred to as high must exist for a hydrothermal system to form. sulphidation system and low sulphidation systems, Firstly, a heat source, of sufficient energy to drive the former refers to Acid- sulphate. The latter to the system, and a fluid phase. The origin of the Adularia- sericite (Corbett, 2005) (Table 1). Both fluids may come from surface (meteoric water), the epithermal systems are found in similar tectonic ocean (sea water), or from magmatic sources or settings associated on continental scale with metamorphism (Evans, 2009). Secondly, the subduction zones at plate boundaries. The ore hydrothermal system needs a pathway through occurs in structurally complex environments, with which hot fluids can be transported. To form a several generations of faults in two or more mineralization there must also be a source rock for directions (Heald et al., 1987). the metals to leach from, and there must also be a Table 1 Mineralogical difference between Acid- deposition place (Pirajno, 2009). Examples of sulphate and Adularia - sericite. From (Heald, Foley deposition sites for a mineralization are faults, and Hayba, 1987) fractures networks and shear zones (Pirajno, 2009), see figure 6. Acid- sulphate Adularia- sericite (High Sulphidation) (Low Sulphidation) Enargite + Pyrite ± No Enargite covelite Extensive Sericitic alteration hypogene alunite dominant Major hyporgene Sometimes kaolinite Kaolenite No adularia Adularia No selenides Often selenides Mn minerals rare Mn gangue present Chlorite rare Often chlorite Sometimes No bismuthinite bismuthinite

In high Sulphidation deposits an advanced argillic alteration is typically associated with the ore. Alunite and kaolinite are other minerals from the argillic assemblage that occur close to the vein and are often formed at the same time as the silicification. The low sulphidation type deposits Figure 6 Structural illustration of a hydrothermal system. Whit the main components, fluid reservoir, are characterized by the dominance of sericitic metal source, path ways, and deposition place alteration in the proximity to the silicified zone (Pirajno 2009). close to the vein. In close proximity to the vein, fine grained potassium feldspar and / or chlorite is

typically disseminated in to the surrounding wall Epithermal systems rock. The serictic zone typically grades outward into a propylitic zone and sometimes in to a Epithermal systems are formed in near surface potassium metasomatized zone (Heald et al., 1987) conditions to 1500 meters and between 50-200 see fig 7. degrees, and they can form ores for Au, Ag, Pb, Zn,

Figure 7 Schematic diagram showing the alteration zones and vein mineral assemblage. For both Acid- sulphate system and Adularia sericite type deposits from (Heald, Foley, & Hayba, 1987). Au as Nano inclusions in pyrite Optical petrography It is not uncommon to find Au in pyrite, either as For petrographic analyses 17 thin sections were free grains inside the pyrite or along tiny fractures, made from the drill cores from Solvik. Both the as native Au or electrum. The pyrite grain might production and the petrography work were carried hold Au as nanoparticle of a variety of out at the University of Gothenburg. compositions.This has been proven by studying of the time resolved spectra from the La-ICP-MS (Deditius et al., 2011). It has been reported that the Analytical methods pyrite holds micro/nanoparticles of Pb, Co, Ni, As, Bi, Ag, Te and Au. In the forms of native Au and Scanning Electron Microscopy Au-Ag telluride’s, and Bi- Ag- Te- Galena (Large, All thin sections and rock slabs were analysed with Maslennikov, Robert, Danyushevsky, & Chang, the scanning electron microscope (SEM) at the 2007) this is also reported by (Sung et al., 2009) University of Gothenburg. The analyses were made who discuss native Au, electrum and Au(Ag) on a HITATCHI S-3400N operating at high tellurides in pyrite. vacuum and specimen current of 3.5 nA at 20 kV and 9.5 mm working distance, with a calibrated Oxford instrument energy-dispersive X-ray Method analytical system. A backscattered electron (BSE) detector was used for imaging. The Au grains were Sampling identified by an automated run based on A total of 34 samples were collected from the drill electrondensity in BSE, by cancelling out all light cores of SOL11004, SOL11005, SOL12001 and minerals. Only galena and denser minerals were SOL8. detected and analysed.

Whole rock Six samples (1-4 and 16, 17) have been collected from the drill core SOL-11005. They are first Laser ablation inductive coupled crushed in a cast iron pounder in to fine gravel. plasma mass spectrometer (LA- The gravel was milled for 15 minutes in a swing ICP-MS) mill to get a completely homogenized sample. Five The LA-ICP-MS analysis was carried out on a grams from each was sent to ALS in Dublin, NEW WAVE Research 213nm laser coupled with Ireland for whole-rock analysis ICP- MS.

9 an Agilent 7500a quadropoule ICP-MS. The pyrite through the section, quartz make up an average of was analysed for 23 elements by a 30x30 μm square 60%, chlorite 18%, sericite 12% and calcite 3%. spot, with a frequency of 5Hz and an energy of 3.0 This lithological unit can be seen in the drill core J/Cm2. The elements analysed in the pyrite matrix SOL11005 from 5 to 175.80 m, in the interval of were S, Ti, Fe, Co, Ni, Cu, Zn, Ga, As, Se, Mo, Ag, 122.05 to 175.80m it looks different than the earlier Cd, In, Sn, Sb, Te, W, Hg, Pb, Bi and U. Electrum portion of the drill core. The reddish colour that was analysed using the same conditions but with a locally stands out is due to the hematite grains 10x10 μm square spot and only 15 elements. For which stain the rock. The matrix is very fine- the electrum grains the following were analysed S, grained and shows laminated in bands. The Cu, Se, Pd, Ag, Cd, Sb, Te, Pt, Au, Hg, Pb, Bi, Th foliation is made up of the lamination, of chlorite, and U. The analytical data was filtered in glitter sericite and hematite. The quartz and calcite is with the standards of NISTSRM610, Mass -1, Po disseminated through the unit, but the calcite is 725 and Bam-H005. NISTSRM610 is a silicate both as dissemination and in late veins that standard to correlate the drift of the instrument. intersects the unit. In the figure 8a-d the K, Na, Mg Mass -1 is a sulphide pellet reference material that and Zr is plotted against Al content. The red contains high amount of base metals and platinum squares represent samples that were mapped as group elements including Au and Ag and was used metaphyllite and the blue represent altered as primary standard for the analysis. The Po-725 is metaphyllites. The plot of K vs. Al, (fig. 8a) show a another sulphide standard which was used as a complex trend. There are no clear difference in the secondary standard for platinum group elements. K content between metaphyllite and altered The Bam- H005 was used as a secondary standard metaphyllite. The samples with the lowest K are for Br, Cd, Cr, Hg and Pb. The final concentrations furthest from the fault zone. This K alteration are were calculated in Microsoft excel spread sheet mostly dependent on the distance to the fault zone. from the counts, to be able to use more than one In figure 8b, the depletion of Na is seen in the standard for comparison. The spread sheet was altered metaphyllite in contrast to the metaphyllite, provided by Zack. Thomas. which has a higer overall content of Na. Plots of Mg and Zr against Al show no difference between metaphyllite and altered metaphyllite. The Results metaphyllite and the altered metaphyllite was originally the same rock, but the parts closest to the Petrography mineralisation have been affected by hydrothermal alteration. Wall rock and veins in the Solvik Sericite and Quartz altered granite area. Sericite and quartz altered granite is olive green in There are a six different rock types present in colour and it consists of ~ 73% sericite and 27% Solvik on the peninsula, and here is a summary of quartz and minor hematite. The ground mass is very the characteristics of these six different types of fine-grained and is strongly foliated. There are two lithology. The mineral modal abundance is different types of veins that intersect this estimated from the microscopic work. For a full lithological unit. The oldest quartz vein is coarse description of each sample and there location in the grained and holds a larger amount of pyrite up to ~ drill hole profile see appendix. 1. 50% and only minor amount of chalcopyrite. The Metaphyllite second quartz vein is also coarse grained and is distinguished by a higher modal abundance of Metaphyllite is typically very fine grained, strongly chalcopyrite. This second quartz vein can hold very foliated and sheaered. It varies from greenish grey large amount of chalcopyrite which can be seen in to spotty reddish grey. The metaphyllite consists the sample SOL11005-11 were a quartz vein mainly of quartz, chlorite, sericite, and hematite, brecciate the earlier pyrite (Fig 9). greay in figure 30 (Appendix 1) The altered metaphyllite is a phyllite which has been affected by hydrothermal alteration, and therefore was given this altered metaphyllite name, in the model of the Solvik peninsula, green in figure 30 (Appendix 1) The modal composition of the minerals is varying

Figure 8 Red boxes are the metaphyllite and the blue diamonds are the altered metaphyllite. From the diagram of (a) an enrichment of the potassium is seen. The blue dots with the lowest K are furthest from the fault zone. For b an depletion of sodium is seen in the altered metapylite, c and d of Mg and Zr no differences are seen. Therefor indicating that the host rock is the same but only a portion of the drill core adjacent to the fault zone has been affected by the potasic alteration. The data is from drill cores SOL 11003, SOL 11004, SOL 11005 and SOL 12001.

grains of zircon, monazite, apatite and xenotime were found. The grain s of zircon and monazite were very few and small ~ 5 μm and could only be located by the SEM. Three different types of quartz veins have been found to be part of this breccia. The first quartz vein generation is identified by greyish greasy colour. It is made of large euhedral quartz grains ~ 500-1000 μm that holds very large euhedral pyrite grains, ~50-5000 μm, and minor chalcopyrite. The second quartz vein has a bone- white colour, but is generally similar to the former in terms of the large quartz grains and large pyrite grains. However chalcopyrite is absent, and most of Figure 9 This second quartz vein is from the sample the pyrite is located along the border of the vein. are SOL11005-11. Here it is obvious to see that large amounts of chalcopyrite are present in this The third and latest vein is fine grained and carries second quartz vein. mainly chalcopyrite and minor amount pyrite. Some of the chalcopyrite grains are very large, between 5-10 mm long. Quartz vein breccia The fault zone has been brecciated by three The Au in this lithology is mainly found as different quartz generations. The wall rock consists electrum inside larger pyrite grains. The bone-white of very high grade of sericite ~ 90 % and 10% quartz seen in the SOL11005-6, SOL11005-8 and quartz characterized by it is greyish green colour SOL12001-9 holds no Au. The quartz vein that is and very fine grained texture. In the wall rock, greasy greyish in colour and contains large pyrite is

11 the one that hold some of the Au. In this quartz- vein breccia, one Au grain was also found in the host rock outside of the brecciating veins (fig 1)However in the drill hole SOL 8 samples 1,2,3,&4) a fluorite bearing quarts breccia is also found, to be brecciating the metaphyllite, the fluorite is both green and pink with large >5mm euhedral grains are common.

Figure 11 Granite classification diagram of (Julian A. Pearce. 1984). This diagram indicating that the granites of sample 11005-1 to 11005-4 are Quartz classified as volcanic arc granite & syn – collision. Au SEM In the SEM scan of the polished thin sections and rock slabs, all the Au bearing grains and minerals of approximately equal density was located e.g bismuthinite and its alloys with galena. The result Figure 10 SEM image of sample 11005-9. On free of the scans is that almost all Au bearing grains that gold grain in, wall rock quartz. was found was the alloy electrum, there are only Quartz feldspar porphyry one grain found that was considered to be as native The quartz feldspar porphyry is seen in the 12001-1 Au. The electrum was found inside the pyrite or it is visually brick-red and aplitic with larger clasts along the fracture planes in the pyrite. When the of micropertitic K-feldspar and consolidated grains electrum was observed there was always more or of quartz. The phenochrysts are typically 0.5- less chalcopyrite present. Bismuthinite was 2.0mm in diameter. The matrix is fine grained and frequently also found were often found in close consists mainly of quartz of 95% and only of 5% proximity to electrum. In fig 12 below we see sericite. electrum inside the pyrite grains together with chalcopyrite. The second place that the electrum Cataclastic granite typically are hosted are with the brecciating This unit is typically very fine grained and brick chalcopyrite in the pyrite, this chalcopyrite also red, it mainly consists of 78% quartz, 20% sericite carries large amount of bismuthinite, see (Fig. 13) and minor hematite, 2%. The hematite is probably causing the red staining of this unit. This cataclastic unit has been cut by chlorite and calcite veins. The chlorite veins are often found along old fractures. See Appendix 1 11005-16.

Host granite In the diagram of (Julian A. Pearce., 1984) (Fig. 11) four of samples were plotted (SOL11005-1-4) samples SOL11005-16 & 17 was left out, because they are too rich in silica and are not valid in this classification diagram. All samples plots within the volcanic arc granites & syn- collision Granites area.

Whole rock Whole rock chemistry can be used to investigate the sitting of Au, and a number of element ratios of certain interest is plotted in fig 14. In fig. 14a it is Pyrite clear that Au correlates with the Ag. However, Chalcopyrite elevated concentrations of Ag is found in some samples without elevated Au concentrations, indicating that Ag also occur in other minerals. For the relation between Au and Bi (fig 14 b), the same Electrum trend is visible as for Au and. Ag. They indicate a good correlation between them, but just like in 14a, there may be Bi presentbut no Au. Fig 14c show a Chalcopyrite very strong correlation between Ag and Bi, indicating that the concentrations of these elements are controlled by same mineral phase. When plotting the Au vs. S (fig 14 d), it is clear that most of the Au is correlated with the presence of sulphides, but Au is also found where only minor P sulphides is present. Quartz Result LA-ICP-MS From the LA-ICP-MS analysis of the pyrite grains (table 1 appendix 1) the following results were Figure 12 Electrum hosted inside a pyrite crystal. obtained. Sulphur and iron is the main constitution The electrum is located with chalcopyrite.This is of the pyrite, but Mo, Ni, Co and As is also present. from 11005-12 Ag, Cu, Pb and Bi are elevated in many analyses. The relatively high Ag concentrations in some analyses are always correlated to the high Lead and Bismuthinite Bismuth concentrations. The copper concentrations are elevated in some analysis, which is probably Electrum due to small inclusions of chalcopyrite. This can be seen in figure 7 appendix 1 from sample Pyrite SOL11005-6 where the chalcopyrite is seen as inclusions. Spot analyses 22-26 (table 1 appendix 1) Chalcopyrite are from the SOL11005-6 and show high copper content. The LA-ICP-MS analyses of the “Au” grains are presented in table 2 appendix 1were it can be shown that the “Au” grains are actually electrum Pyrite and consists to a large portion of Ag. There are always Bi and lead present in the grains. The concentrations of Bi and Pb are in range of a few Quartz hundred ppm to just below 29%. The content of Hg is ~ 800 ppm for all except for spot 97 where it is ~ 1200ppm. The spots 84, 95, 96, 98 and 99 are all very high in copper, but contaminated by chalcopyrite.

Figure 13 Electrum hosted with the brecciating chalcopyrite, and bismuthinite in the pyrite. This is from the sample 12001-5.

Figure 14 Au vs. Ag, to in most cases the Au seems correlate with the presence of Ag. All higher Au results are hosted with higher Ag content. Au vs. Bi, the Au content tends to be higher with the higher Bi content. Ag vs. Bi, this is probably one of the best correlations that can be seen when comparing elements. The Ag and Bi is strongly bound to each other. Au vs. S, this to correlate Au to the presence of sulphur minerals. All data are from 48 elements by ICP-MS with FA AA finish for gold, if grade over 3.0 g/t, data from Höglund Kåre presented on a log log scale.

Time resolved pyrite analysis the Au grains in the pyrite is 38,3% Au and 32,5% Ag in spot 93 and 44.7% Au and 54.9% Ag in spot For spots 31, 40, 58 and 61 is presented in figure 94 and 49% Au and 50.7% Ag in spot 97. 15. The figure shows time resolved spectrum where the counts over time are plotted for Cu, Ag, Au, Bi and Pb in these diagrams it is obvious that Bi, Ag Discussion and Pb is strongly correlated to each other. Cu is showing a similar trends but at lower counts. Au is Sitting of Au typically correlated with bismuth, lead and Ag. The Au at Solvik is almost only seen as electrum, Copper rarely show the same pattern as Au. The and only in one occasion a native Au grain was spikes in the diagrams are inclusions in the pyrite found. The Au at Solvik is hosted in the second that are intersected by the laser. These spikes are generation of quartz and pyrite veins that brecciates indicated by black arrows in in the figure 15. The the area, this vein generation is often carrying actual Au content from the pyrite matrix is 0.2 ppm chalcopyrite. The different generation will be in spot 31 and 0 ppm in spot 40 & 58 and 0.1 ppm discussed later. Electrum is in most cases hosted in spot 61. inside the pyrite and sometimes also in the chalcopyrite. Gold and pyrite was probably in solid

solution during higher temperatures and as the Time resolved analysis of Au grains system cooled off, the Au was exsolved. These When plotting the count per second against ablation precipitated grains of electrum are sometimes fairly time of Cu, Ag, Au, Hg, Pb and Bi, for spot, 93, 94 large and can be up to 50 μm, but they are often and 97 it is obvious the Au and Ag are strongly very small and are only seen in the time resolved connected to each other (Fig. 16). Pb and Bi are spectra from the laser, where the micro-inclusions elevated with high Au and Ag content. For the Cu are represented as spikes in the Au and Ag signal and Hg, the trend is similar to Au and Ag but at figs (15a). The Au is not dissolved in the matrix of lower counts. The actual Au and Ag, content from the pyrite crystal to any major extent indicated by low concentrations of Au in inclusion free pyrite.

10000000 1000000 31 100000 C 10000 P 1000 S 100 10 1 0,0 10,0 20,0 30,0 40,0 50,0 60,0 Time (S)

1000000 100000 40 10000 C P 1000 S 100

10 1 0,0 10,0 20,0 30,0 40,0 50,0 60,0 Time (S) 10000000 58 1000000 100000 10000 C P 1000

S 100 10 1 0,0 10,0 20,0 30,0 40,0 50,0 60,0 Time (S) 10000000 1000000 61 100000 C 10000 P 1000 S 100 10 1 0,0 10,0 20,0 30,0 40,0 50,0 60,0 Cu63 Ag107 Au197 Pb208 Bi209 Time (S)

Figure 15 Time resolved spectrum of pyrite matrix of sample 11005-11 for spots 31, 40, 58 in site 1 an spot 61 in sitet 2. Au content in pyrite matrix of each point are 0,2 ppm in spot 31 and 0 ppm in spot 40 & 58 and 0,1 ppm in spot 61. The black arrows indicate were the micro inclusions are seen.

100000000 93 10000000 1000000 C 100000 P 10000 S 1000 100 10

1,795 0,265 3,325 4,855 6,386 7,916 9,446

18,627 35,459 10,976 12,506 14,036 15,567 17,097 20,157 21,687 23,217 24,748 26,278 27,808 29,338 30,868 32,398 33,929 36,989 38,519 Time (S)

100000000 94 10000000 1000000 C 100000 P 10000 S 1000 100 10

0,265 1,795 3,325 4,856 6,386 7,916 9,446

32,398 10,976 12,506 14,037 15,567 17,097 18,627 20,157 21,687 23,218 24,748 26,278 27,808 29,338 30,868 33,929 35,459 36,989 38,519 Time (S)

100000000 10000000 97 1000000 100000 10000 1000 100 10

0,265 1,795 3,326 4,856 6,386 7,916 9,446

10,976 12,506 14,037 15,567 17,097 18,627 20,157 21,687 23,218 24,748 26,278 27,808 29,338 30,868 32,399 33,929 35,459 36,989 38,519 Time (S) Cu63 Ag107 Au197 Hg202 Pb208 Bi209

Figure 16 Time resolved spectrum of Au grain in pyrite spot 93 sample 11005-12 site 2. Time resolved spectrum of Au grain in pyrite spot 94 sample 11005-12 site 2. The correlation between the Bi and Pb is very clear. Time resolved spectrum of Electrum grain in pyrite spot 97 sample 11005-13 site 2. The laser intersects a Bi- Pb grain.

When studying the time resolved spectrums of There is one case where electrum was encountered pyrite and electrums grains it is clear that Au as an inclusion in chalcopyrite, in this study it is always coexists with Ag, and often with Bi, Pb and uncommon that Au is hosted as inclusions in Cu. Figure 15a-d from the pyrite, indicate that when chalcopyrite. However, this chalcopyrite grain the laser intersects Au then also the Ag, Bi and Pb belongs to the second generation of quartz and increase. A good correlation for Cu is only seen in a pyrite veins, which represent the main Au stage in few cases. Solvik. This grain is seen in the SOL11005-13, see appendix 1.

There is also one grain of native Au in the 11005-9 This might indicate that the Solvik mineralization inside the quartz,. This is the only place where is on the upper side of a lower Sulphidation system. native Au is observed. (intrusion related quartz and suliphide Au ± Cu system). Sitting of the Ag The relation of Au to Ag has been discussed above, The relative ages of the different but the relation between the Ag, Pb and Bi should quartz veins, and the relation to the be clarified. The extremely good correlation Au deposition, at Solvik. between Ag and bismuth seen in fig 8 is obvious. The goal to date the mineralization was not possible This in combination with the time resolved LA- to accomplish, even if there were some minerals ICP-MS analysis of both the pyrites and the “Au” present which could be used. The problem grains. The Ag at Solvik, is likely to be hosted with encountered were that they were too small and few the Bi and Pb as bismuthinite or galena. to be analysed, the grains of monazite which were found was < 5μm. The high number of analysis from the SEM work where many grains of Ag rich Bismuthinite and Ag- There are three different quartz vein generations in and Bi-rich galena was encountered, especially in the Solvik area. They can be differentiated by their the more chalcopyrite rich stage of the second mineral composition. The oldest generation of quartz pyrite generation. Indicate that the majority quartz that intersects the wall rock is the pure of Ag is hosted in this quartz pyrite generation. quartz, which likely corresponds to stage one of (Alm et al., 2003). Alteration The oldest quartz pyrite generation is the one that Host rock alteration. are seen in the 11005-8 (Fig. 17). It is typically The entire mineralized zone at Solvik has been massive in its appearance and looks fine grained. affected by alteration; the quartz and sericite This generation of pyrite do not carry any alteration are most common. It seems that the area chalcopyrite or Au. This quartz and pyrite is silicified by large amounts of quartz, this is generation is likely slightly mylonitiesed, (see especially clear in SOL11005-1 and in SOL12001-1 appendix). This mylonitization explains why these which holds between 80- 95% quartz in their veins seems so massive. matrix. They are extremely hard and almost impossible to cut, which is likely linked to the first quartz generation that affected the area. The second alteration is the phyllic alteration, where feldspar has been altered to sericite. This is seen as the wast amounts of sericite throughout the mineralizone e.g. sample 11005-11.The fact that the Solvik also has been heavily brecciated by 3 quartz generations both with and without sulphides, makes the area look quite complex at the first sight.

To put the Solvik mineralization in high or low sulphidation stage is not easily defined, because the mineralogical components in the Solvik are slightly in between them. The Solvik system is probably in Figure 17 Sample 11005-8, the oldest quartz pyrite generation in the Solvik area. It is typically massive between a high sulphidiation system and a low in its appearance. Photo in reflected light. sulphidation. This is indicated by the relatively high content of sericite and also by the presence of The second quartz pyrite generation is characterized chlorite, which is typical for the low sulphide by the occurrence of pyrite and chalcopyrite. This system, the bismuth, which is seen in the close generation is the Au bearing stage at Solvik, and relation to the major Au bearing stage. can be subdivided into an early and one late phase. The fluid chemistry seems to evolve during crystallization of this generation. In the early stage,

17 pyrite is dominating and only limited amount of Recommendations for future chalcopyrite has been crystallized. During its later exploration stages, less pyrite and more chalcopyrite and finally What is noticed is the enrichment of potassium in only chalcopyrite crystallizes. the sequence throughout the mineralized zone, The first stage of the second generation is found in except for the quartz vein breccia zone. The fact the samples 11005-6 and 1005-13. The chalcopyrite that potassium is slightly radioactive, should make in the oldest veins of these samples is mainly it possible to detect this alteration by a handheld present as inclusions inside the pyrite. These gamma spectrometer, to identify potassium rich inclusions are common and vary in size from 50 μm areas during field work. This method could possibly large down to sub-micro inclusions in the pyrite. locate previously invisible alteration zones for Figure 17 in appendix 1 of 11005-13 represents that further work. electrum grain and the related chalcopyrite are present. These inclusions are also seen in the figure 15 where the spikes of Au, Ag, Cu, Bi and Pb, Conclusions indicate submicron inclusion inside the pyrite. There are two main alterations in the Solvik area, the first is the quartz alteration that has totally Propagation of this second generation quartz vein silicified the granites in some cases up to above continues until it consists almost entirely of 90% quartz. The second alteration stage at Solvik is chalcopyrite, bismuthinite and galena. This late the phyllic alteration of the feldspar to sericite. In stage of this second generation often reactivates the the entire zone, there are only small amounts of early veins and carries with it the chalcopyrite and feldspars left, and most has been altered in to often the bismuthinite and Bi, Ag- rich galena. sericite. It is only in the quartz feldspar porphyry This late chalcopyrite breccia is best seen in the where the K- feldspar is observed as phenochrysts. sample 11005-11 (appendix 1 fig 11&12). In the sericite and quartz altered granite the sericite Reflected light images clearly show that that content is reaching ~ 50%. The Solvik area is chalcopyrite co-crystallized with bismuthinite and probably on the highside of a lower sulphidation electrum (fig 18) system (intrusion related quartz and suliphide Au ± Cu system). This is indicated by the presence of bismuth, chalcopyrite and structural and extural observations. However, due to the complex relations of the multiple veins that intersects the mineralization, this study may only be a initial step to full understanding of the evolution of the Solvik mineralization.

This thesis have revealed that the second quartz and pyrite is the main Au- bearing stage of the Solvik mineralization and the Au-bearing phase in this stage is mainly electrum. This second generation is brecciating the older silica altered granites, and the second generation is often carrying chalcopyrite. A few grains of electrum can be seen under the Figure 18 Chalcopyrite filled vein in pyrite with electrum and bismuthinite, 12001-5. Photo from microscope inside the pyrite or along fractures of reflected light the pyrites, but only the largest grains, up to ~50 μm, are visible. The bulk of Au is hosted as micro The third and last quartz generation is the bone- inclusions in electrum inside the pyrite. These white type. This generation is commonly seen micro inclusions of the pyrite show a strong throughout the area and cut the previous quartz correlation with the Bi, Ag and Pb, and therefore veins. However, there is one example where a indicating that more Au may be hosted in bone-white quartz vein is cut by a vein belonging to mineralizations characteraized by higher degree of generation 2 suggesting a more complex age sulphidation than at Solvik. relation between generation 2 and 3.

A radiometric dating of the minealization was not hosted epithermal deposits; acid- accomplished, even though there were monazite sulfate and adularia-sericite types. present in some of the samples which could have Economic Geology, 82(1), 1-26. been used for dating. However, they were all too Höglund, K. (2011). Solvik Project ONLY small (< 5 μm). Exploration Report 2011: Agnico Eagle Ltd. Acknowledgements Höglund, K. (2012). Solvik Project ONLY I want to thank Kåre Höglund and Agnico- Eagle Exploration Report 2011: Agnico Eagle LTD for providing me with this opportunity to Ltd. work on this project. I also want to thank, my Julian A. Pearce., N. B. W. H., Andrew G. advisor Johan Hogmalm for great support and for Tindle. (1984). Trace Element showing dedication to my work and who Discrimination Diagrams for contributed to many valuable discussions. I also theTectonic Interpretation of Granitic want to thank my family who has supported me Rocks. Journal of Petrology., 25(4), during my last two decades of shool. A special 956-983. thank should go to Marianne. R, Joakim. J and Large, R. R., Maslennikov, V. V., Robert, F., Pär.K and Sofia.K for valuable critics. And to Danyushevsky, L. V., & Chang, Z. Johnny Eliason for teaching me the noble art of (2007). Multistage sedimentary and gold panning and for putting the Solvik gold metamorphic origin of pyrite and gold mineralization back on the map. in the giant Sukhoi Log deposit, Lena Gold Province, Russia. Economic

Geology, 102(7), 1233-1267. References Lindström, M., Lundqvist, J., & Lundqvist, T. (1991). Sveriges geologi från urtid till Åhäll, K.-I., & Larson, S. Å. (2000). Growth- nutid: Studentlitteratur. related 1.85–1.55 Ga magmatism in Pirajno, F. (2009). Hydrothermal Processes the Baltic Shield; a review addressing and Mineral Systems. the tectonic characteristics of Sung, Y.-H., Brugger, J., Ciobanu, C. L., Pring, Svecofennian, TIB 1-related, and A., Skinner, W., & Nugus, M. (2009). Gothian events. GFF, 122(2), 193-206. Invisible gold in arsenian pyrite and Alm, E., Broman, C., Billström, K., Sundblad, K., arsenopyrite from a multistage & Torssander, P. (2003). Fluid Archaean gold deposit: Sunrise Dam, characteristics and genesis of early Eastern Goldfields Province, Western Neoproterozoic orogenic gold-quartz Australia. Mineralium Deposita, 44(7), veins in the Harnäs area, 765-791. southwestern Sweden. Economic Tegengren, F. R. (1924). Sveriges ädlare Geology, 98(7), 1311-1328. malmer och bergverk: Kungl. Corbett, G. (2005). Epithermal Au-Ag deposit boktryckeriet, PA Norstedt & söner. types-implications for exploration. Witschard, F. (1989a). Satellite Imagery Deditius, A. P., Utsunomiya, S., Reich, M., Interpretation (pp. 23): Nämden för Kesler, S. E., Ewing, R. C., Hough, R., & statens gruvegendom. Walshe, J. (2011). Trace metal Witschard, F. (1989b). Satellite Imagery nanoparticles in pyrite. Ore Geology Interpretation. 23. Reviews, 42(1), 32-46. Evans, A. M. (2009). Ore geology and industrial minerals: An introduction: Wiley. com. Heald, P., Foley, N. K., & Hayba, D. O. (1987). Comparative anatomy of volcanic-

Appendix 1

Microscopy work and SEM This appendix describes each sample individually both by the petrographic work and by SEM. The samples exact locations along the drill core are shown in two cross section maps of the Märrnäset peninsula at Solvik. Later on in this appendix the results of the LA-ICP-MS work are presented for each spot both for the pyrite analysis and the “Au grains”. The exact location of each spot is presented on all of the grains.

SOL11005-1 95.83-95.92 Metaphyllite; Not Au-bearing. The rock sample is fine-grained and strongly foliated. It consists of ~. 80% undulose quartz, 18 % of chlorite and 2% of hematite. Small grains of hematite are present in the foliation that probably causes the red colour. In (Fig. 1) below a foliated band of chlorite and calcite grains is seen. The opaque mineral is hematite. The foliation is cut by a quartz-calcite vein. The quartz-calcite vein is also cut in to the foliation. Some late movement along the foliation plane has taken place, because the foliation has sheered across the quartz-calcite vein.

Figure 1. Band of foliated chlorite and calcite in metaphyllite. The big oval grain in the chlorite vein is calcite; opaque mineral in wall rock is hematite. Left photo is in plane polarized light and right in cross polarized light.

SOL11005-3 124.00-124.10 Metaphyllite; not Au-bearing. The sample has a strong foliation and is fine-grained. The foliation consists of ~ 70 % undulose quartz, 10% chlorite, 10% sericite, and 10% hematite. Hematite is present as opaque grains in the more reddish parts of the foliation. The foliation is cut by a late stage of fine-grained calcite and quartz veins, which also is fracturing into the foliation. In (fig. 2) one of those veins cutting through the foliation.

Figure 2. Quartz and calcite vein cutting through the foliation of the metaphyllite. The wall rock is seen in the upper and lower part of the photo and consists of 70% Quartz, 10% Chlorite and 10 % opaque hematite. The photo to the left is in plane polarized and right is in cross polarized light. SOL11005-4 155.60-155.70 Metaphyllite; not Au-bearing. It is very fine-grained and has a strong foliation and consists mainly of 30% quartz, 25 % sericite, 25% chlorite, 10% calcite and 10 % hematite as opaque face. The matrix is fine-grained and laminated into fine bands where the chlorite and sericite lies in the foliation see fig. 3.The quartz is mainly disseminated through the section but it forms larger bands that lay in the foliation thorough the section. Chlorite is often found along the fractures. The calcite is like the quartz disseminated throughout the thin section but the main concentrations of calcite are in late veins that cut through the foliation.

Figure 3. Sample SOL11005-4 from the lithological unit metaphyllite. The green tone seen in the left is due to the fairly large amount of chlorite, in the right picture the colourful grains are sericite. The slightly larger grains in white and black are quartz, except for those black grains in plane polarized light which is hematite. The left picture is taken in plane polarized light and the right in cross polarized light.

SOL11005-6 177.17-177.26 Quartz vein breccia; not Au-bearing. The surrounding wall rock is very fine-grained, it mainly consists of very fine-grained sericite (90%) and quartz

(10%) and there are also some small zircon grains, apatite, monazite and xenotime (YPO4). Both the zircon grains and the monazite grains are all very small, ~ 5µm. Three different quartz veins sets are identified in this sample, the oldest vein consists of larger grained quartz with a size range between 500 and 1000 µm. Additionally it holds large grains 50 -5000 µm of euhedral – anhedral pyrite grains, in between the quartz grains there are chalcopyrite grains smaller than 200 µm. This oldest vein generation is shown (Fig. 4).

Figure 4. This is the oldest quartz vein that brecciates this sample. The quartz is relatively coarse-grained 0.5-1mm and holds pyrite from 50 µm -5 mm in size. In between the pyrite grains there are also some smaller grains of chalcopyrite which are all smaller than 0.2mm.

The second vein which intersects the sample is also formed by coarse-grained quartz, 500-1000µm, it holds euhedral pyrite grains between 20-2000 µm. Most of the pyrite grains are located in the borders of the vein, only a few pyrite grains are located in the vein. There is no chalcopyrite present in this vein see (Fig.5).

Figure 5. The second Quartz vein to brecciating this sample. The vein holds only minor amounts of pyrite which is mainly located along the borders of the vein. No chalcopyrite is present in this vein. The pictures are taken in plane polarized light.

The third quartz vein which brecciate this rock is finer grained then the first two, it mainly carries large grains of (>6000µm) chalcopyrite. Chalcopyrite is mainly located in the centrum of the vein. On the borders of the vein there are some pyrite grains. This vein cuts the previous two quartz generations, see (Fig.6).

quartz

Figure 6. Left: Shown here is the latest quartz vein that intersects the sample, the quartz is finer grained than the first two vein generations, and it carries more chalcopyrite in the centum of the vein. The left picture is in plane reflected light. Right: Massive chalcopyrite in the centrum of the vein. The brighter spots is small grains of pyrite. The picture to the right is in plane polarized light.

In the SEM 9 Au / electrum grains was identified, they were mainly located in the pyrite but also in the sericite quartz wall- rock. In figure 7 below it is clearly visible that electrum is hosted inside the pyrite. This Electrum has been precipitated at the same stage as the pyrite grain formed. This is probably precipitated drops from the Pyrite grain as it cooled off.

Pyrite Electrum Pyrite Electrum

Electrum

Quartz Electrum Chalcopyrite Chalcopyrite

Figure 7. Sample SOL11005-6. Electrum grains are seen in close proximity to the chalcopyrite inside the pyrite.

SOL11005-8 188.23 188.35 Quartz vein breccia; Au-bearing. This sample was collected because the drill coreassay is Au bearing. Within this assay interval there were two different types of pyrite, the finer brecciated type and the coarser grained (SOL11005-9). It consists of a huge amount of fine-grained pyrite, which is brecciated by quartz, (see fig.8). The quartz which is brecciating this sample is bone-white in colour. This rock slab was scanned in the SEM for the Au, but no Au was observed. Some fine grains of galena were observed as inclusions in the pyrite. The quartz and pyrite is sheared or mylonitized.

Quartz

Pyrite

Figure 8. SEM from Sample SOL11005-8 picture BSE fine-grained massive pyrite brecciated by quartz. The bright spots are galena grains.

SOL11005-9 188.79 188.89 Quarts vein breccia; Au-bearing. This is sampled in the same analytical interval as the SOL11005-8 sample, and holds coarser grained pyrite than SOL11005-8 sample. The assay interval is Au-bearing and was therefore scanned in the SEM to see any differences between the SOL11005-8 & 9. The result of the SEM study resulted in seven Au-bearing samples that have been observed, where six of the Au grains occured as electrum in pyrite and one as native Au in the quartz. This relation is seen in (Fig.9). Galena is also present in the proximity to where the electrum was observed not seen in this spots.

Quartz Quartz

Pyrite Electrum Au

Quartz Pyrite Quartz

Figure 9. The upper left picture is a zoomed picture of the bottom left, it shows how the quartz finely have brecciated the coarser grained pyrite. Electrum is also seen in this picture, and occurs in pyrite that is situated along the border of a quartz vein. The upper right picture is in BSE and is a zoomed in picture of the bottom right one. The Au is seen as a free grain inside the quartz. All pictures are BSE images.

SOL11005-11 207.45-207.60 Quartz and sericite altered granite; Au-bearing The wall rock is fine-grained and is consists of ~ 50 % quartz and equal amount of sericite (Fig. 10), but there are also some grains of apatite and xenotime found during the SEM analysis.

Figure 10. Sample SOL11005-11. The left picture is in plane plarized light, the right is in cross polarized light. The content of quartz and sericite is aproxemately 50% to 50%. The foliation of the rock can be seen in the figure.

In the SEM, 18 Au containing grains were located along chalcopyrite filed factures in pyrite or in close proximity to these chalcopyrite veins. Bi and Ag rich galena is often found associated with the electrum, see fig 11.

Pyrite BiAgPbS BiAgS

Electrum Chalcopyrite

BiAgS

Figure 11. Sample SOL11005-11 in BSE. Textural relation for electrum and chalcopyrite in pyrite, the chalcopyrite brecciates this pyrite grain and carries with it the electrum. Here Bi, Ag and Pb are also seen in the same generation. This is seen in the upper right part of the chalcopyrite vein were they coexisting. The grains of BiAgS in the pyrite is probably from this same event but have propagated along fine fractures in to the pyrite.

The thin section is strongly mineralized by pyrite and chalcopyrite with big pyrite grains up to 1mm, se (Fig. 12). The whole section has been brecciated by quartz and chalcopyrite as a main ingredient in this brecciating event. The brecciating of pyrite is obvious. This breccia can easily be observed in the figure below. The bismuth Ag and the lead are deposited as free grains inside the chalcopyrite veins.

Figure 12. Sample SOL11005-11 in BSE. The pyrite is being brecciated by chalcopyrite, the brighter white grains in the fractures and in pyrite grains are BiAg- Galena. The mossy bright is chalcopyrite, dark grey is the Pyrite and the black is Quartz.

Some of the pyrite grains in this sample show a zonation as seen in (Fig.13). There are some darker areas of lower density. This might represent an older core or the crystal that has been exposed to leaching.

Pyrite

Chalcopyrite Quartz

Figure 13. Sample SOL11005-11 in BSE. Pyrite and chalcopyrite in quartz, the chalcopyrite is located along fractures in the pyrite. The pyrite is showing a zonation in density. The darker areas of lower desity and might indicate an older crystal och a leaching stage. SOL11005-12 213.5-213.7 Sericite Altered Quartz; Au-bearing The thin section of sample SOL11005-12 is from an Au-bearing interval. The wall rock has a strong foliation, is fine- grained and consists of ~ 80% sericite and 20% of quartz. Its foliation is cut by a quartz vein of 8 - 10 mm in width. This vein is sheeted and consists of three veins within the same vein. There are two vein sets that have coarse- grained quartz of ~ 200 µm. The first vein has up to 50% pyrite and only minor amount of chalcopyrite. The pyrite is between 100 and 600 µm and euhedral, in this pyrite generation electrum grains was observed, see Figure 14. The second vein type is also coarse-grained and holds less sulphide in it. The sulphide content is less than 5%. Two third of is chalcopyrite, and one third is pyrite. The pyrite is 100 - 900 µm in size, and the chalcopyrite 40 - 500 µm. The third vein consists of fine-grained quartz and holds only pyrite; all pyrite grains are smaller than 100 µm and euhedral. No Au was observed.

In the boundary between the coarser quartz type and the finer grained quartz there are two pyrite grains that hold some fine free Au grains, which are 3 - 20 µm large.

Pyrite

Pyrite Chalcopyrite

Electrum

Galena Electrum Chalcopyrite

Electrum

Figure 14. Pyrite grain in quartz. Five Electrum grains are shown. There is also chalcopyrite in close proximity to electrum. Bismthinite-rich galena is also represented. Picture is taken in reflected light.

The electrum is located as free grains and along fracture planes inside the pyrite. Two of the electrum grains occur along fracture planes inside the chalcopyrite. This Au-bearing generation of pyrite seems to be bounded to the coarser type of quartz vein which are larger than 200 µm. The SEM scan for Au found 15 grains which contained Au. The electrum grains are mostly located in the pyrite as free inclusions (figure 15 below). One electrum grain was also observed in the quartz sericite wall rock.

Electrum Pyrite Pyrite

Electrum Electrum Electrum Electrum Electrum Chalcopyrite Bi Galena

Figure 15. BSE image of the SOL11005-12 sample. The relations of the electrum, chalcopyrite and galena inside pyrite can be seen.

The electrum bearing pyrite in this case is zoned as seen in (Fig. 16). The core which holds the electrum has a lower density than the surrounding pyrite. This might indicate an older pyrite core that has been rimed by newer pyrite, but no clear differences could be seen from analyses chemistry.

Figure 16. BSE images of sample SOL11005-12. The zonation of the electrum bearing pyrite is shown. The core has a lower density than the surrounding rim.

SOL11005-13 215.0-215.1 Sericite Altered Granite; Au-bearing The wall rock is very fine-grained and strongly foliated. This sample consists of 90% sericite, 8% quartz and 2% opaque hematite and is cut by a 10 mm wide quartz vein. This vein consists of two different generations of quartz. The first quartz vein is characterized by coarse-grained quartz with size variation of 200 - 500 µm and holds pyrite grains. The coarser vein contains 30% of pyrite with euhedral grains that range between 40 and 1800 µm in size. In addition, there can be chalcopyrite as well which exists as free grain between pyrite grains or as inclusions within the pyrite. The chalcopyrite varies between 30 and 1000 µm and has an overall content which is below 1%. In the following BSE image (Fig. 17) one can see electrum as inclusions in the pyrite, there are also inclusions of chalcopyrite present. The SEM scan resulted in 23 grains that contained Au throughout this sample. Some of these grains can be found in (Fig 17&19).

Quartz Quartz Pyrite

Pyrite

Chalcopyrite Electrum Electrum

Figure 17. BSE images of sample SOL11005-13 with electrum and chalcopyrite grains in pyrite. Right is a zoomed in picture of the electrum grain.

The second quartz vein is very fine-grained. In this fine-grained quartz there are mostly chalcopyrite and only minor pyrite present. The chalcopyrite is typically 100 - 1500µm in size. This fine-grained quartz seems to have brecciated the wall rock and carried with it minor chalcopyrite into the wall rock. The quartz vein shows a slight coarsening sequence towards the centrum of the vein. The pyrite is located along the borders of the zoned vein while the chalcopyrite is deposited in the centrum, see (Fig. 18).

Figure 18. The second quartz vein that reactivates the older coarser grained quartz pyrite vein. The chalcopyrite is located in the centrum of the vein, while the pyrite is along the bottom border. The larger pyrite grains seen in the upper part is from the older coarser grained pyrite rich generation.

In (Fig. 19) the electrum is inside the chalcopyrite, in between the Pyrite grains, of the fine-grained quartz.

Pyrite e Quartz Quartz Chalcopyrite Pyrite

Electrum Chalcopyrite

Figure 19. BSE images of sample SOL11005-13. Electrum is located inside the chalcopyrite, the right picture is a zoomed in picture. This is from the late fine-grained quartz generation.

SOL11005-16 240-241 Cataclastic Granite; Au-bearing This sample is very fine-grained and has a clear foliation. The foliation is indicated by the sericite, which lies in fine bands through the whole sample. The wall rock consists of ~ 78% quartz, 20% sericite and 2% opaque hematite. The whole sample is reddish and is probably caused by the staining from the hematite. The foliation is cut by two different veins; one chlorite vein and one calcite vein, both veins are ~ 1 mm wide. The chlorite veins occurred along old fractures.

SOL12001-01 121.20-121.30 Quartz Feldspar Porphyry; (no analyses) The sample has a porphyric texture of large micropertitic K- feldspar and clusters of quartz gains. The K- feldspar often shows inclusions of smaller quartz grains. The clasts of quartz are undulautory and fine-grained, together these fine-grained quartz forms larger clasts. In combination with the micropertitic K- feldspar gives rise to the porphyric texture, seen in the sample. The larger phenochrysts consists mainly of micropertitic orthoclase and a few clasts shows weakly tartan twining as seen in figure 20. The K- feldspar in this sample is roughly 10%. These phenochrysts are up to 1 – 2 mm as seen in (Fig. 21).

The matrix of the sample is very fine-grained and consists of quartz, sericite, and minor calcite. The matrix of the sample is 95% quartz and varies in size from very fine-grained to fine-grained. The fine-grained quartz in the matrix forms a foliation that goes through the sample. The matrix also holds ~5% sericite and is bound to the foliation of the matrix (Fig. 20).

Figure 20. Phenocrysts of micropertitic K-feldspar, ~ 2 mm in crosection. The phenorysts holds inclusions of quartz.T sourounding matrix consists of fine-grained quartz and sericite. The foliation bends around the phenorysts. The image shows cross polaized light.

Figure 21. Large phenocrysts of quartz cluster and K-feldspar, with its characteristic tartan twining. The matrix is very fine-grained and consists mainly of quartz and minor of sericite. The foliation here is indicated by the Sericite. The image shows cross polaized light. SOL12001-2 151.57-151.70 Conglomeratic Shear Breccia; Not Au-bearing The sample is from the lithological unit ‘conglomeratic shear breccia’. The sample has a strong foliation and very fine-grained, (Fig. 22). It consists of ~ 70%quartz, 15% chlorite 10% sericite and 5 % opaque hematite.

Figure 22. Microscopy images of sample 12001-2. The rock sample is strongly foliated, and very fine-grained. The chlorite sericite and the hematite lie in the bands and give rise to foliation. The left picture is in plane polarized light, the right is in cross polarized light

SOL12001-5 253.17-253.37 Sericite Quartz Altered Granite; Au-bearing This thin section is from an Au-bearing interval. The wall rock consists of 65% sericte and 35% quartz. This sample is cut by two quartz veins, which carry sulphides, pyrite and chalcopyrite occur in both veins. The coarse-grained pyrite was carried into the wall rock with the first quartz, and was at a later stage brecciated by the quartz- chalcopyrite. The picture below shows the chalcopyrite which has carried the bismunite and Au as electrum (Figure 23).

Bismutinite Pyrite

Electrum

Chalcopyrite

Figure 23. BSE image of the sample SOL12001-5 where the chalcopyrite brings bismuthinite and electrum in to the pyrite. SOL12001-7 257.19-257.34 Quartz Vein Breccia; Au-bearing This thin section consists of large-grained pyrite, quartz and also minor amounts of chalcopyrite. The pyrite in this sample is carried in by the quartz vein. The pyrites are coarse-grained and often holds electrum grains. When scanning the section for Au in the SEM, some 68 Au-bearing grains were located. In many cases bismuthinite occurs together with the electrum and is illustrated in the BSE image Fig. 24. The coarse-grained pyrite in this sample is cut by one later vein that brings with it fractured pyrite as seen in Fig. 25.

Electrum Electrum

BiAgPbS

Figure 24. BSE image of sample SOL12001-7. Electrum grains in pyrite. Bi and Ag rich galena is also present. The smaller grains are all BiAgPbS.

Pyrite

Quartz

Figure 25. BSE image of a late pyrite filled quartz vein. The pyrite in this quartz vein are broken pieces probably from the surrounding pyrite when the quartz vein intruded through the surrounding pyrite.

SOL12001-9 260.28-260.31 Quartz Vein Breccia; Au-bearing It is basically a quartz pyrite breccia that is brecciated a second time, which is similar to the SOL11005-8 sample. The first quartz has brecciated the pyrite and fractured the pyrite into smaller grains. This has later been re-brecciated by a second bone-white quartz phase. This second brecciating stage seem not to have carried any pyrite with it. No free Au has been observed in this sample.

SOL08-01 47.34-47.58 Metaphyllite; not Au-bearing The sample is from the lithological unit metaphyllite. This is a vein breccia and no free pieces from the wall rock are visible in the sample. The whole sample consists of ~ 40% Quartz, 29% Fluorite, 20% Calcite and 1% Hematite is present.

The euhedral fluorite crystals are surrounded by quartz that has grown radiotory from the fluorite crystals, face controlled growth. Both the quartz and the fluorite seem to have grown in open space. The fluorite crystals are large and euhedral, in this fluorite there are quartz inside them, indicating that both crystalized at the same time, see (Fig. 26). The fluorite is giving the rock a nice pink colour. But there is also one later green fluorite quartz vein that cut this pink fluorite generation, the green fluorite is often larger. These green fluorite crystals are in some cases up to 5 mm in diameter.

Figure 26. Microscopic images of sample SOL08-1. The face controlled growth texture of the quartz is visible as nice rims on the quartz grains, the large fluorite lies in bedded in the quartz (isotropic). The large crystals of the fluorite and the zonation of the quartz indicating free space growth. The left picture is in plane polarized and the right in cross polarized light. SOL08-02 70.89-70.93 Metaphyllite; not Au-bearing The sample is strongly brecciated by quartz veins, and the brecciated wall rock mainly consists of ~ 90 % quartz, 6% opaque hematite and 4% sericite. The old brecciated wall rock is very fine-grained, see (Fig. 27). The cutting quartz veins are bone-white type and fine-grained. Close to the border of this sample there is a large quartz vein, the quartz crystals in this vein is like previous sample face controlled growth, indicating growth in free space.

Figure 27. Microscopic images of sample SOL08-02. The foliation is easily seen. And the fine-grained bone- white quartz vein cuts through the sample. The left picture is in plane polarized light and the right is in cross polarized light. SOL08-03 85.02-85.14 Epithermal quartz breccia; not Au-bearing This epithermal quartz breccia is brecciated by quartz and fluorite. Clasts of the wall rock are seen in the sample, they consist of ~ 50% chlorite, 40% quartz and 10% hematite. These clasts are slightly rounded and seem to be dissolved by the brecciating fluid, see (Fig. 28).The brecciating veins consist of quartz and fluorite. The fluorite and quartz is very fine- to fine-grained and, they both show a euhedral crystal structure, the quartz has face controlled growth texture. This indicates that the brecciating vein remained open and allowed the crystals to grow in open space. The quartz in this system is typically bone-white in its colour. The main brecciating quartz and fluorite is cutting an earlier quartz and pyrite vein that holds fine to medium-grained pyrite. This pyrite bearing quartz is greasy greyish in colour. The pyrite in these veins is fractured and brecciated by the quartz from the fluorite quartz generation. No Au, bismuthinite or chalcopyrite was observed in the pyrite.

Figure 28. Microscopic images of sample SOL08-03. Here an old clast of the wall rock is seen. It is strongly "dissolved" on the right side of the clast. Fluorite and large quartz crystals are recognizable. The left picture is in plane polarized light and the right is in cross polarized light.

SOL08-04 87.61-87.80 Epithermal Quartz Breccia; Au-bearing This sample consists of ~ 70 % quartz, 25 % fluorite and 5% sericite. The brecciating veins in this sample have been reactivated many times and deposited rims in the veins. These rims often consist of quartz, however some pulses of pure fluorite can be seen, both the quartz and the fluorite shows nice euhedral crystals, indicating free space growth, see (Fig.29).

Figure 29. Microscopic images Sample SOL08-04. Fluorite grain surrounded by coarse quartz crystals. Left picture is in plane polarized light and the right picture is in cross polarized light.

Samples location. In the following two pictures all of the samples in this study are here shown in their position in the lithological sequence.

Figure 30. In this cross section of the Solvik mineralization the samples are illustrated were they are located in the drill core. The samples illustrated here is SOL11004 1, SOL11005 1-17 and SOL12001 1-9. This cross section is fro(Höglund, 2012)

Figure 31. In this cross section of the Solvik mineralization the samples are illustrated were they are located in the drill core. The samples illustrated here is SOL08 01-04. This cross section is from(Höglund, 2012)

Spot positions for LA-ICP-MS

Figure 32. BSE image of sample SOL11005-6 and the spots 22-26 of pyrite and 84 of the Au grains.

Figure 33. BSE image of sample SOL11005-11 and the spots 29, 31-34 of pyrite.

Figure 34. BSE image of sample SOL11005-11 and the spots 36-41 of pyrite

Figure 35. BSE image of SOL11005-12 and the spots 50 and 53 of pyrite and 93-96 of the Au grains.

Figure 36. Reflected light image of sample SOL11005-13 of the spots 56-60 of the pyrite.

Figure 37. Reflected light image of sample SOL11005-13 of the spots 61, 62 and 64 of the pyrite and 97 of the Au grain.

Figure 38. Reflected light image of sample SOL12001-5 spot 1 of the pyrite analyses 66 and 67.

Figure 39. Reflected light image of sample SOL12001-5 spot 2 of the pyrite analyses 68-70 and 98 of the Au grain analysis.

Table 1. LA-ICP-MS analytical result of content in pyrite in ppm. The spot 22-26 are from SOL11005-6 site 1, 29-35 are from SOL11005-11 site 1, spot 36-41 are from SOL11005-11 site 2, spot 50-55 are from SOL11005-12 site 1. Spot 56-60 are from SOL11005-13 site 1, 61-65 are from SOL11005-13 site 2, spot 66-67 are from SOL12001-5 site 1 and spot 68-70 are from SOL12001-5 spot 2. Elements in the blue rows are normalized against the Mass 1 and elements in green against nistsrm610.

Element / Spot 22 23 24 25 26 29 31 32 33 34 36 37 38 39 40 41 50 447186. 435469. 491176. 359882. 495048. 528996. 516341. 521374. 524848. 523181. 547402. 535328. 553021. 544972. 547933. 545918. 524971. S34 7 7 9 4 5 8 9 0 8 3 7 4 2 7 9 3 8 Ti47 1.1 0.7 1.5 0.7 3.1 1.6 1.2 1.1 1.4 1.5 2.7 1.3 2.0 2.2 2.3 1.9 1.5 369080. 369923. 396402. 295412. 385641. 445517. 410530. 460583. 450505. 442723. 424238. 426910. 439797. 443379. 439980. 453406. 436348. Fe57 4 6 7 4 7 5 7 6 2 4 1 3 9 2 4 7 1 Co59 220.1 128.7 167.3 36.9 270.0 6.7 35.4 5.1 0.7 2.0 5.2 118.3 10.8 37.9 16.0 4.2 42.4 Ni60 175.5 5.5 6.9 4.3 24.8 0.8 33.6 8.0 0.3 0.8 6.4 8.6 6.2 43.2 7.9 13.2 55.3 Cu63 617.3 2174.8 1947.3 118.4 4967.2 0.5 3.1 0.5 0.6 0.4 6.4 1.9 1.3 6.8 2.0 1269.4 0.5 Zn66 2.0 0.6 0.0 0.0 6.4 0.5 0.0 0.4 0.0 0.5 13.0 0.0 1.6 0.0 0.5 1.7 0.2 Ga69 0.1 0.1 0.2 0.0 0.0 0.3 0.0 0.0 0.1 0.0 0.0 0.0 0.0 0.1 0.1 0.0 0.0 As75 6.2 4.2 4.5 3.4 8.3 0.6 1.5 1.0 7.6 7.9 1.0 1.0 1.0 1.1 1.1 1.1 8.3 Se77 19.7 15.2 16.4 30.3 36.4 3.6 5.0 1.8 3.1 4.6 2.1 4.2 0.9 2.3 0.7 0.0 5.3 167990. 190896. 106330. 337073. 113057. Mo95 8 0 9 1 8 24595.8 43189.9 17972.7 24629.6 33968.2 8420.2 33489.4 4946.4 11364.3 3485.4 0.0 38491.3 Ag107 14756.2 946.3 2586.9 7009.2 1409.7 867.8 29135.3 51.3 0.0 106.6 19767.2 3915.4 2200.1 188.4 8464.6 651.7 71.4 Cd111 0.7 0.0 0.2 0.1 0.8 0.1 1.8 0.0 0.0 0.1 0.5 0.0 0.0 0.5 1.0 0.0 0.3 Sn118 0.0 0.0 0.0 0.1 0.2 0.1 0.0 0.0 0.1 0.0 0.1 0.0 0.1 0.1 0.1 0.1 0.0 Sb121 0.7 0.3 0.6 0.3 1.3 0.1 0.8 0.0 0.0 0.0 0.5 0.0 0.0 0.1 0.0 0.0 0.0 Te125 9.0 2.5 5.0 5.5 3.9 0.0 2.1 0.2 1.6 2.3 0.9 1.9 0.3 0.0 0.7 0.0 1.2 Au197 0.1 0.0 0.1 0.1 0.1 0.0 0.2 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Hg202 0.3 0.2 0.2 0.2 0.2 0.1 0.1 0.2 0.1 0.1 0.1 0.1 0.0 0.2 0.1 0.1 0.1 Pb208 60.6 12.6 72.0 329.9 47.5 2.9 480.5 0.0 0.1 0.1 107.6 109.8 3.9 1.9 62.1 0.5 0.4 Bi209 66.8 16.8 99.2 82.9 88.2 3.3 235.6 0.0 0.0 0.2 24.4 109.8 5.8 1.2 39.9 0.6 1.2 U238 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

Element / Spot 53 56 57 58 59 60 61 62 63 64 65 66 67 68 69 70

S34 491348.0 513066.3 493402.8 501080.3 482145.6 503691.5 516185.0 521204.3 514708.4 520185.5 510258.9 507980.7 91425.3 521411.1 522483.8 511300.6

Ti47 1.0 1.2 1.2 2.2 1.6 1.6 3.0 3.9 2.0 4.2 4.4 2.8 0.5 2.1 2.0 2.4

Fe57 401188.7 405846.1 424068.5 449559.4 427632.0 410449.7 440556.8 448109.3 444541.5 443392.7 461944.2 432752.2 74349.4 431001.0 411243.6 451315.9

Co59 32.0 879.1 38.4 288.4 1163.3 306.1 138.2 7.0 394.3 668.9 788.5 218.8 0.0 36.6 147.3 33.7

Ni60 132.0 0.0 0.5 2.8 43.4 20.7 5.6 0.6 24.5 7.8 9.1 78.8 0.0 1004.9 690.9 1147.3

Cu63 2.0 7.1 3.8 36.6 309.9 2341.2 108.2 356.6 2439.1 68.5 27.9 0.8 3.2 2.1 145.6 0.1

Zn66 0.1 1.3 0.5 0.0 26.1 0.6 86.7 0.2 11.9 0.0 0.5 0.4 94.6 1.2 0.0 16.5

Ga69 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.2 0.1 0.1 0.2 0.1 0.0 0.3 0.0 0.0

As75 7.1 63.2 2.5 20.2 93.3 17.7 4.4 1.8 12.0 9.3 10.4 2.6 0.6 1.2 1.1 0.9

Se77 11.1 9.5 8.9 9.5 12.9 13.2 11.0 4.3 6.8 10.2 9.4 15.2 7.8 8.7 11.1 7.6

Mo95 106651.9 80116.6 79084.7 48976.0 87286.1 83416.2 40934.4 12310.0 36937.6 27012.2 24402.9 58943.9 28049.5 45535.5 58142.2 36126.1

Ag107 611.8 1.0 3308.7 22.4 696.2 191.3 1857.1 18114.9 792.9 7015.2 1928.2 0.0 806054.2 960.8 6864.8 45.2

Cd111 1.1 0.0 0.4 0.5 0.1 0.4 7.9 0.2 1.0 1.2 0.8 0.0 2.1 0.0 0.4 0.1

Sn118 0.1 0.0 0.1 0.1 0.1 0.0 0.2 0.0 0.1 0.1 0.0 0.0 0.1 0.2 0.2 0.4

Sb121 0.0 0.0 0.0 0.0 0.6 0.1 0.8 0.1 0.6 0.4 0.5 0.1 0.0 0.0 0.1 0.0

Te125 0.3 1.7 0.4 3.0 1.0 3.3 0.7 0.3 2.6 3.7 5.0 1.8 0.0 1.3 5.3 1.0

Au197 0.0 0.0 0.0 0.0 0.0 0.1 0.2 0.1 0.1 0.2 0.1 0.0 0.0 0.0 97.2 0.0

Hg202 0.3 0.1 0.1 0.1 0.1 0.3 0.1 0.1 0.0 0.1 0.2 0.0 0.0 0.1 0.7 0.1

Pb208 4.3 0.3 45.6 2.0 170.9 0.3 26.5 28.6 67.8 323.3 243.0 1.0 4.0 13.0 28.1 0.0

Bi209 8.9 0.0 31.9 4.2 166.1 12.9 89.8 55.3 73.9 1229.2 364.5 1.5 6.8 19.6 58.9 0.3

U238 0.0 0.2 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

Table 2. LA-ICP-MS analytical result of content in Au grains of pyrite in ppm. The spot 84 are from SOL11005-6 site 1, spot 93-96 are from SOL11005-12 site 1, spot 97 are from SOL11005-13 are from site 2, spot 98 are from SOL11005-13 from site 1 and 99 from SOL12001-5 site 1. Elements in blue are normalized against the mass 1 and Pt in red are normalized against the Po-725.

Element/ Spot 84 93 94 95 96 97 98 99 Cu63 1123.2 875.4 65.1 82610.7 966488.3 46.7 949059.5 415710.0 Se77 92.8 882.1 96.1 397.8 292.9 19.0 20999.7 0.0 Ag107 695988.0 325803.7 549658.0 264695.9 11828.5 507681.4 5150.0 277836.1 Cd111 2.1 532.2 0.0 29.5 0.0 0.0 577.8 0.0 Sb121 11.8 54.3 4.3 9.6 31.9 0.0 66.0 9.7 Te125 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 Pt195 0.7 0.0 0.0 0.0 4.3 1.0 25.2 2.6 Au197 300280.0 383773.2 447007.0 297052.7 3318.4 490904.8 701.0 305190.0 Hg202 781.1 815.9 758.4 773.8 68.2 1241.7 874.5 821.6 Pb208 834.6 95439.0 853.2 190674.5 5516.4 34.0 5479.2 83.2 Bi209 885.8 191824.2 1557.9 163755.5 12451.2 71.4 17067.1 346.7