Vihanti - ZINC Database

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Name	Vihanti	DATA UPDATED	6.3.2007
Secondary names	Lampinsaari, Isoaho
Site photo 1		Site photo 2
LOCATION
Geological domain	Svecofennian	Province	Vihanti Region
Infrastructure fig 1		Infrastructure fig 2
Regional map 1		Regional map 2
Map sheet	243405
Northing	7145820	Easting	2555350
Latitude	64.40660N	Longitude	25.14418E
Municipality	Vihanti
Nearest town, access	11 km SE from Vihanti, 70 km SSW from Oulu. Sealed road and railway to the mine.
MINING
Mine photo 1		Mine photo 2
Mine photo 3		Mine photo 4
Exploration licence no	633/1–12, 739/1, 1107, 2165/1	Mining concession no	633/1–12a, 2165/1a
Present holder	OPEN FOR ACQUISITION
Previous holders	Geological Survey of Finland (GTK) (1946–50), Outokumpu Oyj (1951–2005), SES Finland (2006)
Status of development	Underground mine, closed
When mined	1954–92 [2,17].
Resources and grades	9.164 Mt @ 0.36 % Zn, 0.34 % Cu, and 2.59 Mt @ 284 ppm U, 3.24 % P2O5 [45].
Total production	28 Mt ore: 1.447 Mt Zn, 131000 t Cu, 103000 t Pb,190 t Ag, 3038 kg Au [2,17,45].
Total in-situ content	1.48 Mt Zn, 162000 t Cu, 99500 t Pb, 190 t Ag, 3038 kg Au [2,17,45].
Size of the deposit (Mt)	37	Size reference	[2,17,45]
Best sections
Extent of the deposit	1.5 km long, <50–200 m wide zone, extending to the depth of 1000 m [1,2,17].
Ore bodies	Several, 1–50 m thick, 50–200 m wide and 150–900 m long lodes: pyrite, zinc, chalcopyrite and Pb-Ag-Au lodes; the Zn and pyrite lodes are, nearly throughout the deposit, located 10–20 m apart [1,28]. Main ore bodies (Zn) are Ristonaho, Välisaari and Lampinsaari; Ristonaho and Välisaari are combined 1100 m long, and both are 100 m wide and 10–6 0 thick [38]. Isoaho is a plate extending from the level 350 m to the level 1000 m (below surface) [38]. The main pyrite ore bodies are Hautaräme and Hautakangas which contain low-grade Zn and Cu ore [38]. The Cu ore bodies are irregular masses in the central part of the Lampinsaari Fm [38]. The main Pb-Ag-Au ore bodies are at the W e nd of the mineralisation, near the Välisaari (Zn) and Hautaräme (py) ore bodies
Plan figure 1		Plan figure 2
Plan figure 3		Plan figure 4
Section figure 1		Section figure 2
Section figure 3		Section figure 4
EXPLORATION
Explor. site photo 1		Explor. site photo 2
Discovery year	1946
Discovery	By the GTK; the first indications were mineralised samples from glacial erractics found by amateur prospectors in 1936 and 1939; these led the GTK to discover the ore by drilling into an area indicated by glacial erratic boulder survey and as an electric and magnetic anomaly [1,2,6,7,28,33].
Exploration history	GTK (1936–1950) [1,6,7,8,10,11,27,32,33]: Glacial erratic boulder survey, bedrock mapping, till geochemical survey, ground electric, gravimetric and magnetic survey, diamond drilling, mineralogical studies, lithogeochemical survey. Outokumpu (1951–1989) [1,9,12,14,16,23,27,28,29,30]: Diamond and percussion drilling, ground magnetic, gravimetric and electric surveys, pilot plant tests, mineralogical studies, bedrock mapping. GTK (1970's–2005) [18,19,26,39,40,41,44]: Regional till-, stream-sediment and bedrock geochemical investigations, regional till stratigraphic survey, regional geomathemathical study, geological modeling, diamond drilling.
Drilling	GTK (1946–50): 40 diamond-drill holes, total 5979 m [1,6,7]; 2004–2005: 20 diamond-drill holes, total 2638 m [44]. Outokumpu (1951–1992): extensive diamond drilling in 25 m profiles across the ore; by the end of 1966 total drilling was 120 km [1].
Trench figure 1		Trench figure 2
Elements analysed	SiO2, TiO2, Al2O3, Fe2O3, MnO, MgO, CaO, Na2O, K2O, P2O5, LOI, Ag, As, Au, B, Ba, Be, Br, Co, Cr, Cu, Ga, La, Mo, Nb, Ni, Pb, Sb, Sc, Se, Sn, Sr, U, V, Zn by XRF+ICP+INAA [25]. Ag, Al, As, B, Ba, Be, Ca, Cd, Co, Cr, Cu, Fe, K, La, Li, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb, Sc, Sr, Ti, V, Y, and Zn by ICP-AES, and Au, Pd and Te by GFAAS [44].
Economic evaluations	The first resource estimates by the GTK in 1950 [6]. Full feasibility study by Outokumpu in 1952–54 [1].
Geophysical response	The pyrite lodes have a good response on slingram and gravimetry [7]. The black shales have a strong response on both magnetic and electric methods [2].
Geophys. anomaly fig. 1		Geophys. anomaly fig. 2
Petrophysics	Click here
Primary geochemical dispersion	An extensive Zn anomaly in dolomites and skarns and a similar Pb anomaly in all local rocks, except the black shales [25]. The sequence of increasing lateral extent of the anomalies is: Cu, Mo, U, Ba, Tl, As, Hg, Zn, Ag, Pb, Bi, Sb [28].
Secondary geochemical dispersion	A strong Au anomaly in till related to the ore, also where practically all zinc has been leached away from till [41]. Possibly, an Au anomaly in till related to the ore [18]. Only a low-contrast, incoherent, areally restricted Zn-Pb-Cu anomaly in till; rather, the Zn anomalies in till reflect the locations of granitic rocks in the region [15,19].
Primary anomaly fig. 1		Secondary anomaly fig. 1
Primary anomaly fig. 2		Secondary anomaly fig. 2
Primary anomaly fig. 3		Secondary anomaly fig. 3
Exploration geologist(s) in charge	GTK: Aimo Mikkola, Jarmo Nikander Outokumpu: Pentti Rouhunkoski
ORE
Ore outcrop photo 1		Ore outcrop photo 2
Major ore minerals	Sphalerite, pyrrhotite, galena, chalcopyrite, pyrite [1,12,38].
Minor ore minerals	Cubanite, vallerite, arsenopyrite, stannite, molybdenite, gold, silver, electrum, hessite, uraninite, magnetite, tetrahedrite, tennantite, gudmundite, boulangerite, bournonite, pyrargyrite, niccolite, gahnite, ullmannite, breithauptite, nisbite, bismuth, antimony [1,12,16,23,33,38].
Ore mineral photo 1		Ore mineral photo 2
Ore mineral photo 3		Ore mineral photo 4
Gangue	Diopside, tremolite, baryte, quartz, dolomite, rutile, graphite, tourmaline, fluorite [1].
Zoning	The Lampinsaari lode: Zn shows the highest grades in the central and lower, Cu in the central and Pb in the lower parts of the lode [1]. Ag follows Pb throughout the deposit; there are separate, disseminated, Pb-Ag-Au mineralisations in the area between the Zn lodes and black shale [1,28]. Pyrrhotite-rich margins in the pyrite lodes [1]. A separate U-P rich horizon [4,17].
Ore composition	Click here	Ore mineral compositions	Click here
Primary structures	Bedding in greywacke and dolomite, and, locally, clastic texture in the greywacke; banding the Zn lodes? [1,11].
Ore fabric	Massive banded and non-banded, and disseminated sulphide ore with common sulphide±sulphosalt veins [1,11,27]. Grain size of ore minerals is 0.05–1 mm [1]. Pyrite is commonly euhedral and forms porphyroblasts up to 10 cm in diameter (esp. in the pyrite lodes) [1].
Enriched components	Ore, enriched: Ag, As, Au, Ba, Bi, Mg, Pb, S, Sb, Se, Zn, depleted: Ca, P, immobile(?): Co, Ni [1,3]. Cordierite gneiss, enriched: B, Cu, Fe, Mg, S, Zn, depleted: Ca, K, Na, Si (interpreted from [1]).
Geothermo- and barometry	Sphalerite: 5.8–8.0 kbar (mean: 6.8 kbar) [21]. Remobilisation, according to sphalerite, at 570°C [1].
Ore fluid
Stable isotope data	δ13C in black shale: -16.08 per mill reflecting an effect of alteration into the originally biogenic C-isotope ratio [2]. δ34S, in footwall greywacke: +0.5 – +0.9 per mill (pyrite), in disseminated Cu lode: +2.2 – +4.8 per mill (pyrite),+3.2 – +5.7 per mill (pyrrhotite) [4]. Average values of δ34S: in black shale -5.6 per mill (pyrrhotite), in Zn ore +7.5 per mill (sphalerite, pyrite, pyrrhotite); cordierite gneiss: +8.5 per mill (both pyrite and pyrrhotite) [1].
Pb isotope data	Model age, from galena: 2120 or 2070 Ma; from microcline of cross-cutting dyke: 1860 Ma [1], or 1930–1960 Ma [4]. Ore galena: 1918 or 1925 Ma [22].
GEOLOGY
Regional geology map 1		Regional geology map 2
Local geology map 1		Local geology map 2
Geological setting	The deposit is in an anticline, in the SW limb of a d2 fold where the hosting sequence dips at 40–45° to the SE and the fold axis dips at 30–40° to the SW, in the hinge and limb of a side fold of the main anticline fold [38]. The deposit is in a 500 m thick, E–W striking sequence of 'arenaceous' and calcareous (skarn) rocks located in a mica schist-dominated synform (cf reference 38!) and is cut by several SE-trending faults [1,25,27,28,33]. The full length of the Lampinsaari or Vihanti-type rock sequence is, at least, 60 km [14]. The host volcanic sequence is composed of a bimodal complex of low- to medium-K rhyolites, transitional between calc-alkaline and tholeiitic, and sub-alkaline low- to medium-K tholeiitic basalts and basaltic andesites. Trace element chemistry of the volcanic rocks indicates a mature island arc setting [43]. The deposit is in an overturned monocline of a drag-folded volcanic sequence [12,17]. The Zn and Cu lodes are chiefly in the diopside skarns and pyrite lodes in the 'arenaceous rocks' of the sequence [1,17,28]. The 'arenaceous rocks' are in fact volcanic or, at least, of volcanogenic material and located in a formation characterised by turbiditic mica schists, and are 1.90–1.88 Ga in age [17,25,31]. The ore-hosting sequence also contains a bed of phosphoritic tuff(ite) in the same stratigraphic horizon as the pyrite lodes [2,3,4,12,17,28].
Major host rocks	Rhyodacitic porphyry [25].
Minor host rocks	Skarns [25], codierite gneiss (= subvolcanic sill) [38].
Intrusives	Early- (1900 Ma) and synorogenic (1875 Ma) gabbroids and granitoids surround and intrude the mica-schist area hosting the ore sequence [1,22,24,38]. Mafic dykes occur in the sequence as conformable and cross-cutting units [1]. Felsic to intermediate porphyry dykes, parallel to the local faults, cut across the ore and its host rocks and, also, the mafic dykes [1]. There are, in addition, granitic, more coarse-grained dykes which represent the latest intrusives in the area [30]. The local quartz-feldspar porphyries and cordierite-sillimanite gneisses, which cut across the local volcanic and sedimentary units, are interpreted as partially altered subvolcanic intrusions [37,38]; this intrusion in at Lampinsaari 5–60 m thick and subconformable in the hosting sequence [38].
Outcrop photo 1		Outcrop photo 2
Outcrop photo 3		Outcrop photo 4
METAMORPHISM AND DEFORMATION
Metamorphic history	Peak regional metamorphism at about 1876±2 Ma [2,3,5] related to the intrusion of synorogenic, 1.89–1.87 Ga, granitoids [31].
Metamorphic grade	Transitional between amphibolite and granulite facies [25] or upper-amphibolite facies [1,2], peaked at about 6.8 kbar [21] and 630±10°C [25]. Upper-amphibolite facies (Garnet-cordierite-K feldspar-biotite grade) [31].
Metamorphic mineral assemblages	Mica schist: quartz-biotite-plagioclase ± hornblende, tremolite, cummingtonite, K feldspar, garnet, cordierite, sillimanite, corundum, tourmaline [1]. Black shale: quartz-plagioclase-phlogopite-tremolite-K feldspar-pyrrhotite-pyrite-graphite [1]. Greywacke (= felsic to intermediate volcanic rock) [12,20]: quartz-biotite/phlogopite-plagioclase ± sulphides, hornblende, diopside, tremolite [1]. Cordierite gneiss: quartz-phlogopite-plagioclase ± sulphides, K feldspar, sillimanite [1]. Dolomite: Biotite-dolomite-calcite-diopside-tremolite-olivine-clinohumite-garnet-pyrrhotite [1]. Tremolite skarn: tremolite-quartz-plagioclase-phlogopite-calcite-dolomite-pyrrhote-pyrite ± talc, tourmaline, scapolite, baryte, fluorite, corundum [1]. Diopside skarn: dioside-quartz-plagioclase-phlogopite-calcite-dolomite-pyrrhote-pyrite ± talc, tourmaline, scapolite, baryte, fluorite, corundum [1].
Metamorph photo 1		Metamorph photo 2
Deformation history	The regional D1 and D2 possibly produced flat-lying nappes and isoclinal folding – these are not visible locally; the regional D3 was related to NE-SE compression and peak metamorphism (possibly at ca 1884 Ma), produced subvertical folding with a dominantly NW-trend; the regional D4 was related to N-S compression and produced and remobilised large-scale (>100 km long) strike-slip shear and fault zones; post-D4 brittle faulting took place in several stages acoss the region [37]. The D4 possibly took place at ca. 1784 Ma [42].
Structure photo 1		Structure photo 2
ALTERATION
Regional alteration	Formation of cordierite and skarn rocks [1]. Skarnified zones common at the contacts between dolomites and greywackes, and skarns and greywackes [1,11].
Local alteration	Cordierite gneiss, derived by cordierite±sillimanite±Kfeldspar alteration form the subvolcanic quartz porphyry, is abundant in the W and upper parts and dominates in the hanging wall (there, several tens of metres thick) of the ore-hosting rock sequence [1] (is this the original chlorite±clay mineral zone of alteration??; in any case, it is a Mg-Al-B-enriched rock). Skarns are the most common immediate wallrocks and may, perhaps, show signs of Mg metasomatism in the form of phlogopite or cordierite formation [1]. Also, the dolomites may be Mg-metasomatic derivates of sedimentary/biogenic limestones [25].
Alteration figure 1		Alteration figure 2
Alteration figure 3		Alteration figure 4
Post-mineralisation modifications	Regional metamorphism and polyphase deformation with significant increase in the grain size of the sulphides and, possibly, increase in the thickness of the Zn-lodes by deformation [1,2,12,13,25]. Folding and multi-stage transverse faulting has significantly modified the form of the lodes [1]. Local remobilisation of the sulphides and, especially, sulphosalts into veins [1]. During deformation, the ore and skarn rocks have, in many areas, behaved in a plastic manner whereas the arenaceous interlayer have been much more competent and broken into small fragments within the ore-skarn matrix [1].
TIMING	1922±6 Ma zircon U-Pb for host rock [36]. Between about 1960 and 1930 Ma [4]. The sulphides were formed at about 1900 Ma [22,24].
SUPERGENE ALTERATION	In the uppermost parts of the deposit, replacement of pyrrhotite by pyrite, marcasite and limonite and, very locally, formation of chalcosite [1]. Note the conflicting timing information given for the host rocks in 'Geological setting'.
GENETIC MODEL	Submarine felsic-dominated volcanic and subvolcanic activity produced an hydrothermal system which produced, as chemical sediments, the sulphide deposit, carbonate rocks and the U-P rich metasediments [12,20,25,30]. The host formation was originally a single volcanogenic horizon with two main cycles of sulphide precipitation: 1. Fe-sulphides and 2. sphalerite [17]. Early NW- and NE-trending shear and fault zones, located near the margins of the gabbros in the region, may have behaved as conduits for mineralising fluids and even magmas [30]. According to [34], the mineralising fluids may have precipitated the metals below a cap rock formed by low-permeability black shale unit.
GENETIC TYPE	Epigenetic, submarine	References	[38]
Alternative genetic type 1	VMS	References	[2,12,25]
Alternative genetic type 2		References
GENETIC TYPE	Syngenetic, felsic volcanism- and sediment-related, stratabound [2,12,25]. [38].
Schematic model 1		Schematic model 2
References 1. Rouhunkoski, P. 1968. On the geology and geochemistry of the Vihanti zinc ore deposit. Bulletin de la Commission Geologique de Finlande 236. 121 p. 2. Loukola-Ruskeeniemi, K., Kuronen, U. & Arkimaa, H. 1997. Geochemical comparison of metamorphosed black shales associated with the Vihanti zinc deposit and prospects in western Finland. Geol. Surv. Finland, Special Paper 23, 5–13. 3. Rehtijärvi, P. 1984. Distributions of phosphorus, sulphur and sulphur isotopes in a strata-bound base metal deposit, Kangasjärvi, Finland. Geol. Surv. Finland, Report of Investigation 65. 16 p. 4. Rehtijärvi, P., Äikäs, O. & Mäkelä, M. 1979. A middle Precambrian uranium- and apatite-bearing horizon associated with the Vihanti zinc ore deposit, western Finland. Economic Geology 74, 1102–1117. 5. Vaasjoki, M., Äikäs, O. & Rehtijärvi, P. 1980. The age of mid-Proterozoic phosphatic metasediments in Finland as indicated by radiometric U-Pb dates. Lithos 13, 257–262. 6. Laatio, G. 1952. Vihanti. Geol. Surv. Finland, Report Dc N:o 29. 4 p. (in Finnish) 7. Kahma, A. 1950. Yhteenveto geologisen tutkimuslaitoksen suorittamista tutkimuksista Lampinsaaren sinkkiesiintymällä Vihannissa. Geol. Surv. Finland, Report M17/Vti-50/3. 9 p. (in Finnish) 8. Vaasjoki, O. 1946. Vihannin näytteiden malmimineraalikokoomus. 3 p. Geol. Surv. Finland, Report M17/Vti-46/3. (in Finnish) 9. Anon. 1958. Selonteko hakemusten alaisten kaivospiirien Lampinsaari 9–16 alueilla suoritetuista tutkimuksista ja niiden tuloksista. Outokumpu Oy, Vihanti mine Report. (in Finnish) 10. Mikkola, A. 1949. Vihannista lähetetyt kansannäytteet. 2 p. Geol. Surv. Finland, Report M17/Vti-49/2. (in Finnish) 11. Mikkola, A. 1947. Lampinsaaren kiisumalmin kairasydänten tutkiminen. Geol. Surv. Finland, Report M17/Vti-47/1. 7 p. (in Finnish) 12. Rauhamäki, E., Mäkelä, T. & Isomäki, O-P. 1980. Geology of the Vihanti mine. In: Häkli, T.A. (ed.) Precambrian Ores of Finland: Guide to Excursions 078 A+C, Part 2 (Finland). Espoo: Geol. Surv. Finland, 14–24. 13. Lång, K., Gaál, G. & Starostin, V. 1984. Structural and petrophysical features, some Precambrian stratabound base metal deposits of Finland (Outokumpu, Vihanti, Riikonkoski). In: 27th International Geological Congress = 27-j mezdunarodnyh geologiceskij kongress, Moskva, 4–14 avgusta: Tesizy = Abstracts. 6, 186–187. 14. Rauhamäki, E. 1979. Vihannin kaivoksen uraani-fosforimineralisaatio. In: Parkkinen, M. (ed.) Uraaniraaka-ainesymposiumi (1979). Vuorimiesyhdistys. Sarja B 27, 65–79. (in Finnish) 15. Björklund, A., Kontio, M. & Nikkarinen, M. 1976. Vihanti: the geochemical response of bedrock and ore in the overlying till. Journal of Geochemical Exploration 5, 370–373. 16. Pelkonen, K. 1987. Hopeamineraalien esiintymisestä ja rikastettavuudesta Vihannin malmissa. Summary: Silver minerals in the Vihanti ore deposit and their behaviour in concentration process. In: ed. H. Kauppinen, R. Blomqvist, H. Laapas et al. Tuotantomineralogian seminaari 16.1.1986 TKK:n Vuoriteollisuusosastolla. Vuorimiesyhdistys Sarja B 38, 44–56. 17. Kousa, J., Luukas, J., Mäki, T., Ekdahl, E., Pelkonen, K., Papunen, H., Isomäki, O-P., Penttilä, V-J. & Nurmi, P. 1997. Geology and mineral deposits of the central Ostrobothnia. Geol. Surv. Finland, Guide 41, 43–67. 18. Iisalo, E. 1995. Vihannin karttalehden 2434 vanhan moreeniaineiston uudelleen analysointi ICP:llä, tulosten vertailu ja anomaliat. Geol. Surv. Finland, Report S/41/2434/95/1. 16 p. (in Finnish, 10.7 MB) 19. Kauranne, L-M. 1979. Vihannin karttalehtialueen geokemiallisen kartoituksen tulokset. Summary: The results of the geochemical survey in the Vihanti map-sheet area. Explanation for geochemical maps, Sheet 2434. Geol. Surv. Finland. 55 p. 20. Lestinen, P. 1983. Sulphide deposits of central Finland. Outokumpu, Pyhäsalmi, Vihanti. X IGES – III SMGP Symposium, 1983. Excursion Guide. Espoo: Geol. Surv. Finland. 9 p. 21. Törnroos, R. 1982. Sphalerite geobarometry of some metamorphosed sulphide ore deposits in Finland. Geol. Surv. Finland, Bulletin 323. 42 p. 22. Vaasjoki, M. 1981. The lead isotopic compositions of some Finnish galenas. Geol. Surv. Finland, Bulletin 316. 30 p. 23. Sotka, P. 1981. Vihanti: Välisaaren ja Isoahon malmimineraalien koostumuksesta. Outokumpu Oy Exploration, Report 070/Vihanti/PMS/1981. 2 p. (in Finnish) 24. Vaasjoki, M. & Sakko, M. 1988. The evolution of the Raahe-Ladoga zone in Finland: isotopic constraints. Geol. Surv. Finland, Bulletin 343, 7–32. 25. Papunen, H. (ed.) 1990. Sinkkiprojektin loppuraportti. Univ. of Turku, Inst. of Geology and Mineralogy, Publ. 22. 143 p. (in Finnish) 26. Tontti, M., Koistinen, E. & Seppänen, H. 1981. Vihannin Zn-Cu-malmivyöhykkeen geomatemaattinen arviointi. Summary: Geomathematical evaluation of the Vihanti Zn-Cu ore zone. Geol. Surv. Finland, Report of Investigation 54. 58 p. 27. Isokangas, P. 1954. The Vihanti zinc deposit. In: Aurola, E. (ed.) The Mines and Quarries of Finland. Geol. Surv. Finland, Geoteknillisiä julkaisuja 55, 29–32. 28. Autere, I., Pelkonen, K. & Pulkkinen, K. 1991. Outokumpu Finnmines Oy:n Vihannin kaivos. Summary: Outokumpu Finnmines Oy's Vihanti zinc mine. Vuoriteollisuus 49, 81–88. 29. Wennervirta, H. 1968. Litogeokemiallinen tutkimus, Vihannin malmikompleksi. Outokumpu Oy Exploration, Report 061/2434 05/604/HW/68. (in Finnish) 30. Kuronen, U. 1988. Ajatuksia vuosina 1984–1987 Vihannin alueella suoritetuista tutkimuksista. Outokumpu Oy Exploration, Report 020/2434/UOK/88. (in Finnish) 31. Korsman, K. (ed.) & Glebovitsky, V. (ed.) 1999. Raahe-Ladoga Zone structure-lithology, metamorphism and metallogeny: a Finnish-Russian cooperation project 1996–1999. Map 2: Metamorphism of the Raahe-Ladoga Zone 1:1000000. Geol. Surv. Finland. 32. Salli, I. 1958. Vihanti. Geological Map of Finland 1:100000. Pre-Quaternary Rocks, Sheet 2434. Geol. Surv. Finland. 33. Salli, I. 1965. Pre-Quaternary Rocks of the Pyhäjoki and Vihanti Map-Sheet areas. Geological Map of Finland 1:100000. Explanation to the Maps of Pre-Quaternary Rocks, Sheets 2432–2 434. Geol. Surv. Finland. 52 p. 34. Loukola-Ruskeeniemi, K. 1999. Origin of black shales and the serpentinite-associated Cu-Zn-Co ores at Outokumpu, Finland. Econ. Geol. 94, 1007–1028. 35. Lahtinen, R., Korja, A. & Nironen, M. 2001. Evolution and metallogeny if the Paleoproterozoic Svecofennian Orogen. In: Williams P.J. (ed.) 2001: A Hydrothermal Odyssey. May 17–1 9th, 2001,Townsville. Extended abstracts. EGRU and JCU. 110–111. 36. Nikander, J. & Luukas, J., Ruotsalainen, A. & Kousa, J. 2002. Kallioperä- ja malmitutkimukset Vihannin Vilmingon ja Rantsilan Pelkoperän välisellä alueella vuosina 1993–2002. Geol. Surv. Finland, Report M 19/2434, 3412/2002/1/10. 71 p. (in Finnish, 4.9 MB) 37. Luukas, J., Kousa, J., Nikander, J. & Ruotsalainen, A. 2004. Raahe-Laatokka –v yöhykkeen luoteisosan kallioperä Länsi-Suomessa. Geol. Surv. Finland, Report M10.4/2004/2. 6–37. (in Finnish, 17.1 MB) 38. Nikander, J., Luukas, J. & Ruotsalainen, A. 2004. Vihannin alueen massiivisten sulfidimalmiesiintymien geologia ja malminmuodostus Raahe-Laatokka –vyöhykkeellä Länsi-Suomessa. Geol. Surv. Finland, Report M10.4/2004/2. 38–60. (in Finnish) 39. Iisalo, E. 2004. Moreenin stratigrafia ja geokemia Raahe-Laatokka –vyöhykkeen luoteisosassa, Länsi-Suomessa. Geol. Surv. Finland, Report M10.4/2004/2. 61–72 p. (in Finnish) 40. Iisalo, E. 2004. Moreeni-, rapakallio- ja kallionäytteiden geokemialliset erikoispiirteet Vihannin alueella, Länsi-Suomessa. Geol. Surv. Finland, Report M10.4/2004/2. 73–89 p. (in Finnish) 41. Iisalo, E. 2004. Geokemialliset malmiviitteet Vihannin alueella, Länsi-Suomessa. Geol. Surv. Finland, Report M10.4/2004/2. 90–108 p. (in Finnish) 42. Kousa, J., Huhma, H. & Vaasjoki, M. 2004. U-Pb –ajoitukset eräistä magmasyntyisistä kivistä Pohjois-Pohjanmaalta, Raahe-Laatokka –vyöhykkeen luoteisosasta. Geol. Surv. Finland, Report M10.4/2004/2. 127–141. (in Finnish) 43. Weihed, P. & Eilu, P. 2005. Fennoscandian Shield – Proterozoic VMS deposits. Ore Geology Reviews 27, 324–325. 44. Nikander, J., Luukas, J. & Ruotsalainen, A. 2005. Vihannin Lampinsaaren ympäristön ja Kuuhkamon kairaukset karttalehdellä 2434 05 vuosina 2005–2005. Summary: Drillings in the Lampinsaari area and in Kuuhkamo in Vihanti on the map sheet 2434 05, during the years 2004–2005. Geol. Surv. Finland, Report M19/2434/2005/2/10. 14 p. (in Finnish, 1.3 MB) 45. Outokumpu Oy. 1992. Outokumpu Oy, internal report.
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