Bergvesenet Rapportarkivet2001

Bergvesenet 5Ie Postboks3021, N-744I Trondheim Rapportarkivet2001 Bergvesenet rapport nr Intern Joumal nr Gammelt interntrapp. nr. Rapportlokalisering Gradering BV BV 3083 Kasse34 Trondheim

Kommer fra ..arkiv Ekstem rapport nr Oversendt fra Fortrolig pga Fortrolig fra dato:

N- 8I - 2 Tverrfjellet

Tittel Diamond drilling program 1982with a review of the geologi of the Finnmark-district Text and diamond drill logs. Finnmark project (N-81-2).

Forfatter Dato Àr Bedrift Priesmann, Frank-Dieter 1982 Folldal Verk AJS Amoco Norway Oil Company

Kornrnune Fylke Bergdistrikt 1: 50 000 kartblad 1: 250 000 kartblad Karasjok Finnmark Troms og Finnmark 20334 Karasjok

Fagområde Dokumenttype Forekomster Boring Rapport Madijavri Daktejåkka Sammalcåkka Gætkevarri Aslat Pier Varri Dabmutsuokkadas Råstoffgruppe Råstofftype Gæssaroavvi Malm/metall , Au Cu

Sammendrag / innholdsfortegnelse Borprofilene finnes på By 3084.

I duplikat. Amoco Norway Oil Company P. 0. Box 2494 Solli Oslo 2 Norway

go..recr

b 1-cis FINNMARKPROJECT(N-81-2) FOLLDALVERKA/S- AMOCONORWAYOILCOMPANY DIAMONDDRILLINGPROGRAMME 19 8 2

with a review of the geology of the Finnmark-distriel

By FRANK-DIETER PRIESEMANN 1. INTRODUCTION.

The Karasjok-programme is located i8 Finnmark fylke, Northern Norway, centered at 69°20' N and 25 15' E. (Fig. 1). The tract of land is called Finnmarks-vidda, an area of about 14.000 km2, which means the southgoing sheety extension of the normal northern norwegian coaststate into the "Lappi" - district of Finland. It represents the norwegian part of the north scandinavian, respectivly artic, peneplain.

The project-area lies in the eastern part of this region in the nearea, west of Karasjok, a town located at the Karasjåkka (Karasjok-river) 18 km west from Ihe Finnish-border. The prospected area is about rRctangular shaped with a N-S extension and encloses aboul 1000 km'. It encludes the main part of the so called "Karasjok-feltet" (WENNERWIRTA, 1968).

The landscape of this district is formed by extense glacial erosion and shows therefore a very soft relif. It predominates knolls or smouth mountain ridges surrounded by flat u-shaped valleys, which are normally covered by svamps. The general heights differes between 400 and 250 m, with an average of about 300 m. The main elevation is the Iskuras mountain belt - made up out of quartzite - with 642 m a.s.1.. It is outside the work area.

The drainage is undertaken by the main rivers: Karasjåkka, Jesjåkka and Bavtajåkka. They are running mostly either in a strict N-S or E-W direction with rectangular bands in between. They are following and pointing out by that way the prominent tectonic lineaments. The riverbeds are wide - 40 - 170 m - and u-shaped and filled with fluviatile and glacial material. The older river terrasses are in general 6 to 7 m above the nowadays run. Due to the very little fall - Kara- sjåkka: 90 m on a distance of 60 km (Baeivasgiedde: 218 m, Karasjok church: 125 m) - the rivers are even in the summer- time navigable by engined riverboats.

There exists a typical vegetation of the higher latitudes. It comprises of cripple - birches, juniper, dwarf - birches and small willow-trees and bushes. Furthermore there are existing pine-trees, but they are restricted to the river- valleys. The ground is covered by gras, several kinds of berries (e.g. rubus chamaemorus, arctostaphylos alpina, vaccinium uliginosum, vaccinium vitis-idea) mosses and different kinds of lichen (cladonia mitis, peltigera aphthosa, cladonia pyxidata). At some locations there were found flowers of viscarla alpina which are typical indicators for Mg-rich rocks. (see also REITAN, 1963). rkenes %A0 Attc Trtm I innmar Pro ect Ga'P

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2.1 THE "ØST-FINNMARKS GRUNNFJELL".

Only very little information are available about the geology and lithostratigraphic of the precambrian base- ment south of Varangerfjord. That is why most of the works are carried out by geologists of Sydvaranger A/S, here under the leadership of J.A.W. Bugge (BJØRLYKKE, 1982). However some notes and within that a general stratigraphy are found in OFTEDAHL (1974) and BJØRLYKKE (1982). After OFTEDAHL (1974) the precambrian rockgroup is divided into three main groups. (Fig. 3).

Ære og omtrentlig StrMig rali alder i mill. år

Gjennomsettende diabasganger

Foldning og metarnorfose

Petsamo-gruppen. 1). Underordnet: Lag av glimmerskifer, kalk, Katelider 2. Skogfoss grønnstein ca. 1930 tuffer og sure lavaer. I tilslutrung: Basisk gabbro og peridotitt. 1. Neverskrukk-konglomeratet: Polymikt baselkg1.

jennomsetten genger av granitt og pegmatnt.

2500 Sterk foldning og metamorlose med dannelse ev feks, den anatek- tiske Neiden granitt.

Norvego- Elj•rnevannagruppen. samider 4. Ørnevann meta-vulkanitter: Biotitt-hornblende-gneiser (vesentlig meta-andesitt og metadacitt). 3. Sydvaranger jernmelm (Mt kvartsrandrnalm). ca. 2500 2. Bjernevann gneis: Mest kvartsitter og glimmerskifre, tynne rhyo- litthorisonter. 1. Baernevenn konglomerat: Polym. basalkgi. 1): Jarflord-komplekeet Pre- Gammelt gneisunderlag i Sydvaranger med granitttske gneiser, mig- samider matitter, glimrner og granatgnemer, akinzigitto og arntibolitt. ca. 2800 7 Fra Polmak vestover langs Tana: Granulittgneiser.

1) Forslag tit nye stratigratuke navn

Fig. 3: The precambrian of the east-Finnamrk (OFTEDAHL, 1974).

There are from the basis upwards the "Jarfjord-komplexset" (2800 m-Y), which consists of granitic gneises and migmatites and-finds its pendant in the archean gneisdome on the Finnmarks-vidda (see 2.2), than the "Bjørnevanns-gruppe" (2600 m.y.) supposely a geosyncline series and at least, with a clear discordance to the underlying group, the "Petsamo- gruppe" (1800 m.y.), a typical geosynchine sedimentation pile. This group startsat its footwall with a basal-conglomerate (Neverskrukk-conglomeratet), what is mixed with arkosic sandstones. Upon that rests a sequence of basic volcanics ("Skogs- foss grønnstein"), made up out of submarine - pillowed - basic volcanics,now metamorphosed to greena_ones and or amplibolites and not further differentiated ultrabasic volcanics with inter- - 5 -

bedded graphite slates and - schists. Further up there are following more felsic volcanics and, in a greater amount, metasediments like micaschists and carbonates.

The series as its whole could be related to a rift - volcanisme (BJØRLYKKE, 1982). There are some indications - age of formation and lithostratigraphie - what leads to a correlation of this group with the volcanic-sedimentary sequence of the Finnmarks-vidda (OFTEDAHL, 1974).

2.1.1 ECONOMIC GEOLOGY.

Connected to the BjØrnevanns-group there is an exhalative - sedimentary iron-ore deposit called "Sydvaranger quartz - banded iron ore". Further informations can be taken from BUGGE (1978).

In the norwegian part of the Petsamo-group no sulfide mineralisation of economic importance has yet been found. Well known is a Ni- Cu - mine (Petsamo) on the russian side, not far away from the norwegian border. This pentlandite/chalcopyrite appearence is connected to serpentinized peridotites and metagabbros. On the norwegian side there have been re- portet boulders of equivalent mineral compositionin glacial residues from the Pasvik-area. Glacial transport direction and trace-element analysis of these heavy sulfide boulders point to an own mineralisation supposely located in this area. In the last few years prospecting activities were carried out by Sulfidmalm A/S. They included diamond-drilling. In fact of the negative results these activities were stopped in the middle of 1982.

2.2 GEOLOGY OF THE FINNMARKS-VIDDA.

The geological structure of the Finnmarks-vidda is from the first point of view a very simple one. (Fig. 4). In central position there is found a tongue-shaped gneisdome of archean age (2800 m.y). With a mainly N - S elongation this body covers an area of about 5000 km2. Its northern hinge is located in the nearea of Skoganvarre. This gneisdome is surrounded by a volcanic-sedimentary series metamorphosed in lower greenschist - to amplibolite-facies. Its horizons are running more are less N - S and by that parallel to the gne,isborders.This unit shows lithological differences between its eastern and western part, what efforts a discrimi- nation in the West-Vidda, with the westerly greenstone-belt and the Karasjok-group (east side). Their separate discrip- tion will be given later.

The total age of this rockgroup is nowadays in discussion. Former age-determinations pointed out a karelish (1800 m.y) formation. Never works carried out on samples of adequate

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4: 1:ta,„4 fied map or ?inLmarksvi,:.:a - 7 - material from northern Finland lead to a possibly archean age (BJØRLYKKE, 1982).

Both, gneisdome and volcanic sedimentary pile are intructed by gabbros - the majority of them is found in the Karasjok-greenstone - belt-, granites and dolerite - dykes.

2.2.1 THE CENTRAL GNEISDOME.

This basal gneis varies from granitic to dioritic in compostion (BJØRLYKKE, 1982) - granodioritic to quartzdioritic (SKÅLVOLL, 1972) - and shows by that locally enrichments of mica and garnets, what leads to a mica - or garnet gneis. It predominates a medium grain-size and a granoblastic texture. Pegmatitic equivalents develops as small (dm) "veins" and or certain bodies with typical mikrographic textures between quartz and feldspar. Enrichments of large biotite-plates are common in these zones.

Inclusions of unfamiliar material as amphibolites, hornblende- gneises and micagneisses are reported from WENNERVIRTA (1969). HOLMSEN et al (1957) describe micaschists, greenschists, quartzites and talkschists, the common types of rocks in the westerly greenstone-belt...

The contacts between the gneisdome and the onlying meta- sedimentdry formation are as well concordant as discordant.

2.2.2 THE KARASJOK-GROUP.

The stratigraphie of the Karasjok-group given by WENNERVIRTA (1968) and SKÅLVOLL (1972) basis essentially on one good outcrop, called the "Cag'gejåkka nØkkelområde", which is located about 10 km south of Skoganvarre. After that the Karasjok-group consists of two, supposely three groups: an arenaceous basis, the following volcanic-sedimentary pile and a more sedimentary completition part (Fig. 5). The last two ones are described as the Karasjok greenstone-group. It builds the Karasjok greenstone-belt,(BJØRLYKKE (1982)),a mainly N - S trending formation, which runs from Porsanger- fjorden in the north to the southern corner of the Finnmarks- vidda. From here it continues further into Finland, where it forms the Kittil.å greenstone-complex.

Fig. 5: Strati9raphic of the Karaslok-group

Karasjok greenstone-group amphibolite, hornblendeschist (marbel) meta-picrite (mafic, ultramafic, laves) - 8 -

supposely Karelish Arenaceous basis

(1800 m.y.) - mica schists, metagreywacks, graphiteschists quartzites, metaarenites basalconglomerate Basal gneis-complex arkean (2800 m.y)

The arenaceous basis comprises out of a typical basal conglomerate, which grades upwards into arkosic sandstones and further into pure quartzite. This alignment characterizes an typical clastic evolution of shelt deposition. Upon that follows a more pelitic section made up out of quartz-mica schists, which contain small horizons of metagreywackes and graphite schits.

The contacts between the base - sediments and the onresting volcanic-sedimentary pile appearse to be very sharp with locally obvious brecciation. This let think about tectonic conditions, which are mainly accepted by SKALVOLL (1972) and BJØRLYKKE (1982) - he believes in an overthrusted sequence from the east.

A detailed description of the whole volcanicsedimentary pile or even an idea of the karelish (?) volcanic evolution hasn't been found in any of the publications. Surely, this is why there is a lack of information about the geology based on the very small amount of outcrops.

The greenstoneunit starts at here base with basic and ultrabasic volcanics, which show locally very well preserved pillow - and agglomerate - structures (Njuvcokka). They occure nowadays as more or less massive amphibolites or garnet - amphibolites and greenstonesand can be interpretated as former submarine basalt-flows.They are accompanied by amphibolechlorite schists, supposely tuffaceaus in origin (WENNERVIRTA, 1968). Furthermore SKALVOLL (1972) reports rockmaterial composed of amphibole, chlorite and serpen- tine surely an altered ultrabasic volcanic. Interbedded in this section are some arenaceous layers, described as biotite - bearing metasandstones (BJØRLYKKE, 1982). Furter are associated one or even more horizons of iron-banded quartzites (banded iron-formation) and beds of graphite slates and - schists.

These banded iron-formations are of possibly exhalativ - sedimentary origin and occure in 8 to 15 m big horizons - 9

mostly on top of marked basalt-flows (masses of amphibolites with underlain amphibolite-chlorite), from which they are divided by 5 to 20 cm thick seams of sulfides (composed out of pyrrhotite with minor amounts of pyrite and chalcopyrite). The formations show in general a wide mineralogy. Main components are quartz, carbonate and magnetite. In a lesser degree there appeares garnet, pyroxen, biotite, g runerite and ferric tremolite and in addition hematite and Mn-oxides. By diamond drilling (TRØFTEN, 1957062) there is proved a distinct zoning, both in a horizontal and vertical extension, what is indicated by mostly slowly changes in mineral compostion. Carbonate - facies banded iron-formation occures for example at Njuv- cokka in a higher niveau as the magnetite enriched more quartzite variation. The pure silicate section, very often located at the footwall of the formations, are always overlain by "Skarnstein" (WENNERWIRTA, 1968), supposely the silicate-facies of banded iron-formation.

As a rule the banded iron-formations are capped by graphite- rich pelites.

Higher up in the volcanic-sedimentary sequence there are found greater amounts of quartzites (with and without fuchsite), arkosic sandstones, micaschists and carbonates.

The uppermost part of the Karasjok-group consists mainly out of amphibolites (massive and banded, garnet-bearing or not) and hornblende gneisses, which are interlayered by small horizons of carbonate.

2.2.2.1 ECONOMIC GEOLOGY.

GOLD.

The Karasjok-district has been noted for many years for the occurence of placer gold. Nearly all of the earlier papers available were restricted to these occurences (DAHL, 1891, RENSCH, 1903). A good review of all is given by BJØRLYKKE (1966).

Most of the placer gold prospects are located in the south- west of Karasjok along the Bartajokka and Karasjokka (here only the streak between Baeivasgiedde and Raitejavri). From this areathere are reported both, basic and ultrabasic volcanics, which belong to the bottom part of the Karasjok-group. Connected to are banded iron-formations. Another placer gold area is the Gorzzejåkka-/Anajåkka-field, lying in the far south of Karasjok close to the easterly border to Fin- land. This occurence is arranged - after SKÅLVOLL (1972) - in the completion pile of the Karasjok-group.

There are three different types of placer gold occurences - 10 -

reported by BJØRLYKKE (1966). The first two ones are restricted to the old erosional river terraces, which often lie 6 - 8 m above the present river level. These occurences are described as

preglacial placers which have not been affected by glacial erosion and pregalcial placers which are enclosed in glacial residues.

The third type is represented by postglacial gold concentrations in present river beds. This is only found at the "Sargejok-gullfelt".

The estimated total gold production of the Finnmarks-vidda is of the order of 40 kg. The extracted gold consisted mainly out of small plates of 1/2to 1 mm in diameter. No gold dust has been reported. Besides that there were found some nuggets, with up to 17 g ip weight ("Sargejok-gullfelt")

Native gold has been found by RENSCH (1903) in quartzites and sandstones near Baeivasgiedde and Skiecamjokka. From Finland (Lappi-district) there have been reported gold- bearing pyrrhotite and siderite veins.

At last should be mentioned, that the highest gold-concentration of more than 2 g/m3 was found in the "Sargejok - gullfelt". This is located at the Sargejokka south of Baei- vasgiedde.

IRION-ORE.

In 1956/57 a prospecting programme on magnetic iron-ore connected with the banded iron-formation was carried out at Soulomaras, Njuovcåkka and Gaessagielas. These activities included as well geophysical surveys as diamond-drilling. On the best looking mineralisation south of Njuovcokka there were drilled altogether 12 holes with a total meterage of 1100 m. The iron-content ranged between 22 - 27 % by a thickness of 10 to 15 m. No economic iron - enrichments have been prooved (TRØFTEN, 1957/62, WENNERVIRTA, 1968).

SULFIDES.

A chalcopyrite occurence, bearing some gold, in a gneis of dioritic composition was discovered by Sydvaranger A/S at Raitivarri in 1966. The exploration programme lasted for several years (a member of 10 were named by local persons).

Sulfidmalm A/S concentrated their activities on Cu - Ni - occurences bounded to ultramatic volcanics, the same type of deposite they were looking for in the Pasvik-area (2.1.1). These activities were dropt in 1976. Several chalcopyrite, pyrite, pyrrhotite mineralisations are described from metamorphosed mainly basic volcanics of the Caskias-Porsanger group, which is the northern lithological eqUivalence of the volcanic-sedimentary section of the Karasjok-group. The occurences are divided into a stratiform type with a domination of pyrrhotite and a Cu-enriched brecciated vein-type. The stratabouad.sedimentary deposits consists of alternating bands of quartzitic and schistose rockmaterial with sulfide-rich seams. This section can be followed on the base of a distinct rusty colouring over a distance of several hundrets of meters along the strike. Its thickness vary from 10 to 20 m. The main sulfides reported are pyrrhotite and pyrite with lesser amounts of arsenopyrite (gold ?) (BUGGE, 1978). The brecciated vein-type shows a very inhomogeneous habit and develops mostly in the greenstones. The vein-material consists of quartz (carbonate is not reported) (TRØFTEN, 1957) and sulfides, mostly chalcopyrite with bornite and digenite. Typical are ore-shots near boundaries of greenstones.

All prospecting programms in the last 50 years,which encluded yeophysical surveys, diamond-drilling and pitting came to a negative result.

2.2.3 THE VEST-VIDDA.

A nearly complete description of the Vest - Vidda is given by HOLMES et al (1957). The results of further works, namely carried out by A. SOLLI are at the present time not available, though they are discussed already by BJØRLYKKE (1982). Uurthermore there are found some regional studies mainly dealing with the Bidjovagge Cu - Au - deposit. Espesially they led forewards to a better understanding of the tectonic structure of this area.

The rocks of the Vest-Vidda are metamorphosed in either very low greenschist (Caravarre region) or in amphibolite- facies.

The nowadays valid stratigraphy for the "Vest- Vidda" oriyinates from OFTEDAHL (1974) Fig. 6.

As pointed out, the supracrustale rock-assemblage comprises out of three main groups. The bottom-part builds the "Masi- yruppen", which mainly is composed out of arenaceous sediments, here the Masi - konglomerate and the Masi-quartzite. This Masi-quartzite is well known especially from its significant amount of Cr-mica (Fuchsite). Right beyond this horizon there is found the "lowest" greenstone-series which is called the Gåldenvarriformation (BJØRLYKKE, 1982). - 12 -

fEra og alder Stratigrafi.

Ost-karelsk Yngre efiabasganger.

Invasjon av pegmatittgranitt på sprekker. (Sen-karelsk) Foldning, metamorfose, granittiseong.

Careverre-gruppen. Sandstein, dels grov og feltspatisk. Karelsk Argillitt med karbonatlag. Kautokeino-konglomerat. Argillitter, tuffittiske leirskdre.

'&skias-gruppen. 1800-1900 Grønnstem; dertil tuffskdre, agglornerat, kvartskeratobir. intrusjoner av gabbro og ultrabasoke bergarter

Mesi-gruppen. Masi kvartsdt, bl.a. med fuchsot

Masi konglomerat. Grønnskifer-fm. (?), Masi-kbron Basal-arkose (Karasjokk, 100 m v. Skoganvarle). Skoganvarre-kg1... Basalkg1. log breksiel -• Pre-samdfisk. Ca. 2800 Migmatitt-gneoer med rester av ambboint, etc.

Fig. 6: Stratigraphic of the Vest-Vidda (OFTEDAHL, 1974).

The following "Caskias-group"comrpises out of masses of metabasalts(amphibolites) with local obvious pillow- and agglomerate-structures, beds of tuffites, graphite rich pelitic sediments and the often described and discussed Albite-felsite from the Bidjovagge-mine, a rock, which supposely represents a felsic volcanic tuft (leptite) (HOLLANDER, 1979).

This rockgroup with predominating basic volcanics is capped by the "Caravarre-group", a more arenaceous and argillaceous unit, which carries minor amount of the tuffaceous pelites.

2.2.3.1 ECONOMIC GEOLOGY.

1n the opposite to the Karasjok-group no placer gold occurences are reported from the Vest-Vidda. Several Cu, Zn, Pb enrichments are pointed out by HOLMSEN et al (1957). These occure as syngenetic mineralisations in graphite-rich sediments (either untouched by tectonics or brecciated)(ppto 0,5 % Cu. (GJERSVIK 1957))or are bound as a epigentic type of deposition to metasomatic alt-ra- tions or to vein likestructures. All of them are restricted to the Caskias-formation.

The one and yet only reported deposit of commercial size is the Bidjovagge-mine, located in thembstwesterly part of the Vest-Vidda. Mining operations here started in 1970, after several years of prospecting and exploration. "Due to the falling prices of copper" the production was already closed down in the middle of 1975 (HOLLANDER, 1979). - 13 -

The Cu - Au mineralisations at Bidjovagge occure in the Casikas-Stuorajavre group, which consists in that part out of either greenstones or greenschists, than carbonaceous schists, the albite-felsite and further more out of intrusive amphibolites and metadiabases. The sulfides are mainly localized to the albite-felsite and the carbonaceous schists, which in places show a significant brecciation (matrix out of chalcopyrite). The heavy sulfide concentrations are found in more or less lenseshaped bodies which are following the main tectonic structures. They represent remobilisations from syngenetic, stratabound mineralisations.

The ore-minerals are chalcopyrite, pyrite and pyrrhotite. Galena, sphalerite and magnetite are restricted to fissuring. The reported gold is mostly connected with chalcopyrite and pyrite, or, by lesser amounts of sulfides, to Bi-, Ni-, Fe- tellurides (HAGEN 1981/82).

The Cu-content varies between 1,8 and 2,1 %. The Au-content shows a great variation, but the average grade is about 1,2 ppm. (HAGEN, 1982), 0,5 Ppm (HOLLANDER, 1979).

2.3 THE ALTA-KVENNANGEN "TECTONIC-WINDOW.".

The Alta-Kvennangen window:-is used in fact,of the very good ouccrop-situation,as a referance-district, by, for example, interprelations of the precambrian rock-unit of the Finnmabksviidda.

Most of the papers available are dealing with the Cu- mineralisations, found at Raipas and Kåfjord and further in the Bergmark-district. From ZWAAN a GAUTIER (1980) there exist a geological map (1 : 50000) and a detailed description of the Alta - Gargia region, the east part of the precambrian tectonic window.

The precambrian rocks of this area are combined to the Raipas-group, which consists, following the new subdivision, out of four sections, known as the "Kvenvik-","Storviknes-", "Skoaddivarri-" and the "Luovusvarriformation". (Fig. 7).

This group is overlain by the senprecambrian "Bossekop-" and the Bocambrian "Borrasformation". - 14 -

Fig. 7:

Stratigraphie of the Alta-Kvennangen tectonic window

Luovusvarriformation (dolomite with sandstone) Skoaddivarriformation (sandstone with metapelites) Raipas- group Storviknes-formation (carbonates and metapelites) Kvenvikformation (metagabbro, metabasalt, tuffs, metapelites, carbonates).

The Kvenvik-formation encloses a more or less volcanic sequence, mainly built up out of metagabbros and metabasalts. They are interlayered by tuffs and tuffites which gradually increase in amount up section. This pure volcanic pile is in his upper parts more and more intermixed by pelitic and carbonaceous sediments.

The following Storviknes-formation carries an alternating bedding of carbonates and pelites.

Messive to slightly bedded sandstone, which is interbedded by some horizons of pelitic material, predominates in the Skuaddivarri-formation.

The Luovusvarri-formation shows a significant alternation of dolomites and sandstones.

For the better understanding of the lithology of the Raipas- group, there are given, in the following, some simplified profiles published in different NGU-reports and by ZWAAN a. GAuTIEA (1980). (Fig. 8 - 10).

SKYVEDEKKER Skifer/sandstein

Skifer/sandstein BORRASGRUPPEN

BOSSEKOP ".. GRUPPEN . • Kvartsitt, noe skifer RAIPASGRUPPEN

koaddevarri- Sandstein. Dolomittlag f orrnasjonen i •vre deler

Siltstein

..--, Massiv dolomitt

Storviknes - Dolomitt/skifer formasjonen

Laminert sandstein , ->. ..., ....- / Tuff/tuffit/grennskifer ... / 1 t . ...,- - ‘ % / c> Putelava , / 0 17 ... ig"

0 I 1 % ./ 0 . • v Metagabbro 1 - 1/ \ V- . V v , _ Kvenvik - v v - Dolomitt \ for masjone n v ... i /

I ..., 1 / fl

Fig. 8. Sinp1ifiai stratigraphy of the Alta - Kværangen window (VIK, 1979).

GRANATOLIMMERSKIFER

„ALTASKIFER" NALGANAS-DEKKET leokambrium?) META-ARKOSE

GLIMMERSKIFER

Nentjellgruppen 13.1110E7GMEIS 14EDAMFIBOLITTLINSER mkjent atder,antott) kprekambrium KALKGLIMMERSKIFERMED DUMIe1KR,OPP

HORMOLENDESKIFER ' KVARISKERATOFYR/F114KORNET,LYS GARGIA-DEKKET GM(ISIOFTE KALKSPATHOLDIG1 GYEGMEIS

------Komsagruppen

- - leOkornbrium?) -

mETA-ARKOSE

POLYRIKTKONGLONERAT

BOrmsgruppen SAbOS1EINOG GRGNN SKIFER leokambrium og yngre?) -.. -- -- , -. GLAOG GRINN SIGFER ----' •KVARTSITT-KONGLOMERAT BassekoPgrUOWIR C."TILLITT (sen-prekarnbrium) ....-• • . • • ' . KvARTS111I VEKSLINGMED LEIRSKIFER INARTSITT DOLOMITIi VEKSLINGMED SANOsited IHOYESIE FORMASJONI

Øvre Rwpas :SANDSTEINMED NOEN LEIRSIOFERLAG

LEIRS/cIFERLAG OCILOMITTOG KALKSTEIM RAIPASGRUPPEN Ikarelsk?) METABASALT

METAGABBRO

Nedre Rempos 'BASALIISK TUFF OG TUFFITT

LEOISKIFERLAG

METABASALTMED PUTESTRUKTUR

001.014ITT OG KALKSTEIN

Fig.9. Tektonostratigraphicoolumn(map-sheetAlta).Vertical scaleis approximate.(NAAN og GAURLER,1980). KALAK — DEKKET

Metaarkose KJÆKAN —GRUPPEN Kvartsitt tillitt leirstem

RAIPAS— GRUPPEN 4. IS000 rn Luovusvarrisandste;nen; Dolomitt vekshng med sandstem

Skoadduvarrisandstemen Feltspat sk sandstem med tynne leirstemslag og konglomerater

Grafittholdig sandste n)

. .• •• ••• ø • • ••• • 4.• • b • • • ••• • b, Storviknesdolom;Iten:

Siltstein med tynne dolorni ttlag ^, 350 rn Dotomitt Imed underordnet kalkspat

RodLig sittstein

Kvenvikgronnstemen

Tuffitt

Met abasaltlag sk lt av tynne tufflag. Pwer den overste enheten

Kalkspaldom nert karbonat Svartsksfer

‘;/f 5,f I, Metagabbro

Putelava med endel metagabbrolinser 1 'Blandet enhet- ftuffitt , els, svartfels1

. . — Svartfels Fels Intrudert av rnagnehttholdige --• ••.'"•\7--1 '• metagabbro - sItts Dolom tt + 10 0Orn _ . _

° 0 ° 0 ° 0 00 ° ° Dolom tt feltspat b a

\--/ -1•

••/‘ •"„I 1%-/' 1—% 1 C-G•1;,1,' ‘1,

Fig. 10. Simplifiedstratigraphyof the hata - Kvanangenwindow (VIK,1981). - 18 -

2.3.1 ECONOMIC GEOLOGY.

The Alta-Kvennangen window shows a great number of Cu- mineralisations and - deposits, that have been extensively explored or even have been mined for a longer period. The most important Cu-occurences were Kåfjord and Raipas, both located in the Alta-Gargia district, and the "Bergmark- området" in the western part of this window.

There are found two main types of deposits (VIK 1979/80/81), both located in the Kvenvikformation of the Raipas-group. The first, dessiminated type, is connected to albite-felsite and graphite-schists of a greenstone sequence. This appear- unce makes it comparible with the Cu-mineralisation at Bidjovagge

The second type represents vein-deposits. There are described either quartz - carbonate - or siderite - veins, which carry chalcopyrite and pyrite in bigger and smaller lumps. These veius occure mainly in altered metagabbros (VIK, 1981) greenstones (BJØRLYKKE, 1982). This group includes too the Raipas-copper-mine, a brecciated vein-type deposit, but located in dolomites and metapelites of the "Storvikformation".

2.4 THE KOMAGFJORD-WINDOW.

The general geology of the Komagfjord-window is described either by REITAN (1963) or by PHARAOH (1980) (see BJØRLYKKE, 1982).

The supercrustale series of karalish age is divided into the "Holmvannsgruppen", the"Sa1tvannsgruppen" and thc "Nus.serengruppen".Both the first and the last one, enclose basic and ultrabasic volcanics (metabasalt, tuffs, tuffites) and in minor amounts calcareous sediments, quartzites and carbonaceaus layers. The "Saltvannsgroup", located in be- Lween these volcanic-sedimentary sections,comprises out of arkosic sandstones and polymikt conglomerates.

2.4.1 ECONOMIC GEOLOGY.

There are known a lot of copper-iron sulfide deposits from the Kvennangen-window. These mineralisations are divided into a more Cu-rich dessiminated type, found for example in the arkosic sandstones of the Saltvannsgroup at Ulve- ryggen (Repparfjord) and a more pyrite-rich paragensis, which is represented by small vein-fillings especially occuring in the greenstones and quartzites of the Holmvanns- and Nusserengroup. This type of deposite has been mined at Bratthammeren, Porsa and Bachkes. - ty -

2.5 CORRELATIONS BETWEEN THE PRECAMBRIAN AREAS OF THE FINNMARK-DISTRICT.

Most of the correlations between the supercrustale series of precambrian age, found in the Finnmark-district, are made for only that reason, to clear up the geology and lithostratigraphy of the highly covered areas, especially these of the Finnmarks-vidda. Further more these combi- nations can also help with prospecting and exploration programmes. These correlations were made with the use of marker horizons and characteristic rock-groups.and several interpretations may exist. The "Masigruppen" finds, and there is no doubt, its pendant in the arenaceous bottom part of the Karasjok-group. Com- plicated is the situation of the Gåldenvarriformation. Egual material has not been found in the basis section on the east side of the gneis-dome. This unit may be correlated with the Holmvannsgroup of the Komagfjord tectonic window. The following Caskejasformation (Vest-Vidda) is comparable with the volcanic-sedimentary section of the Karasjok-group, the Nusserengroup of the Komagfjordarea, the Kvenvikformation of the Alta - Kvenangen - window and the Skøgsfossgreenstone of the Petsamogroup of the east Finnmark-district. The arenaceous sediments of the Caravarriformation (Vest-Vidda) supposely find their northern extension in the Skuadduvarrisandstone of the Alta - Kvenangen area. Further it may be equivalent with the Saltvannsgroup (Komagfjord window), but also with the Masi-quartzite of the Vest-Vidda.

A main problem is the stratigraphic position of the Iskuras quartzite (Karasjok-district), which can be, based on the mineralogy, combined with the Masi-quartzite in the west. This is done as well by OFTEDAHL (1974) as by BJØRLYKKE (1982). WENNERVIRTA (1969) tries no real correlation. He comes only to the result, that this block of rock must belong to his sedimentary-volcanic complex, what includes the arenaceous basis and the volcanic-sedimentary section, without the upper amphibolited and hornblendites (2.2.2).

From the economic point of view, it it to stress out, that placer gold occurences are restricted to the eastern side of the Finnmark-vidda. It is conspicuous too, that no banded iron-formations are reported from other precambrian outerop-areas. Furthermore no gold-quartz veins are found at all within the norwegian part.

The Cu-mineralisation and - deposits are restricted, with only some exceptions, to the volcanic-sedimentary rockgroup at the basis of the precambrian supercrustale series. No - 20 -

real massive stratiform sulfide-deposite is known from the whole district. On the opposite, mumerous vein-type or u-ecciated vein-type deposits with sometimes high Cu-values >. 10 % (VIK,1980/81)) are described from the precambrian vindows and also (one)from the north-part (Porsanger) of the fLrasjok greenstone-belt. Stratiform dessiminated types it albite-felsits (possibly of volcanic origin) and carbona- ct:.usschists and greenstones have been mined at Bidjovagge secondary enriched, tectonically controlled) and in tht Bergmark-district. Equal mineralisations have been re- por:,d from North-Sweden and North-Finnland (BJØRLYKKE, 1982).

3. G (LOGY OF THE KARASJOK-DISTRICT.

The glc1ogy of the Karasjok-district is mainly described by WENNER''RTA (1969) and SKALVOLL (1972). From the last one originttes too the nowadays valid geological-map (scale 1 : 250 000 of this area. Further informations are available by diffttent NGU-rapports, which in the majority are dealing with the irospecting on iron-ore connected to the banded iron-foric.tion(2.2.2.1). Several other papers, such from BJØRLYKKL (1966) and REUSCH (1903) are more or less restricted to the pl,ler gold occurences in this area (2.2.2.1).

Both, stratiraphy and the main geology of this area are not really clea.td up yet. But a model of the lithology of the precambrian c)ckgronp is already in operation (2.2.2).

The geologica map draws a very diffuse picture of the Kara- sjok district. Phe whole series of supercrustale rocks seems to be divided n several small blocks, which have been rotated against each otPlor.This is shurely on one hand due to a lack a information (Ivw degree of outcrops), to the other .due to a certain high diree of deformation, which is represented by isoclinal folO_ng, obvious, both, in a smaller and a greater scale ann in an extreme thrust faulting.

However, even from he very little information available, it is possible to dra. out belts of specific rock appearence.

The basis and ultrabt;is volcanics for example, classified by SKALVOLL (1972) a metapicrites, together with the banded iron-formations are siread out over a crescent shaped area, which extends from Vuuilosjavri in the south to Bakkelvarri in the north. (Fig. 4). This area lies very close to the border of the gneis-dom, but east from Bavtajåkka and Karasjåkka. In this belt the metavolcanics are accompanied by the mica schists and luartz-mica schists of the arenaceous bottom-patt.Further to tle east there follows the large district of the hornblen: schists and the amphibolites. A belt of quarlzites (with ruchsite) is extending from Biesken- jarga in the west over Jaegilvarri to the east side of Karasjok. - 21-

The strike of the horizons varies between 00 and 360° (4000). Locally there is found a very distinct E - W trend, here especially in the metapicrites at Njuocåkka and Gaessagielas. The dip is in all directions, but clearly predomigates to- wardsthe east. The gipangles are normaly 30 to 45 , sometimes higher, at 60 , ore even more.

Tectonical studies from the Karasjok-district have not really been carried out yet. No foldaxis or faults are included in the geological map from SKÅLVOLL (1972). A structural sketch with a brief explanation is given by WENNERWIRTA (1969). This illustration shows foldaxis, which are mostly N S trending, here in Iskuras-district (south of Karasjok) and strict E - W orientated in the far south at Baeivasgiedde. Fractures occure as flat lying uplifts strikeing ca. NE - SW. The direction of movemertor even the age are not discussed.

4. DIAMOND-DRILLING PROGRAMME 1982.

The diamond-drilling program in the Karasjok-project area lasted at least three month, from the 18th of June to the 16th of September. On ground of a mutual aggreament, there was a two weeks break from the 13th to the 27th of July.

The works were carried out by the norwegian drill-company TERRANOR A/S. Drilling-operations were undertaken in two skifts. The equipment consisted out of a rig-slade, a transport-slade and muskeg (Bombardier, Can.). The drill-rig was a fully automated hydraulic core drill of the type DBH 700 from Diamond Boart, Belgium,with wireline. Normal coring was undertaken by 46,1 mm (1.815') (0.D.) steel-rocks of the metric system and diamond-bits with impregnated dia- monds Ly different hardnesses and diamond-qualities. The normale casing was done by 56,1 mm (2.209') and 66,1 mm (2.602') rocks. In only half of the cases, there was used a 76,1 mm (2.996') dimension.

The drilling operations were concentrated in two main areas. (Fig. 11). The first is the tract between Karasjok and Bieskenjarga, which encloses the drill-targets on Madijavri (1 holo), Daktejåkka (2 holes), Sammelcåkka (1 hole), Gaetkevarri (2 holes) and Aslat-Pier-Varri (1 hole). These locations are connected to good supply gravel roads. The secOnd drill-area is lying in the far southwest at Baeivas- giedde, about 35 km (linear distance) from Karasjok. Drilling was done here at Dabmutsuokkadas (3 holes) and Gaessaroavvi (1 hole). This place can be reached only either by tractor or heavy cross country cars on swampy dirt roads or by heli- copter. No supply is possible by water-plane. The transport of the drill-equipment to this operation area was undertaken by muskeg.

There were drilled 11 holes (13 with stucked ones: DAB-82-01/04) with a total meterage of 1.337,35 m. The drill-targets were - 22 -

KARASJOK

MAQ -82-01 war3-- ‘DAK- 82-02 OAK-132-01 lies.5kka 0 SAM - 82-01 ° GPET- 82-01

APV- 82-01 0 G/K T- 82-02

BIE KENJARGA

•

4—PROSPECTION - AREA •

BEIVASGIEDOE

DAB-82-04/05 0 0-DAB- 82-03 0 DAB- 82- 01/02 44' o GMS- 82-01

C:=>

• •

10 15 k Orin hole INacer gold occurence scale 1 : 250 030

Fig. il. Drill hole location map, Karasjok-prosject.

- 23 -

good corresponding EM- and Mag.-anomalies of ground geophysical surveys. Some conductors could be eliminated before as graphite hosizons by former fieldobservations. The dråll- angle was - 45 , that in fact of the mostly low (30 - 45 ) dipping of the supercrustale horizons. The direction of drilling was mostly aligned with the geophysical profils.

4.1 DIAMOND DRILL HOLE DESCRIPTION.

The logs of the single drill holes are arranged at the end of this report.Furthermore, from every drill hole there are columnar profils available. The illustrations include too the estimated total sulfide contents of the different rock- lypes, the sample-locations together with their chemical results and sketches of the EM- and Mag.-anomalies of the target.

MAD-82-0)

location: Madijavri-grid, 1 km southwest of Karasjok L 1 + 00 N / 0 + 00 drilling: - 450, grid west (3300) overburden: 3,40 m depth: 75,00 m further points of interest: started : 19.06.82 (d) finnished : 21.06.82 (d) cementation at 35,30 m. samples: 4, covering together 6 m.

This drill hole intersected three distinct rock-units. These are from the top downwards a metagabbro (0 - 46 m), a graphite sequense (46 - 57 m) and a series of argillaceous metasediments with interlayered basis volcanics (57 - 75 m).

The metagabbro (amphibolite) is a massive, locally - here pspecially in the contamination zone to the metasediments - slightly schistose, greenish black rock, which occures as well in a medium (0,2 - 0,5 mm) as a coarse grained (0,5 - 1,0 nm) variety. The plagioklas-content may rise to about 60 % - this gradual but is mostly very very low. A neglig- able titanomagnetite impregnation is recognized between 22 and 23 m. Sulfides, here mostly pyrite accompanied sometimes by pyrrhotite, are present sporadically. At about 40 m there occures a massive sulfide seam (pyrrhotite overestimates pyrite), which shows very irregilar walls to the surrounding foliated and disturbed metagabbro. This mineralisation shows no characteristics with a real vein-type deposition. It is more to think of a lense shaped remobilisation. The cnntact between the metagabbro and the metasediments are clearly discordant. - 24 -

The graphite sequence, of 11 m thickness, is maid up out of a more or less massive, blackish coloured graphite pelite, which posesses some bands of biotite-phyllite. To the irregular fissuring, there are bound quartz (remobilized, autochthon) and the only visuable sulfides (pyrrhotite, pyrite).

In the lowest sequence there predominates a dark grey, very well schistose garnet phyllite (garnets reach locally 10 Vol. - by an average grainsize of 0,2 mm), which is interbedded by a green to light green biotite-chlorite-amphibolite, perhaps a basic tuff to tuffite.

The sedimentary pile of this drill hole shows a clear domination in pelitic sediments. The amount of intermixed volcanics is very low.

Tho EM-conductor is represented by the graphite sequence.

DAK-82-01. location: Daktojåkka-grid, 4 km west of Karasjok. 9 00 S / 1 + 25 drilling: - 45°, grid west (340°) overburden: 17,00 m depth: 91,60 m further points of interest: startet : 23.06.82 (n) finished: 25.06.82 (n) samples: 13,covering together 27 m.

From the lithology this drill hole is to divide into an upper section mainly made up out of quartz-feldspar-biotite- amphibole gneis (17,00 - 57,82 m), a middle one, named yraphite sequence (57,82 - 84,42 m) and a last one, consisting out of metagabbro (84,42 - 91,60 m).

The first section shows a high contingent of metamorphosed areaceous sedimentsoccuring as quartzites, metasiltstones/ sandstones and the quartz-feldspar-biotite-amphibOle gneis, a may be in situ recrystallized arkose or greywacke (WINDLEY, 1977). This gneis is for the first described as a rock of sedimentary origin, thought it is not clear yet, of -rhat kind of parent rock it originates.

The following graphite-rich zone shows a distinct alternating bedding of a massive to well laminated, sometimes distorted graphite slate with the equal arenaceous metasediments of - 25 -

the more upper section. The contacts between these pelitic and argillitic/arenaceous beds are always extreme sharp.

The sulphides as pyrite and pyrrhotite (no chalcopyrite has been observed) displays a clear rockpreference. Pyrite is the only sulfide occuring in the quartzites. It is hear filling cracks and veins, what let think of a secondary enrichment (5 to 7 Vol.-%). In the graphite slates there is mineralized as well pyrrhotite (major part) as pyrite (1 - 2 Vol.-%).

The EM-conductor is the graphitic sequence.

DAB-82-02.

location: Daktejåkka-grid, 4 km west of Karasjok. • 3 + 00 N / 0 + 50 V drilling: - 450, grid west (3400) overburden: 7,60 m depth: 82,75 m further points of interest-started: 25.06.82 (d) finished: 26.06.82 (d) samples: 4, covering together 7 m.

The main part of this hole is made up out of a amphibole/ hornblende schist, supposely the same kind of rock SKALVOLL (1972) already described from this area. This rock occures in several varieties, here, with or without biotite and garnets (0,5 - 1,0 mm), or markedly enriched in quartz or graphite. It is possibly of sedmentary origin. This amphibolite is furter down interlayered by thinner (20 cm) and • thicker ( 2 m) bands of graphite slate and metasandstone/ -silstone.

This series is intruded b a gabbraThe contamination zone between the metasediments ana this intrusive rock is charak- terized by an alternating of bands of highly reworked graphite schist with a very schistose metagabbro.

Sulfide mineralisation is found in metasiltstones,graphite horizons and distorted sections of the metagabbro. The values in general do not pass 2 Vol.-%. Pyrite is the most occuring sulfide.

The EM-conductor is represented by the graphite horizons. - 26 -

SAM-82-01. location: Sammelcåkka, 11 km west from Karasjok. 3 + 00 S / 1 + 25 Ø drilling: - 450, grid west (3100) overburden: 6,50 m depth: 124,00 m further points of int-erest:startet : 29.06,82 (n) finished: 01.07.82 (n) samples: 6, covering together.10 m.

The drill hole shows a very clear predominance of metamorphosed arenaceous and argillitic sediments. Products of volcanic activities are only obvious in one section. Here they even exceed the accompaning sediments.

The revealed rockpile presents four significant rockunits. These are the arkosic sandstone (6,50 - 36,68 m), the upper garnet schist (36,68 - 56,70 m), the volcanic-sedimentary section (56,70 - 84,40 m) and the lower garnet schist (84,40 - 124,00 m). The first two ones and the last one are very homogeneous in character. The most important part of this drill hole is the volcanic-sedimentary interval, which consists out of an alternating bedding of graphite slates, laminated intervals with graphite schists, phyllites, biotite schists and metasiltstones, than quartzites and basic to ultrabasic tuffs and tuffites. Further with are intermediate volcanics. The contact between the different beds or horizons are always sharp. This section carries the highest sulfide mineralisation which can reach in places 20 Vol.-%. The most important sulfide is pyrrhotite. Pyrite occures in only minor amounts.

High magnetite concentrations accompanied by idiomorphic pyrite (2 Vol - %) are found in the arkosic sandstone. The garnet schist are always sulfide - or oxide - free.

The Em-anomaly indicates surely the graphite and the sulfide of the volcanic-sedimentary section. The weak and wide Mag. should be referred to the magnetite found in the arkosic sandstone and the higher pyrrhotite concentration in the volcanic-sedimentary section.

GET-82-01. location: Gaetkevarri, 14 km west from Karasjok. 3 + 00 N / 0 + 75 Ø. drilling: - 45, grid° west (304). 0 - 27 -

overburden: 6,00 m depth: 137,80 m further point of interest: startet : 02.07.82 (n) finished: 04.07.82 (d) samples: 18, covering together 28 m.

The drill hole intersected a very structured sedimentary - volcanic pile. The sediments consists mainly out of pelitic rocks, either metamorphosed to garnet-aphibole schists or, by consSderable amount of carbon, to graphite slates. Further more there are occuring carbonate beds (the only drilled ones) and some horizons of quartzite. The volcanic material is of basic and supposely of intermediate to felic composttionand represents tuffs and tuffites. Some greenstones are surely metamorphosed basalt-flows. They build up only some thinner bands.

The division of this sedimentary-volcanic pile into a metagabbro section (6,00 - 26,00 m), a graphitic interval (26,00 - 80,70 m), a unit of garnet - amphibole schists (80,70 - 94,70 m), a volcanic sequence (94,70 - 117,30 m), a carbonate horizon (117,30 - 132,80 m) and a massive quartzite occurence (132,80 - 137,80 m) is surely practicable.

Sulfidmineralisation is restricted to the graphite slates and the basic volcanics. The amount is normally very low and varies between 1 and 2 Vol - %. Pyrrhotite is the most common sulfide. It is accompanied by some pyrite. Chalco- pyrite is in the opposite only mineralized in the graphite slates.

The EM-conductor is represented by the graphite slates.

GÆT - 82 - 02.

location: Gaetkevarri, 14 km west from Karasjok. 18 + 00 S / 9 + 75 drilling: - 450, grid west (304o). overburden: 6,05 m depth: 157,40 m further points of interest : started: 06.07.82 (n) finished: 08.07.82 (d) samples: 31, covering together 54 m.

The top group of this drill hole consists of two thick graphite horizons, which are divided by a 11 m thick volca- niv sequence. This divisionpart shows in the majority biotite- - 28 -

carbonates, which have been interpretated as intermediate tuffs or tuffites. The whole group extends from the overburden to 85,40 m, were it stands in a contact to a supposely sill-like intructed metagabbro. This shows a distinct frac- tionation from a Fe, Mg-rich bottom part, now described as a plagioklas - amphibolite, to a Ca-rich hanging portion , consisting of quartz - feldspar - amphibole - gneisses or schists. They carry a significant titanomagnetic - mineralisation.

The lower sedimentary interval - from 111,90 to 157,40 m - is mainly made up out of an alternating bedding of laminated biotite schists and well bedded graphitic phyllites. In this group the content of tuffaceous material may be important, especially that in the laminated intervals. In this lower sedimentary section there are further found bands of very homogeneous biotite phyllites.

The sulfide-mineralisation, as pyrrhotite, pyrite, chalco- pryite and spahlerite, is restricted to the not intrusive rockvarieties. The content is reaching sometimes 10 Vol.-%, but varies normally around 1 and 2 Vol.-%. The highest chalcopyrite values are found in the upper graphitic section, where there also appearse sphalerite. Further down in the hole pyrrhotite and pyrite are nearly the only sulfides.

Both, graphite slates and the mica-carbonatesshow no significant differences in their sulfide-charge.

The EM-conductor is represented by the graphitic units.

APV-82-01. location: Aslat-Pier-Varri, 18 km weet from Karasjok. drilling: - 45o, grid west (324o). overburden: 4,40 m depth: 86,54 m. further points of interest: startet : 28.07.82 (d) finished: 29.07.82 (n) samples:

Intersected is a single basalt-flow, now occuring as a more ore less massive greensone. This is capped by a volcanic- sedimentary sequence, build up out of graphitic slates and basic - to ultra basic tuffs and tuffites. Further with are, but in minor amount, intermediate volcanics. This volcanic rockgroup is intruded by a gabbro, occuring as a plagioklas -amphibolite, which carries very locally some garnets. - 29 -

Sulfide mineralisation is found only in the volcanic - sedimentary section. The amounts do not pass 2 Vol.-%. Pyrrhotite is the main phase.

The EM-conductor is represented by the graphitic material.

DAB-82-01.

location : Dabmutsuokkadas, 35 km. south-west from Karasjok. L 3 + 00 S/ 2 + 75 Ø drilling : - 45, grid west (2500) overburden : 6,75 m depth : 55,60 m further points of interest: started : 09.08.82 (d) finnished: 11.08.82 (d) stucked samples : 15, covering together 31 m.

A general description of this stucked drill-hole is included in the explanations for DAB-82-03.

DAB-å2-02.

location : Dabmutsuokkadas, 35 km. south west from Karasjok. L 3 + 00 S / 2 + 85 Ø drilling : - 450, grid west (2500) • overburden : 10,25 m depth : 121,90 m further points of interest: started 12.08.82 (n) finished 15.08.82 (d) samples : 47, covering together 93,00 m

The drill hole shows a typical volcanic cycle consisting out of basic to ultrabasic volcanics with intercalated banded iron- formations. The amount of sedimentary componenSis very low.

The series starts at the bottom with a massive basalt±tI~ occuring as amphibolites or greenschists and greenstones. The following volcanic-sedimentary interval shows an alternating bedding of basic to ultrabasic volcanics (supposely tuffs), described as talk-chlorite schists, chlorite-amphibolite schists or chlorite-biotite-amphibolite schists, with graphite-felsite breccias. The contacts between each layer are mostly sharp and furthermore sometimes distorted. Some thicker horizons are - 30 -

looking very knead, what is obvious by either small scale zick-zack folding or brecciation or even mylonitisation.

The onresting banded iron-formation consists out of two main horizons, which are devided from each other by beds of graphite-felsite breccia and basic tuffs. The banded iron- formations show- only silicate or oxide facies. Interlayered are bands of cummingtonite/grunerite, which may carry significant amounS of idiomorphic garnets.

The uppermost volcanic-sedimentary section has the same lithology like the lower volcanic-sedimentary interval. But there exists a slowly incoming of argillaceous and arenaceous material up section, what is visuable by the occurence of beds of sandy metapelites.

This drill hole, together with the stucked one of DAB-82-01, shows the highest sulfide content - up to 60 vol.-% - this drilling programme has indicated. The most common sulfide is pyrrhotite, which is accompanied by lesser amounts of pyrite. Chalcopyrite is very rare.

The highest sulfide content is found in the graphite-felsite breccias, where pyrrhotite and pyrite are locally the only matrix. Furthermore concentrations of about 10 - 15 vol-% occure also in basic to ultrabasic volcanics. But here predominates a dessiminated type of mineralisations. The banded iron-formations carry lower degreese of sulfides (1 to 5 vol.-%), while the basalt-flows normaly are barren.

Magnetite occures only in the banded iron-formations and shows a distinct preference to silicate-rich rock-types.

There are several indications, which lead foreward to the assumption, that this drill hole is located in the very nearea of a thrustfault. There is first the anomalous high distortion, which grades locally in a distinct mylonitisation and second the results from the ground geophysical survey, which point out a very diffuse structure especially for the area of the drill- target. Further south all anomalies are suddenly cut off.

The EM-conductor is represented by the graphite horizons and the high sulfide mineralisations. The Mag. can be explained by the magnetite and pyrrhotite mineralisations.

DAB-82-03. location : Dabmutsuokkadas, 35 km south west from Karasjok. L 4 + 50 N/ 6 + 00 ø. - 32 -

Drilled is a banded iron-formation with silicate facies. This horizon is to correlate with the first "banded - quartzite" out off drill hole DAB-82-05.

DAB-82-05.

location : Dabmutsuokkadas - north, 35 km. south-west from Karasjok. L 1 + 50 N / 7 + 40 Ø. drilling : - 45, grid west (255°) overburden : 33,75 m depth : 114,51 m further points of interest: startet 26.08.82 (n) finished 30.08.82 (n) cementation at 35,90 m samples : 16, covering together 29 m.

The drill hole shows in equation to DAB-82-02 a very typical volcanic cycle. This starts at the base with a basalt-flow, which is here interlayered by some basic to ultrabasic tuffs. Immediatly on that follows a series of three banded iron- formations in silicate facies. As division-horizons between them appears a rock-assemblage, made out of basic to ultrabasic tuffs and graphite-felsite breccias. Further with, is one thin bed of a graphite-bearing siltstone. This section is capped by a very well strucktured rockpile, consisting out of an alternating bedding of basalt-flows, basic/ultrabasic tuffs, thin bands of banded iron-formations and some arenaceous metasediments.

Highest sulfide-concentrations, of 10 Vol-%, are locally found in the banded iron-formations. Amounts of 5 to 7 Vol.-% are reached in the graphite-felsite breccias. The most common sulfide is pyrrhotite.

Magnetite is restricted to the banded iron-formation.

Responsible for the steep Mag; is the high magnetite-concentration in the banded iron-formation. For the distinct EM- anomaly, there is no real conductor available. That is shurely, why this drill hole was not directly aligned on the geo- phySical profile.

GÆS-82-01.

location : Gæssaroavvi, 36 km. south-west from Karasjok. L 6 + 00 5 / 0 + 75 0 - 33 -

drilling : - 450, grid west (3100) overburden : 9,75 m depth : 137,00 m further points of interest: startet 01.09.82 (n) finished 12.09.82 (d) cementation at 33,55 m waiting for rods (3 days) repairing of the rotation- motor (3 days). samples : 21, covering together 45 m.

Intersected with this drill hole is a section, formed out of mainly volcanics. The most characteristing parts are two thick basalt-flows, situated at the bottom and at the top of the hole. These more or less homogeneous flows are divided from each other by a greywacke interval, which is occuring on the top of the lower flow and a volcanic section, made up out of minor basalt-flows, basic tuffs and banded iron-formations (silicate-facies).

Sulfide-mineralisation is restricted to the banded iron- formation (1 to 2 Vol.-%) and to the greywacke interval (mainly 1 Vol-%).

Magnetite occures in places in the banded iron-formation.

The geophysical anomaly is due to the pyrrhotite and magnetite enrichments and further due to a distinctiv graphite content of the greywacke.

4.2 SUMMARY AND CONCLUSION OF THE DIAMOND DRILLING PROGRAMME.

The diamond drilling programme turned out for the present no attrictive gold,gold-sulfide or sulfide mineralisation. All of the dilled conductors were graphite-rich horizons, occuring either as graphite slates or schists, which carry only un- importent amounts of dessiminated pyrrhotite, pyrite and chalcopyrite, or graphite-felsite breccias, with locally higher sulfide mineralisation. Further-more, dessiminated sulfide is found in some quartzites, tuffs or tuffites and the banded iron-formations.

In general, the most frequent sulfide occuring is pyrrhotite, what is often accompanied by pyrite. Chalcopyrite is very rare. The estimated total sulfide contents of mineralized rocks vary normally between 1 and 2 Vol.-%. But they reach locally 5 Vol.-%, or can even grade up, in very rare cases, to 60 or 100 Vol.-%. The best mineralisation is found in the drill holes DAB-82-01/02. The diamond drili holes are one of the best information available about the lithology from the Karasjok greenstone- helt.

By the holes BAB-82-01/02 it is shown, that correlaticus even between nearby driilholes are only possible by the use of marker horizons (banded iron-formations, basalt-flows) er characteristic rockgroups. Gombinations in a smaller soale are very difficult to ostablish.

ri'ne11 drill holes can be summarized to two grwips. There are nn uhe one hand those, with a very clear domination of basic volcanics, here zietabasalrs and basic to eltrabasic teffs, which carry sediments in a very low percentage. These are the drill holes from the Baeivasgied.:e area and tnat lonely one from Aslat-Pier-Varri. The further east located Ones from Gaetke- varri, Sammelckka, Daktejåkka and Madijavri show significant amounts of metamorphosed pelitic and arenaceous sediments. These are interbedded by thick horizons of carbonaceous material. Nearly no basalt-flows are obvious, but tufts and tuffites of m.ostly intermediate or even felsic compostion.

The first group of holes represent a typical Lasic to ultra- ba[:ic suBuiarine voicanic pile, a very normal bott0z.-part uf a archean greenstone-belt (WINDLEY, 1977). The second group shows sOme SL.Dts Out of a higher proportion of the volcanic .volution. They can be interpretated as marine shallow: -water deposition products, mostly bouLded to low energy environments.

This conclusion results in a possible modei fcr the litho- stratlgraphv of the Karasjok greenstene-belt (Big. 12).

intcrmodLate (felsic) mostly sediments veloanIcs (quartzites, carbonates, garnet-mica (w.,Jhibo1e) (Gaetkevarri,Sammecåkka, schists, mocapelites, Daktejkka,Madijavri graphite slates/schists) nearly no basalt-flows tuffs and tuffites basic to intermediate more sediments voluanics minor basalt-flows mcre tuffs, tuffitcs basic + ultrabasic minor sediments volcanics (metapelites, graphite slates, graphite-felsite breccias) (Dabmutsuoakkadas, several cycles of submarine Gaessaroavvi, Asiat- basalt-flows, with inter- Pit.r-Varri) bedded banded iron-formations (silicate-, oxide-, karbonate facies) tuffs Big. 12: Model of the stratigraphy of the Karasjok greenstone-belt (Karasjok-district). - 35 -

It is not clear yet, if there occures in the real a slowly outdieing of the basalt-volcanisme upsection. In the comparable greenstone-formation of the Alta-Kvenangen window, the metabasalts for example, obvious only in one horizon (Kvenvik- formation), show no distinct graduation (Fig. 8 - 10). This lead further foreward to the assumption, that the rockmaterial of the second group of drill holes - with nearly nc metabasalts- represents already sections, equally with those of the Storvik- nesformation of the Alta-Kvenangen window. But from here no tuffs or tuffites are reported. Therefore this volcanic- sedimentary assemblage should be best correlated with the uppermost sections of the Kvenvikformation of the Alta- Kvenangen window.

All these ideas do not coincide with the geological interpre- tation of the Karasjok-district. The map from SKALVOLL (1972) points out occurences of the micaceous basis of the super- curstale series (micaschists and quartzmicaschists) from the Gaetkevarri, Sammalcåkka, Daktejåkka and Madijavri areas. This opinion should be wrong, from the nowadays available information.

5. GEOCHEMICAL RESULTS.

From the 13 drill holes there were taken altogether 197 samples. These covered a total length of 377 m, what are 35,4 % of the drilled meterage. The decision either to take 1, 2 or 3 m material depended on the lithology of the sampled section. There was only taken special looking rockmaterial, like visuable mineralized metasediments-quartzites, carbon-rich metapelites - all kinds of tuffs and tuffites, banded iron-formations and obviously altered basic volcanics. Further were included all quartz-carbonate occurences (very rare mineralized). The samples were assayed by assessment assay methods for Au, Ag, Cu, Zn and Pb. Not all results have been received yet.

From the nowadays available results only one Au-assay (GET- 82-02, sample 17, 54,50 - 55,50 m) showed an attractive enrichment. Furthermore no higher copper-mineralisation hhs been prooved.

Except from MAD-82-01 all the other drill holes contain one or even more samples with a low Au-content, variing mostly between 0,034 and 0,102 ppm. The highest value of 0,816 ppm Au was found in GÆT-82-02, a sample which consists out of graphitic slate, mica-carbonate and biotite-chlorite-talk schists. This content stands alone for only 1 m. The surround samples do not reach more than 0,064 ppm Au. Furthermore there - 36 -

are better looking Au-targets occuring in a banded iron- formation of DAB-82-02 (66 - 72 m), with a Au-content of 0,102 to 0,544 ppm and in a graphite slate of GÆT-82-02 (12 - 27 m) with 0,034 to 0,374 ppm Au.

It is obvious, that the detacted Au normally is accompanied by somewhat higher values of Cu and Zn. One anomaly is found in the above mentioned banded iron-formation, where the assayed Au stands alone, joined only by traces of Cu, Ag and Zn.

It is surprising, that no real Au-enrichment has been prooved. There are visuable all characteristics of good Au-occurences, for example talk-chlorite schists and banded iron-formations. Anyways, the uneconomic Au-content of the assayed banded iron-formation does not surprise very much. It is already proposed by several authors, that high Au- values are bound only to the sulfide - or carbonatic facies of • banded iron-formation, while the argillaceous variety, rich in pyrrhotite, mostly is barren (FRIPP, 1976; UITTERDIJK APPEL, 1979).

The Cu-values range normally between 0,02 and 0,05 %. The highest content of 0,13 % is found in drill hole SAM-82-01. The procentage of Zn does not increase over 0,24 (DAB-82-02), normal rates are between 0,02 and 0,09 %. No, or only traces of Ag and Pb have been reported.

•

TABLE OF CONTENTS

Summary: Page:

1. Introduction 1 - 2 2. General, geology of the Finnmark- district 3 2.1 The "Øst-Finnmarks Grunnfjell" 4 - 5 2.1.1 Economic geology 5 2.2 Geology of the Finnmark-vidda 5 - 11 2.2.1 The central gneisdome 7 2.2.2 The Karasjok-group 7 - 11 2.2.2.1 Economic geology 9 - 11 2.2.3 The Vest-Vidda 11 - 13 2.2.3.1 Economic geology 12 - 13 2.3 The Alta-Kvenangen window 13 - 18 2.3.1 Economic geology 18 2:4 The Komagfjord-window 18 2.4.1 Economic geology 2.5 Correlations between the precambrian areas of the Finnmark-district 19 - 20 3. Geology of the Karasjok-district 20 - 21 4. Diamond-drilling programme 1982 21 4.1 Diamond drill hole description 23 - 33 4.2 Summary and conclusion of the diamond 33 - 35 drilling project 5. Geochemical results 35 - 36 REFERENCES.

Diamond drill hole logs. MAPS .

MAD - 82 - 01 DAK - 82 - 01 DAK - 82 - 02 SAM - 82 - 01 GÆT - 82 - 01 GÆT - 82 - 02 APV - 82 - 01 DAB - 82 - 01 DAB - 82 - 02 DAB - 82 - 03 • DAB - 82 - 04/05 GÆS - 82 - 01

• SUMMARY.

The this year's diamond drilling programme of the Karasjok-project (N-81-2) lasted for three month, from the 18th of June to the 16th of September. in that time, there were drilled 11 holes (13 with stucked ones), with a total meterage of 1.337,35 m. The targets were good corresponding EM-MAG.-anomalies of ground geophysical surveys.

There were two main drill areas, first the tract between Karasjok and Bieskenjarga and second, the area around Baeivasgiedde.

Arl

The drill holes are separated from their lithology into two groups. The Baeivasgiedde holes, together with that one from Aslat-Pier-Varri show a clear domination in submarine basic volcanics, accompanied by banded iron- formations. The further east located ones are characte- rized by significant amounts of metasediments, interbedded by intermediate, (felsic) tuffs and tuffites. These significant differences between the two groups lead to a possible model for the stratigraphy of the Karasjok greenstone-belt. Correlations to the good described precambrian Alta-Kvenangen window are carried out.

The drilling programme turned out for the present no attractive gold, gold-sulfide or sulfide mineralisation. But the revealed rockmaterial shows all characteristics of good Au-occurences. • REFERENCES

BJØRLYKKE, A. (1982): NGU-Rapport Finnmarksvidda.

BJØRLYKKE, H. (1966): De alluviale gullforekomster i indre Finnmark. NGU 263, 1 - 66.

BUGGE, J.A.W. (1978): The mineral deposits in the precambrian of northern Norway in: BOWIE, S.H.U., KVALHEIM, A., HASLAM, H.W.: Mineral deposits of Europe. Vol. 1, Northwest Europe London, Inst.Min.Metall, Min. Soc., 202-211.

DAHL, T. (1891): Om fjeldbygging i Finnmarkens og guldets forekomst sammesteds. • NGU 4, 1 - 21. FRIPP, R.E.P. (1976): Stratabound gold deposits in archean banded iron-formations, Rhodesia. Econ.Geol. 71, 58 - 75.

GJERSVIK, T. (1957): Epigenetisk kobbermineralisering på Finnmarksvidda. NGU, Årbok 1957, 203, 49 - 60.

HAGEN, R. (1981): Gullet i Bidjovagge kan avgjøre gruvens skjebne. Kjemi 1, 8 - 10.

HAGEN, R. (1982): The Bidjovagge Copper-Gold deposite of western Finnmark, Norway. Geol.Rdsch. 71, 1, 94 - 103.

The geology of the Bidjovagge • HOLLANDER, N.B.(1979): mining field, western Finnmark, Norway. Norsk geol. Tidsskr. 59, 327-336.

HOLMSEN, P. PADGET, P. PEHKONEN, E. (1957): The precambrian geology of Vest- Finnmark, northern Norway. NGU, 201, 106 pp.

OFTEDAHL, CHR.(1974): Norges Geologi Tapir, Trondheim 169 pp

REITAN, P.H. (1963): The geology of the Komagfjord tectonic window of the Raipas suite Finnmark, Norway. NGU 221, 71 pp.

RENSCH, H. (1903): Fra det indre av Finnmarken NGU 36, Aarbog 1903, 1 - 64

SKALVOLL, H. (1972): Geologisk kart over Norge - berggrunnskart Karasjok - M 1 : 250 000, NGU

TRØFTEN, P.F. (1957): Regional malmleting i Finnmark Bergarkiv NGU, Rapport 3081.

TRØFTEN, P.F. (1957): Geologisk/geofysisk undersøkelse og diamantboring Karasjok. Resymé Bergarkiv NGU, Rapport: 3095.

TRØFTEN, P.F. (1962): Magnetisk rekonosering, Diamant- boring: Bakkelvarre, Suolomaras, Guoikkavarre (Karasjok). GM-Rapport: 204 C

UITTERDIJK APPEL, P.W. (1969): Stratabound copper sulfides in a banded iron-formation and in basaltic tuffs in the eary pre- cambrianIsua Supracrustal Belt, West Greenland. Econ.Geol. 74, 45-52.

VIK, E. (1979): Geologiske undersøkelser ved Raipas kobbergruve, Alta, Finnmark. NGU-Rapport nr. 1625/10 A.

VIK, E. (1980): Middavarre kobberforekomst, Kvenangen Troms. NGU-Rapport nr. 1650/46 A.

VIK, E. (1981): Bergmark gruvefelt, Kvenangen, Troms. NGU-Rapport nr. 1800/46 C.

WENNERWIRTA, H. (1968): Karasjokområdets geologi. NGU 258 (Årbok 1968), 131-184.

ZWAAN, K.B. . a.GAUTIER' A.M. (1980): Alta og Gargia. Beskrivelse til de berggrunns- geologiske kart 1834 I og 1934 IV. M 1 : 50 000. NGU, 357, 47 pp. #1-9e r

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Act - _Cardam,"_.0144 31i DIAMOND DRILL LOG • FOLLDAL VERK A/S • PAGE j/3 From To Intoryal Assays Description DDH N0.160 _n_ From To Cu Mo Pb Zn A9 q.htcoxIctriaritedeLower&‘; /7eat.-±4)

5 .44 6-714 gHolfiu,' ik_f(ec,v_4_4_91a4Zo.nr&_-srl 1110 r 2 Si 6-4.80 61.60 0.02 — 0.02

k/44.414C.A 6 15us. if,«• fik it4ifirieci/09t. (trato

._c_oniserizobat:34q/cil.—/,696-%

- 4799 7,-ez

.30 -54.32

f—

Hanin I ryili AfS. • le • e Gle ai • a•• DIAMOND DRILL LOG PAGE / FOILDAL VERK AtS D D H No • AzImoth Started DirecIlonal surveys Ak-e2-0l 390° 23.06.82 Deplb Azim. Dip. Deplh AzIm Dip. Property Angle Finishpd IZTE A — 25. 06.12 Co ord Depth Logged by +00 P2s- 9/. do From IntervaI FTwm To r».-,cuption Jr) o Assays To Cu Mo Pb Zn 71/7walinitAt"

o Ovo-25u_reLeu.

20.49 - zoatJl&k efriat

20.5r - 20.12 94s,a-L4i 4 u44 u1/444c 1244“,34 a? d)10 a«a

kA:c: d clissetflec( 4z44cLff&sue

20.92 - 20.1e Jic) 44 - aw./4“:351.44 21.510 _ 22.(10 _ctee itt? 34k- 2- .1 22. 90 .to 94.14,7 1-2, M9Car aQ044 -frees Z3.019 ZS: 00

ACC 11.00 - 21.v

23,00- 23.16"«, 9,44.6ti:44 u(c.449464.4“..) (ft94.4 Ifit etit cadokcde Veiu .A q. 40,4.4e eaws," ticS)sj cwinta2_ DIAMOND DRILL LOG PAGE c3/43 FOLLOAL VERK A/5

Interval AssayS Frotn To Describbon 131)" N °34ft-i2- Ot Frorn To Cu Mo Pb ZJ Au Ag

11:1 . a44.41 if

14,481 4øi. te..4.4 - 4 (± filat

23.2323.33 9.44.0-4-112;

ilesX ‘U.4.44.< ? 1 it44:4ccr_

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23. - 2.3 ou.44-itik4io eac

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melAti:trictet4

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lliMi fl hterfar SiteA‘ DIAMOND DRILL LOVii • FOLICIAL VERK A/S 1111, PAGE 3//3 Interval Assays From To Descoption DDH Nc34k.12_49, Fram To Cu Mo Pb Zn Au Ag

ontte& d _

14414Ste

491EA suAait_ az«msla

iistac .421:?4.14 d /00

tiht: disseueciva le _tutLit9u c

11,41AtixoWai da.vc4 4 mAy3.4‘ri ,s,914.4c.94.cpi2

kaL4-kelÅt

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1.44.4,44tol.å5.ruaA4; g

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caaa atfr2SN.ait

11.mn AIN DIAMOND DRILL LOQ PAGE • FOLLDAL VERK A/S Assays From To Descriphon DDH No3144,..820, From To Cu Mo Pb Zn Au Ag

30. cia-, icte SVelitaue

30.“ catio-cmit 41:cwd

/-/44.444cd J(Å,retaCt9tici

fict C

‘47.4- Sfariattutn

carta.“ a cvi

304-3- - CariOnailt -

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k;14.: t

Sr;94.

1.33 3 I.3.Vr rt.4-66kg.:‘

32 13 - 32,t4/ :

2,2 - 32.2fi ra. u-S121.44#

2.Z't - 32.36-1 Ltue144; (1-145nt

frea.ciet a /8

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314 .32301_;11iC?tit:tr_LkitAr_ ri«a

c4 bri‘c Icittc

rity _dit‘Claiketted (.4407g4 Caza- -

111 Inar I rykk DIAMOND DRILL LOG • FOLLDAL VERK A/S • PAGE S /2 Intoryal Assays From To DOSCrIption DDH Noa4k4/)2- / -• From To Co Mo Pb Zn Au

bted atib; ‘44,2,1.

33.80: itter447 oleitt cw ic44,441.4

' CCSZCIL 3WO - 3(2 dct..A0(

wiutot rximAr9u;s

34.42 - 34_437: pht40.‘lael~_e 144_69 4'144.2. 644"4 4 pa£4,tiotte. ilis.a: /7 4,914,e_4elp

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oo - 320 atctåt; V ttte,ict.tietti

3e.249 n60: (1>tt ~:C.SIG4.2

3940 - 90419, 144.0.44;v

liamar-1~5 DIAMOND DRILL LOG PAGE FOLLOAL VERK A/S • • Inierval Assays Frorn To Dewription DDII No j4 q 12_0/ From To Cu Mo Pb Zn At, Ag

9/.21 - (14: tuassi 9t444143.cc itzt eiSlome

41.3. - W,33 Cad

42.00 9215". uha,d4iv4.4:54rtrizi lut /44;e1)/(me

43.95- 5tuatial'4_ -49kte (46itt aSile14. „ Ittatc d,sttai lettaltd

(13. Vb--"1 myk gai cieLhuc. 46:10 (ci.‘2 9.Ax.o.r/L. e

( Ii7.42 41. I 9buatia;4-c :144(.{(41.4141_10c«..) ,91 ‘64.4-0‘

s I 4./ .00

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tiitof› ctact it-ebsj 2 - P

98.35:7:4 e. : Cuaifit4:1)0(4 Jie 1-4;it - tchAct de.

itf.cto cel;t1(6`ciimn.72~. - - DIAMONDDRILLLOG 04; PAGE g/ FOLIDAL VERN A/S • • Inlerval Assays From To 0C5CI I p1ran DDH Nafg 42- 0, From To Cu Mo Pb Zn /4"4 /Ziga<

9.4Aott4,14 tuAVA ccitr

1/61/41.e H;« Q1/44‘e.sp.91‘ frj

itts4,91.14'; rtaltAi kz$cQ,4 i. , fale

41.29 - qg 40.

ctsioc14:8_14

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2 - 3 Pcit. %)

52_32 51.5"0 9u4nri?t. DI1. - 3 140LI .57.00 a. 012 3 ‘,4 17-4-luts X P

St - .91.114:ral.91.;;.Ctaitt /10 inNct 497.44.cdriwes CRI cof DIAMOND DRILL LOG

FOLLOAL VERIS A/S 414) PAGE Ce

Interval Ftoto To Doseriplinn DDH Noj4.k. 82_ 01 From To Go MO Pab A sZa: ilf4» t

kik clidectithk tvo4- 3/1 zec,41(904, Hit4:fry .‘idurk COMalr-

1(144 Jeda;u1 ,ig4.4e4

sit" --ae°1----"4"tX , tte 1.41(xt oincipti waf.

. thie 4C4»ta 1:51)4#1-Clad-e

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iSostic etwit4 f4tir a4 . obk

VorLioi Log42lc9La4e2a - /0(c i

ki,..:n._&„e„./Ctifreetteetit4 01A yoc Jtn frea“e4

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.44- citcxs(ome, ge-a. 491 fareic freor;(4, 9u.c.e.th(14 DIAMOND DRILL LOG

• FOLLDAL VERK A/S •PAGE 9//3 Interval 04 Assa ys 4 From To DescroRlon DDH Noi444/..fa_of From To Cu o Pb Zn NAI7 fil944

_ Wtticledor(AGI cuig 21(9anc9:-( it icact4;«,i , Car.£014a frie+Li.y.At

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issu‘c carity-tAcc,it Puida.2 DIAMOND DRILL LOG PAGE le2 FOLLOAL VERK A/S • tj Inloryal Assays Frorn To DescrIplIon DDH Ot From To Gu Mo Pb Zn

lo cli,szew ilualerilec nialt-e* huiricita cio_yinchz« 63.09 bt oe 9w076; _ _ lAruxicut a4.4caccctj 4w2oa czad

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66:12- 6,5-itpaldlede 4rh tailt

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11-1,mmlnkkAA. DIAMOND DRILL LO4 • FOLLDAL VERK A/S 0/0 PAGgE Intorval r Assza:s /7/7 //74,4 Etorn To Doscdplinn ODH 0/ fi Frorn To Go Mo Pb

1-1,ta:/,_Jue4 ittegehlat 9244 at _35ea 4,164;

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4e) ColtaAtC10441

DIAMOND DRILL LO

FOLLDAL VERK A/S PAGE /2 ,3

Interval Assays From To Description DDH No()fik,... 4.2_ ( From To Cu Mo Pb Zn Au Ag

À4A4€4 C )014 cat lach

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nzo - eyip : ettai LL‘ock:it.(011usgzit.) DIAMOND DRILLLO4 • FOLLDAL VERK A/S PAGE Inlerval Assays From To Descrplion DDH No ),441, n_0 From To Mo Pb Zn Au Ag eva- zzatafr44:30(4:4 ittilitita ctiÅt.ei csizz-1.5:n tAsta£11"putr, å;s4,4;~fretiity4-

n . .54,;44c

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IrIAMOND DRILL LOG .122-01 PAGE SAKPLES FOLLDAL VERK A/S //9

Intoryal Assays bzieL • 1-4 ¼ From To DescrIplion DDEI Nosh411`f2-01 rorn To Cu MO Pb Zn Au Ag

g 01 I. 0 tik - 422- .7,44,4,fteva,3(/&44,0-m441‘6-

erswe Siert

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acrwmi,iin.‘.61

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20.9L- Z0.9/1_ si,5244

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?xta Aet: IX610-21110

23 00 -23./.5 74,4culafire a4:65 4“41-1

Ituteti fratrittit ASewteCcuitSiAalePeeuitti fia4Q4aucl 4,494‘

1,nur nkt Ai .DIAMOND DRILL LOG FOLLDALVERKA/S 111 PAGE a

Interval Assays Frorn To Descriplion DDH NO3)14/.82_,9, —From Cu Mo Pb Zn Au Ag cw‘talx. jait hm.v.1

ilzwQ ki« Lfrif Limp‘ auctiOtat Jttin «,firde<< J/01;41,4 ,4 (t /siffit-s4)

2313 - 23 33 9~4/fp

Sguirat quAsukci-Q gpl wka k.,Lm 40,y e9,9L,

23.13- n.m!_atc.MAAjle._

234s- - zq. lo ati-tualtiv2 (iusA,) til s4U»k - frettede__, hed_ae

, (tuali_,ScuxciA021"14419- ei

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2'i.2( sa,“

- 2‘01/. cdiuusL,Ai 4wirdiK2(k.“‘„)

II imar I t,I.• 31 ODIAMOND DRILL LOG PAGE 379 FOLIDAL VERK AIS

Interval Assays #24? Description DDH Noalt cfP2_ From To From To Cu Mo Ptj Zn Au Ag

4 5tutAt4ii,tuzg s6941t- friztLit 233C- 2(1.10

26-39C.a.1-

1-(lAcattec(

aa-os

tekLmiLdit-t veiLitå

— riace 1/4.30 ri) YAW-12- 3 52.6,0 5 no 0 03

u<0.44/v

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«.61 liatds ,

(g- I/d.-t)

52,32* 53 5-09.12()Alf DIAMOND DRILL LOG

FOLLDAL VERK AIS PAGE 4/9

IntervaI Assays Fiorn To DescrIptIon DDH No From To Cu Mo PO Zn Au Ag

kisd

P) funtri_fEi

ek- disi

corcarda“loWdi

.10-

4eC: 5140 - .522

(Pni P2- 9 .6- .0 • 0.0 »aCe - 911-(41 itiam;‘, 5721 . ?eue

apIAMOND DRILLLOG 111 FOLLDAL VERK AIS PAGE )79

Inlerval Assays From To Descriplion 0011 Noa(X_fl..Ø, From To Cu Mo Pb Zn Au AV

,14.464 St;iki_.2.4.44‘ deasaiu&

_ 4_;_ ti

.ghut 14.4.1e4ce,,,tct

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4441t_ditia_ried—kitzi 4414'

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,Thuite/3, '4

nyn DIAMOND DRILL LOG FOILDAL VERK A/S 111. PAGE 6/9' Inloryal Assays Frorn To Descript lon _ DDH No. :D.4il-e2-of Frorn To Cu Mo Pts Zn Au ez 42 lo ?roLgult- sffictir tttk- e2- 6 40.00 62.00 0.0/ - (tlace -

iseza‘ve

461. cod‘ , disto1dtd Adzmal ?miN-616 u)14(

tkrt;ks-trear- re- tO l'ex(.4W iO.W-Ltze. 742a.t4

fav.p.ucc_613/o_44.-.02L4fttcd4_

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HarnarI nk“.!, epIAMOND DRILL LOG 111 PAGE FOLLDAL VERK AIS 7/9)

Interval Assays From To DescoptIon DDH No.34g _,4_0/ From To Cu Mo PO Zn

k45T-41.3C: alifmak<7 Jc4W4«,) 92othilc6So6rea 9thwkle_g wdzSis14,4 taal ac.: Yfy -Gtof

iz oo 222 •J44 tuf9? reucv_7 4 - 4,2- 72.00 woo 0.03 cllace_ azoy —

4ai itot ZZ 22 (citarc)

n. 2 2 V.3, a raiAdt—t£41•6

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11.1.A.1 A

•IAMOND DRILL LOG 0 FOILDAL VERK A/S PAGE .1 791 Intorval P_ A sszanya From To DesenplIon DDH No34 g From To Cu Mo PO Ag

t/.41 1$56 itagithlte scPzic

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lt,k1 A DIAMOND DRILLLOG

FOLLOAL VERK A/S PAGE 9/9

Interyal 0 Assays Frorn To Description DDH No.CU‘k Frorn To Cu Mo Pb V. Au Ag

e0.00 U.S? ?ta rpta( (,411 42- /3 10390 f 2.00 0.02 — cfiace 0.0d8 — 2.0,44

i X2-22 lo (ctint)

as Cb-c20-icuctke4CM0w-t

Mic fl tfl0 weo (4:6,9scj

(J-04 114-LieS8U;SI-

4«.1 y2.22h, 2 1.0(0

?c, Zr.eo_(adxsvc.) fl.10 11.1 z rephiLe 49frisf

, Yee: 2.22f0 32,1.81(46K/cj

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Ihmat lt, A,• 411 DIAMOND DRILL LOG PAGE /9 FOILDAL VERK A/S

D.D.H. No. AzIrouth Started Direct lonal surveys hk - A22- 02 3110 ° 25: 04. 4.2 Depth Azim. Dip. Depth Az DIp. Property Angle Flnished .7214RTE 2wg4 — 24.04. n Co-ord Depth Logged by L3+001.7/ 0,-5-01.1 °F-P Interval Assays From To Descritaion From To Mo Pb Zn

O.00 eisicrak-t de,“

59. 49 ta&t.la 4e?4nuce

419- 10.10 74~d2,,,Lri

kgs.li laux.; haied , isconteiiu.an bumA fr(

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10.10- 4.00 2a.nuzi - J;01.tit. - re9u:r1

0.s -1.0 cga

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ctatre,(414:i itclet-at of carioxa4

fic.R r4.462,h1 ufidfit zuket - cari.

13.5-8- 131.0 t - 1.6:92

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3.2c1d;LL.? itOclia-N

DIAMOND DRILL LOahn

FOLIDAL VERK AiS 111, PAGE 2 9

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PAGE 37/9 FOLIDAL VERK A/S Ø

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FOLLDAL VERK A/S 04. PAGE X/9

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FOLLOAL VERK AIS PAGE 9/9