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Tungsten potential in Greenland
No. 25 - February 2014
Tungsten-associated mineralising sys-tems are evident in central East andSouth Greenland and present in sever-al other regions of Greenland. This isone of the conclusions from a work-shop on the assessment of undiscov-ered tungsten deposits that was heldin December 2013. The highest rankedtracts, mineralisation types and grade-tonnage estimates from theworkshop are briefly summarised here.
Introduction
Tungsten (W) has recently gained a lot ofinterest and is in several resource-criticalitystudies regarded as a critical metal withsignificant economic importance and sup-ply risk. Tungsten possesses some uniqueproperties such as high-tensile strength athigh temperatures, low expansion coeffi-cient, very high density, and high thermaland electrical conductivity. Properties thatmake it impossible to substitute in particu-lar industrial applications such as hardmetals used for cutting, drilling and wear-resistant parts or coatings, or specialiststeel and other alloys for e.g. high-speedsteel, heat-resistant steel and tools wherehardness and strength are required over awide temperature range. The largestknown deposits of tungsten mineralsoccur in China, Canada, UK and Russiawith China being the world’s dominatingproducer for many years with 64% of theglobal tungsten reserve (2010 figures).
A workshop on the ‘Assessment of thetungsten potential in Greenland’ wasarranged by the Geological Survey ofDenmark and Greenland (GEUS) and theMinistry of Industry and MineralResources (MIM) in December 2013. The purpose of the workshop was toassess the possible presence of undiscov-ered tungsten deposits in the top 1 km ofthe crust in Greenland and to rank themost prospective areas. The proceduresfor the assessment and ranking of theindividual tracts were designed to comply,as much as possible, with the ‘GlobalMineral Resource Assessment Project’
(GMRAP) procedures defined by the USGeological Survey (USGS). One furtherobjective of the workshop was to stimu-late new exploration campaigns inGreenland.
This edition of Geology and Ore highlightsthe main results from the workshop,including descriptions of the most impor-tant tungsten provinces in Greenland,their known tungsten occurrences and theresulting potential for undiscovered tung-sten deposits within these provinces. Amore comprehensive GEUS survey reportdocumenting the results from the work-shop will be available mid-2014.
The methodology applied
The evaluation of the potential for undis-covered tungsten deposits in Greenlandwas carried out according to the standard-ised process utilised in the GMRAP. In thisprocess, an assessment panel of expertsuse all available knowledge and data for aspecific region (tract) to assess the possi-bility of finding new undiscovereddeposits within this tract. The assessmentpanel for the tungsten evaluation consti-tuted twelve geologists from the USGS,GEUS, MIM and private exploration com-panies; each with specific knowledge onaspects of the geology of Greenlandand/or expertise in tungsten deposits.Each tract was defined from the surfaceto 1 km’s depth. The members of theassessment panel made their individualestimates (bids) of the number of undis-covered deposits they believed could befound under the best circumstances in atract. A panel discussion of the bids led to
a consensus bid, which was used as inputto a statistical simulation. Based on estab-lished grade-/tonnage models of knowntungsten deposits worldwide this simula-tion can provide a prediction on howmuch undiscovered ore and tungstencould be found within a tract. The con-sensus bids and predicted number ofundiscovered tungsten deposits per tractare shown in the table on page 5.
Types of tungsten mineralisation
Regardless of the classification, economictungsten deposits are invariably linked togranitic rocks. Provided granitic magmashave undergone the appropriate evolu-tion, leading to progressive enrichment intungsten, these magmas have the poten-tial to generate economic tungstendeposits. Depending on the local geologi-cal setting, namely structural frameworkand type of country rocks, two differenttypes of deposits can be formed: tungstenvein-type and/or tungsten skarn-typedeposits. However, it should be noted thatthere is a gradation between these twodeposit types, and very often both can bepresent in the same district or region.
While only these two deposit types wereassessed during the workshop, a variety ofadditional tungsten deposit types hasbeen described in the literature. However,some have no or only minor economicinterest, such as the brine/evaporite, peg-matite and placer deposit types. The inter-est in these deposit types is very limitedand no grade-tonnage models are avail-able for them, so these were not assessed.
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4 Tungsten potential in Greenland
Deposit type
Tungsten vein
Tungsten skarn
Tonnage ore
560,000
1,100,000
Tungsten gradeWO3 %
0.91
0.67
Number of deposits
16
28
Worldwide summary statistics for the mean tonnage and grade for tungsten vein and skarndeposits. Based on data from Cox (1986) and Cox & Bagby (1986).
Other proposed deposit types can beaggregated to other, more encompassingtypes. For example, the breccia and stock-work deposit types can be considered tobe part of the vein-type deposits, forwhich a grade-tonnage model exists. The stratabound tungsten deposit type,for which some authors propose anexhalative origin, was not assessed. This was due to their enigmatic and con-troversial nature and the absence of a
grade-tonnage model. Nevertheless, ashort review of the tungsten mineralisa-tions in the Nuuk region, which have beeninterpreted by some authors to corre-spond to this deposit type, is included inthis edition of Geology and Ore.
Worldwide, the vein- and skarn-types aresignificant in terms of economicallyexploitable reserves: vein-type, includingstockwork (44%) and skarn-type (48%).
Grade-tonnage models have been devel-oped by the USGS for these types ofdeposits through the compilation of pub-lished data from known deposits that areformed through the same genetic processand can be mined and processed usingsimilar methods. Table on page 2 outlinesthe mean tonnage and tungsten gradefrom the grade-tonnage model. The skarndeposits tend to be larger but of lowergrade than the vein-type deposits.
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T U N G S T E N P O T E N T I A L I N G R E E N L A N D
Vein type Skarn type
Typical sizesVeins: 10s to 100s of Kt.; groups of veins, stockworks: Mt to 10s of Mt
Most exploitable deposits contain >10,000 tons of W
Typical grades 0.3 to 1.5% WO3 for veins, lower for stockworksUnderground mines generally grade >0.4% WO3, and >1% in remote areas
Greenland examples
Ymer Ø (central East Greenland), 0.075 Mt @ 2.5% WO3 & 0.042 Mt @ 0.7% WO3; Scheelitdal, Galenadal and Trekantgletscher(central East Greenland), No resource estimate
Knivbjergdal and Kalkdal (central East Greenland), no resource estimate
Foreign examples
Panasqueira (Portugal), 31 Mt @ 0.3% WO3; Mount Carabine (Australia), 35 Mt @ 0.1% WO3; Hemerdon (Cornwall, UK), 42 Mt @ 0.43% WO3; Appalachians: Burnthill (NB, Canada), 4 Mt @ 0.12% WO3
Shizhuyuan (China), 170 Mt @ 0.33% WO3 (including a stockwork); Tymyauz (Russia), 50.8 Mt @ 0.6% WO3; Sangdong (South Korea), ~20 Mt @ 1.0% WO3; King Island (Tasmania), 14 Mt @ 0.8% WO3; Mactung (NWT), 33.0 Mt grading 0.88% WO3; Cantung (NWT), 1.7 Mt @1.17% WO3; Tabuaço (Portugal), 2.7 Mt @ 0.56% WO3
Tectonic contextCollision zones, continental arcs, continental rifts; granitic plutons derived from melting of continental crust
Orogens; continent-continent collision zones / subduction zones?
AgeLate-orogenic to anorogenic, mostly Late Palaeozoic, Mesozoic and Cenozoic
Syn-orogenic (++) to late-orogenic (-), mainly middle Palaeozoic to Late Cretaceous
Geochemistry
Granites; strong fractionation, A- or S-type granites, enriched in lithophile and volatile elements, ilmenite-series if related to Sn mineralisation ('specialised granites')
Quartz diorite, quartz monzonite or granodiorite, calc-alkaline trend; type I or type S
Texture Presence of aplites, porphyry, granophyric or micrograph. texture, comb-layered quartz
Coarse- to medium-gr. intrusions, porphyry texture, K feldspar megacrysts, aplites and pegmatites
Emplacement depth; size1-4 km; cupolas of batholith, small isolated cupolas/plutons, small subvolcanic intrusions
5-15 km; ranging in size from stocks to large batholitic plutons
Alteration
Greisen in upper parts: Li-, F-, and B-bearing minerals (topaz, tourmal., fluorite, micas), ± albite, microcl., chlor., qtz, dissem. sulfides; pervasive albitisation in deepest parts
Generally unaltered but intrusive borders can show argillic or greisen alteration
LithologyNo typical host rock, but often in thick, non-carbonate sedimentary piles - sandstone, shale and metamorphic equvialents
Platform carbonates and pelites, recrystallised during contact metamorphism
AlterationGreisen selvages around veins; greisenisation may be pervasive throughout host rock in stockworks
Metasomatism of marbles and calc-silicate hornfels = skarns; prograde phase: pyrox., garnet, calcite, dolom., qtz, vesuv., wollast.; retrograde phase (highest W grades): hornbl., biot., plag., epid., sphene, chlor., actin., apatite
Location and shape
Location: contained within parent magmatic rock or surrounding host rocks; tensional fractures in granitic plutons and their wallrock; shape: veins <1 cm to several m-thick veins, typically 10-20 cm thick, distributed in single veins, narrow vein networks, sheeted vein zones, stockworks, or breccias
Mainly stratabound exoskarns (in recrystallised limestone), with orebodies reaching 100s of m in length (but <15 m in thickness); located 10s of m away from intrusion, along a lithological contact (e.g. limestone/pelite). Contacts and roof pendant of batholith and thermal aureoles of granites that intrude carbonate rocks
Mineralogy
W in wolframite [(Fe,Mn)WO4], but sometimes in scheelite; accomp. by cassiterite, stannite, molybdenite, bismuthinite, chalcopyrite, sphalerite, pyrite, pyrrhotite, hematite, arsenopyrite
W in scheelite (CaWO4); accompanied by chalcopyrite, sphalerite, molybdenite, pyrrhotite, late pyrite, magnetite, native bismuth, bismuthinite
Characteristics of related intrusions
Host rock characteristics
Ore characteristics
Economic and geologic characteristics of the two main types of tungsten deposits
GEOLOGY
ECONOMICS
Economic and geologic characteristics of the two main types of tungsten deposits. Based on data from Cox (1986), Cox & Bagby (1986) and SIDEX(www.sidex.ca).
Descriptive economic and geologic charac-teristics of the two deposit types (referredto as a mineral deposit model – see tableon page 3) were used together with abroader-scaled mineralising system ap-proach to set up the elements that shouldbe evaluated for in each tract.
Vein-type depositsTungsten vein-type deposits tend to be thehigh grade, yet low tonnage deposits. Thesecan often also produce tin and occasionallygold. The primary tungsten mineral tends tobe wolframite, which occurs in quartz veins,
stockworks or breccias, in greisen-graniticand/or metasedimentary country rocks. Thegranitic magmas associated with thisdeposit type are derived from remelting ofcontinental crust and these magmas shouldbe emplaced as small granitic cupolas,rather than large batholiths. Representativedeposits include Mount Carabine (Australia)and Hemerdon (UK).
Skarn-type depositsIn contrast to the tungsten vein-typedeposits, the tungsten skarn-type depositstend to be lower grade but higher tonnage
deposits. Their main tungsten mineral isscheelite, which tends to occur in tabular orlenticular bodies within metasomatised mar-bles and calc-silicate hornfels, at variable dis-tances to granitic intrusions (endoskarns toexoskarns). Representative deposits includethe Shizhuyuan deposits in China andTymyauz (Russia).
The economic and geologic characteristics ofthe two deposit types are described in moredetail in the table on previous page.
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4T U N G S T E N P O T E N T I A L I N G R E E N L A N D
Note:HMCs are obtained usingdiffernt methods, hence W dataare not directly comparable
GEUS, NM, NunaminHMC W ppm
GEUS stream sediment<0.1 mm grain size fractionsamples with W > 2 ppm
Black dots: sample loc
WGS 84 / UTM zone 24N
250 km
W ppmW ppm
688371275230161129105
898062534740342923201713
21.214.111.8
9.98.17.06.96.16.05.04.94.94.14.03.13.02.92.12.0
Left: Stream sediment localities with tungsten values higher than 2 ppm. Right: Heavy Mineral Concentrate (HMC) sample localities collected by GEUS,Nordisk Mineselskab A/S and NunaMinerals A/S. Red ellipses mark areas that are highly anomalous in tungsten. From Steenfelt’s (2013) tungsten work-shop presentation.
Undiscovered tungsten deposits
A total of eight tract groups were definedand assessed for undiscovered vein- andskarn-type tungsten deposits at the work-shop. The tract areas were based on anextraction of granitic intrusions on the1:500 000 (1:250 000 in central EastGreenland) scale geological map. Theseunits were extracted as geo-referencedpolygons. Extensions to known intrusionsor the presence of additional intrusions atdepth are, however, possible elsewhere.Therefore, a buffer of 20 km was putaround the extracted polygons and theresulting polygons were further groupedtogether within larger tracts, consideringsimilarities in known granite ages andgeochemistry, as well as comparable levelsof knowledge/investigation.
The consensus bids on the number ofundiscovered tungsten deposits for bothtypes are summarised in the table below.The eight tract groups cover an area of199,400 km2 in total.
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T U N G S T E N P O T E N T I A L I N G R E E N L A N D
Illoqqortoormiut
Tasiilaq
UummanaqE2
E1
E3
E4NW1
S1
S2
S3
Nuuk
The areas (tracts) assessed for bothvein- and skarn-type tungsten depositsduring the workshop.
Tract name Tract typeTract Area
(km2)N90 N50 N10 N05 N01
Number of unknown deposits
Deposit density
Mean estimate of undiscovered
tungsten resources (metric tons)
Rank
E1_V 11,350 1 1 3 4 6 1.70 1.40 33,000 2
E2_V 24,900 0 0 1 2 3 0.41 0.82 8,400 4
E3_V 4,110 0 0 1 2 3 0.41 0.82 7,900 6
E4_V 66,600 4 6 8 12 15 6.10 2.80 130,000 1
NW1_V 41,160 0 0 0 1 3 0.14 0.56 4,500 8
S1_V 16,420 0 1 3 4 5 1.40 1.50 28,000 3
S2_V 10,290 0 0 1 1 2 0.33 0.62 7,100 7
S3_V 22,960 0 0 1 2 3 0.41 0.82 8,100 5
Total amount of undiscovered resources related vein-type tungsten deposits in Greenland (metric tons) 227,000
E1_S 11,350 1 2 4 5 7 2.40 1.70 82,000 2
E2_S 24,900 0 0 1 2 3 0.41 0.82 14,000 3
E3_S 4,110 0 0 0 0 1 0.03 0.24 980 7
E4_S 66,600 2 5 7 9 13 4.80 2.70 170,000 1
NW1_S 41,160 0 0 0 0 2 0.06 0.37 2,200 5
S1_S 16,420 0 0 0 0 2 0.06 0.37 2,300 4
S2_S 10,290 0 0 0 0 1 0.03 0.24 900 8
S3_S 22,960 0 0 0 0 1 0.03 0.24 1,600 6
Total amount of undiscovered resources related skarn-type tungsten deposits in Greenland (metric tons) 273,980
vein
skarn
Summary statisticsConsensus bid on number of undiscovered tungsten
deposits at different confidence levels
N90, N50, N10, N05, N01 = Confidence levels: a measure of how reliable a statistical result is, expressed as a percentage that indicates, the probability of the result being correct. A confidence level of 10% (N10) means that there is a probability of 10% that the result is reliable.
Summary of consensus bids from the tungsten assessment workshop on the number of undiscovered vein- and skarn-type tungsten deposits in Greenland.
East Greenland potential
Central East and North-East Greenlandwas evaluated as being the area with thehighest number of undiscovered tungstendeposits of both vein- and skarn-type. Thiswas largely attributed to the presence offavourable granitic intrusions and hostrocks for the formation of tungstendeposits, several known tungsten depositsand occurrences in the area and thenumerous geochemical anomalies seen inthe area. At the same time, large parts ofthe area have only seen limited explo-ration activities of which most only havebeen carried out on surface exposures andthe potential for hidden deposits withoutdirect surface expression has not beeninvestigated.
According to Stendal & Frei (2008), isotope analyses of scheelite from EastGreenland indicate a heterogeneous, prob-ably local, source for tungsten, and sup-port a genetic link to Caledonian magmaticactivity. The isotopes also indicate mixingof late waning-stage fluids from the gran-ites and from interaction with wall rocks. Inaddition, the isotopic data indicate that aportion of the rare-earth elements wasderived from fluids that had interactedwith both Archean-Palaeo pro terozoic crys-talline basement and Meso proterozoic-Neoproterozoic sedimentary rocks. Mineraloccurrences associated with fault zonesand late Caledonian veins all show agenetic relationship with Caledonian gran-ite emplacement. Thus, the multi-isotopestudies indicate that tungsten may havebeen deposited from fluids associated withCaledonian granites, which provided heatsources for local hydro thermal circulationcells. Forced into faults, thrusts and frac-tures, the fluids were trapped by domi-nantly Ca-rich sediments.
Tracts E1–E4 are all located within the EastGreenland Caledonides and include UpperProterozoic and Caledonian granites ofmainly S-type origin that are intruding lateProterozoic sediments of the Eleonore BaySupergroup (EBS) and Tillite Group, and byCambro-Ordovician sediments (Hallenstein
& Pedersen 1983). The S-type graniteswere formed by anatexis of schists andparagneisses of the late MesoproterozoicKrummedal supracrustal sequence prior to
or during emplacement of two majorthrust units and subsequent collapse of the orogeny (Kalsbeek et al. 2008).
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$1
$1
$1
E1E2E3E4
GemmedalEremitdal
KnivbjergdalNoa Dal
North Margerie Dal
South Margerie DalYMER Ø
Panoramafjeld
ANDREELAND
SUESSLAND
LYELLLAND
Galenadal & ScheelitdalTrekantgletscher
Randenæs
MILNELAND
East Milne Land
STAUNINGALPER
Roslin GletscherMalmbjerg
Bersærkerbræ
Skjoldungebræ
Kalkdal
JAMESONLAND
LIVERPOOLLAND
TRAIL Ø
HUDSONLAND
Parkinson Bjerg &Blokadedal
E1
E1
E1
E3
E3
E3
E4
E2
20°0'0“W25°0'0“W
30°0'0“W75°0'0“N
76°0'0“N
25°0'0“W
74°0'0“N
73°0'0“N
72°0'0“N
71°0'0“N
70°0'0“N
GEUS stream sedimentW ppm
5 - 1011 - 30
31 - 220
GEUS HMCW ppm
Legend
0 - 100101 - 500
Nordmine HMCW ppm
0 - 100101 - 1000
1001 - 40000
Nordmine HMCScheelite grains
0 - 100101 - 1000
1001 - 7200
Nordmine HMCSn ppm
0 - 100101 - 1000
1001 - 50000Tract area
50 025
Kilometers
Geological map of central East Greenland showing the location of the E1–E4 tracts and selectedscheelite-mineralised areas. Geochemical anomalies of W, Sn and scheelite grains in pan samples(HMC) and from stream sediment samples are also included on the map. For geological legendplease refer to http://data.geus.dk/map2/geogreen.
The following description of the EastGreenland potential is derived fromHallenstein & Pedersen (1983). Numerousscheelite-mineralised areas have beenfound in a 350 km long belt in centralEast Greenland. Outcropping scheeliteoccurrences are thus known from at least12 areas with footprints varying from 1 to20 km2 in size, and scheelite-bearingboulders have been located in anothertwo areas. The location of all areas is indi-cated on the map on page 6. It is possibleto divide the scheelite-mineralised areasinto three groups on account of their geo-logical setting. The groups and theirrespective areas are as follows:
• Scheelite mineralisation in UpperProterozoic metasediments, often spa-tially associated with Caledonian orolder granitic intrusions. The areasassigned to this group are Kalkdal,East Milne Land, Knivbjergdal,Gemmedal and Eremitdal.
• Scheelite mineralisation in the LowerEBG sediments, up to 7 km from out-cropping Caledonian granites. Theareas of this group compriseBersærkerbræ, Skjoldungebræ,Trekantgletscher, Galenadal &Scheelitdal and Randenæs.
• Scheelite mineralisation in fault zonesin Upper EBG sediments without spa-tial relation to granitic rocks. The areasof this group comprise North andSouth Margerie Dal on Ymer Ø,Panoramafjeld & Eleonores Bugt andNoa Dal.
The areas in bold are further described inthe following section:
Kalkdal (Part of the E1-tract)Kalkdal is an EW-trending valley inLiverpool Land with several scheelite min-eralisations occurring within a 20 km2
area of the valley. The geology of Kalkdalcomprises ESE-striking metasedimentsintruded by pinkish biotite granite in thewest and grey foliated granodiorite in the
east. The metasediments are dominatedby biotite-hornblende-garnet schist andparagneiss, with some dolomitic marblebeds and amphibole gneiss. Skarn hasdeveloped in marble when in contact withgranodiorite and in a marble horizon sev-eral kilometres from outcropping intrusiverocks. Skarn does not occur at granite-marble contacts.
Scheelite mineralisation in Kalkdal hasbeen located in the skarns and in a fewpegmatite and quartz veins which cut theskarns. Tungsten contents in hand-sizedsamples may reach 1%, but the overallcontent of the skarn is less than 100 ppm.The scheelite is molybdeniferous.
Lenses of molybdenum-free scheelite min-eralisation, up to several metres long,
occur in the skarn, and are accompaniedby sericitisation of plagioclase and scapo-lite. The lenses contain up to 2% W, butthe tungsten content of the entire skarn isless than 500 ppm. The scheelite-bearingskarn are enriched in lithium (up to 100ppm) and beryllium (up to 100 ppm).
Scheelitdal, Galenadal andTrekantgletscher (Part of the E4-tract)Scattered scheelite mineralisation hasbeen located along 15 km of the westcoast of Alpefjord. The geological settingof this area comprises quartzitic sedimentsof the Nathorst Land Group of the LowerEBS (Neoproterozoic) and Caledonianintrusive granites. Scheelite mineralisationsare known from three localities:Trekantgletscher, at the contact of thelowermost-preserved sediments of the
7
GE
OL
OG
Y A
ND
OR
E
25
/ 2
01
4
T U N G S T E N P O T E N T I A L I N G R E E N L A N D
Time-domain electromagnetic and magnetic survey performed by SkyTEM ApS on Ymer Ø, centralEast Greenland in 2008. Copyright SkyTEM ApS.
Lower EBS and granite in the south of thearea and at Scheelitdal and Galenadalwhich respectively are 1 km and 3 kmstratigraphic higher than the sediments atTrekantgletscher, and which are 5 to 7 kmeast of the outcropping granite.
At Trekantgletscher, scheelite occurs incentimetre- to metre-dimensioned lensesof contact metamorphosed calcareousquartzite – the skarnoid rocks. The lensesare often zoned, with an approximately 1 cm thick, greenish hornblende-diopside-clinozoisite rim and a calcareous core usually dominated by garnet-hornblendeskarnoid. The garnet-hornblende skarnoidcomprises quartz, grossularite, diopside,hornblende, clinozoisite, plagioclase,scapolite and calcite. Most scheeliteoccurs in the garnet-hornblende skarnoid.Tungsten contents of grab samples varyfrom 0.1 to 0.8% W. The average contentof an entire skarnoid lens is only a fewhundred ppm tungsten. The skarnoids arealso enriched in beryllium (300 ppm), tin(200 ppm) and bismuth (100 ppm).
At Scheelitdal, scheelite is associated withconcordant quartz veins. The veins arefrom fifty to several hundred metres apart,are up to 3 m thick, and can be followedfor up to 500 m. In addition to coarse-grained quartz, the veins contain coarse-grained arsenopyrite and rare scheelite ascentimetre large idiomorphic crystals. Thescheelite occurs near the contact to thewall rocks.
In an approximately 5 km2 area south ofGalenadal, quartz veins and fracture zonesare mineralised with arsenopyrite andscheelite. The mineralised veins and frac-ture zones occupy 1 to 2% of the volumeof the sediments. At one locality, moreintense scheelite mineralisation has beenlocated in 2 to 6 m wide, E–W-strikingquartz-vein swarms. The swarms are notcontinuously exposed, but it appears as ifone continues for 800 m along its strike.Detailed field observations of the swarmshave revealed the existence of severalgenerations of quartz veins. The oldest
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veins contain most of the scheelite,whereas arsenopyrite, galena, chalcopy-rite, pyrrhotite and bismuthinite occur inthe youngest veins. Systematic samplingof the vein swarms indicates an averagecontent of 0.1% W and 0.2% As.
North and South Margerie Dal onYmer Ø (Part of the E4-tract)Geochemical anomalies for tungsten andantimony were identified in the streams ofwest Ymer Ø in the mid-seventies byNordisk Mineselskab A/S. Subsequentexploration from 1979–1983 locatedsmall, high-grade scheelite and stibnitelenses. Initial drilling revealed approx.75,000 tons @ 2.5% WO3 at SouthMargerie Dal, and 42,000 tons @ 0.7%WO3 + 108,000 tons with 3.5% Sb atNorth Margerie Dal. Since 2008, theGreenlandic exploration company,NunaMinerals A/S, has made additionalinvestigations on Ymer Ø, including geo-chemical sampling and airborne magneticand electromagnetic surveys to identifypossible new targets.
Margerie Dal is a 20 km long, NNE-strik-ing valley on west Ymer Ø. Scheelite min-eralisation is known in two areas, Northand South Margerie Dal – about 12 kmfrom each other. In Margerie Dal, UpperEBS sediments of the Ymer Ø Group arecut by large EW-striking faults, over 10km long and with throws of 100 to 1000m. The northern blocks are generallydownthrown. Many second-order faults,up to a few hundred metres long, branchoff the main faults. The throws of the second-order faults are up to 100 m, butdiminish away from the main faults. Thesediments of Margerie Dal form part of theeasterly dipping flank of an open anticline.On the structural contour map, it can beseen that the anticline forms a dome culmi-nation on west Ymer Ø.
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Tungsten-mineralised carbonate breccia fromthe Ymer Ø tungsten deposit in central EastGreenland. Photo: 21st North.
Mineralisation in North and SouthMargerie Dal occurs in the 100 m thick,lowermost limestone unit of the Upper EBSas veins in second-order structures. InNorth Margerie Dal, the largest vein con-tains both scheelite and stibnite in a brec-cia zone striking 80° and dipping 75°N.Stibnite predominates in the 65 m of thebreccia zone nearest the main fault. Itoccurs as decimetre-thick massive veinsand as thin veinlets in the hanging wall ofthe breccia zone in the limestone.Scheelite has been observed in the brec-ciated limestone of this 65 m long zone,but only as scattered grains. West of thestibnite-dominated zone, the brecciatedlimestone is mineralised along strike for110 m, mostly with scheelite, but also withstibnite. Sampling of the entire 110 mlong zone indicates contents of 0.8% Wand 2.4% Sb with a thickness averaging 3 m. Dolomitisation and silicification of thelimestone are also present in the brecciazone. Several other mineralised lensesoccur in an overlying limestone unit up to40 m north of the main fault. They are upto 1 m thick, 10 to 15 m long and containabout 1% W but no antimony. The tung-sten (scheelite) occurs as breccia fillings insecond-order fault structures. Similar smallscheelite-mineralised lenses have beenlocated in second-order structures in theoverlying limestone approximately 200 meast of the main mineralisation.
The main mineralisation of SouthMargerie Dal is in a vein in an ENE-strikingbreccia zone, dipping 80°N, and withoutany noticeable amount of displacement.The zone is up to 3 m wide and can befollowed from the bottom to the top ofthe 100 m thick, lowermost limestoneunit. Scheelite occurs as breccia fillings inthe limestone, and is particularly concen-trated in the breccia zone in the lowerhalf of the unit. The tungsten content
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Scheelite and calcite veining from the Ymer Øtungsten deposit in central East Greenland.Photo: 21st North.
averages nearly 3% over an average widthof 2.5 m. Dolomitisation and silicificationare pronounced and correlate well withthe distribution of scheelite.
According to Pedersen & Stendal (1987)the mineralising event on Ymer Ø wascontemporaneous with folding and fault-ing during the Caledonian orogeny. Base-metal and silver mineralisation occurs atthe base of a 1500-m stratigraphicsequence and antimony-gold-tungstenmineralisation is found further up the suc-cession. High-grade scheelite mineralisa-tion is associated with the first majorappearance of carbonaceous limestone,and high-grade stibnite is hosted in theoverlying evaporitic shale-dolomite mem-ber. Precipitation of the ore-forming fluidstook place at temperatures of 170-240°Cfrom saline solutions with 2-6 wt% NaClequivalent. The origin of the hydrothermalsolutions may have been either igneous ormetamorphic; the fluids were probablychannelled to the surface along deep-seated NNW-SSE-striking structures.
South Greenland potential
Based on the regional geology and the dis-tribution of tungsten stream sedimentanomalies, it was decided to divide SouthGreenland into three different tracts S1–S3.
The S1 tract corresponds to a transitionalzone between tracts S2 and S3, within theKetilidian Mobile Belt (Palaeoproterozoic),characterised by the presence of bothJulianehåb batholith and rapakivi intru-sions. Several tungsten anomalies associat-ed with gold and/or arsenic anomalies instream sediments are present in theNanortalik area which also hosts knowngold ± arsenic ± tungsten occurrences.Additionally, the Nalunaq gold mine oper-ated in this same area until 2013. It hasbeen suggested that both tungsten andgold are related to an intrusion-relatedmineralisation continuum. This tract wasconsidered to hold a moderate potentialfor tungsten vein deposits. In contrast,skarn-type deposits were considered to be
insignificant, due to the absence of car-bonate rocks. A typical hydrothermal ele-ment association within the batholith hasbeen described as Au-Bi-W-Cu-Pb-(Mo).
The S2 tract is centred on the southern-most Palaeoproterozoic rapakivi graniticintrusions of the Ketilidian Mobile Belt.These intrusions are mostly emplaced intothe pelite zone, where no carbonate rocksare known. It was considered to have alimited potential for both tungsten veinand skarn deposits.
The S3 tract is centred on the northern-most part of the PalaeoproterozoicJulianehåb batholith of the KetilidianMobile Belt. This batholith is a large com-posite body, which has been deeply erod-ed. The tract also includes the alkalineMesoproterozoic Gardar rift zone, towhich some stream sediment tungstenanomalies, associated with uranium,appear to be related. Furthermore, no car-bonate rocks are known in the area. Nodeposits are known, so it was not consid-ered favourable. As a result, the tract wasconsidered to have a limited potential forboth tungsten vein and skarn deposits.
West Greenland potential
An area which stretches from Maarmorilikto Steenstrup Glacier in North-WestGreenland with stream sediment tungstenanomalies is included in tract NW1.
The NW1 tract includes the ProterozoicPrøven granite batholith which is intrudedinto the Karrat Group metasedimentaryrocks (Palaeoproterozoic), including mar-bles and the basement. Pegmatites andanatectic melt veins are abundant on bothsides of Prøven batholith. It appears how-ever that the granite batholith has beenintensively eroded, so that what is nowexposed corresponds to its roots ratherthan its top, where the more favourableapical zone/cupolas would have beenlocated. As a result, the tract was consid-ered to have a limited potential for bothtungsten vein and skarn deposits.
Stratabound tungsten mineralisation, asscheelite in tourmalinites and maficmetavolcanic rocks, is known from StoreMalene, Sermitsiaq, Storø and Ivisaartoq,in the Nuuk region, southern WestGreenland.
The similarities between the scheeliteoccurrences from the Nuuk region(Archaean rocks) and what has beendescribed at the Mittersill mine (Austria)created some interest in them for a while,before the tungsten price collapse of the1980s. At that time the prevailing view wasthat this type of occurrence is of syngeneticnature, formed after exhalative tungstendeposition on the sea floor. However, morerecently, a number of authors working onMittersill have been arguing that there is alink to granite fluids, the mineralisation isclearly epigenetic and its stratabound char-acter results from subsequent deformation.The same could be the case for the tung-sten occurrences of the Nuuk region,where there is a spatial associationbetween mineralisation and the presenceof pegmatites. In this case, the associationof the mineralisation with pillow lavas, pre-sented as an argument for its syngeneticorigin, could instead simply result fromtheir reactivity during a previous carbonati-sation event. As such, these occurrencesshould rather be compared to skarns.
The highest-grade tungsten occurrencesare found in the Ivisaartoq area. Channelsamples revealed grades of 0.44% WO3
over 2.5 m and 0.48% WO3 over 1.5 m.The scheelite-rich zones can be traced withintervals for more than 10 km along strike.Regardless of the genesis of the tungstenmineralisation found in the Nuuk region, itis unlikely that it can be of economic inter-est due to their intermittency. Because ofthe uncertainty of the genesis of thestratabound tungsten mineralisation, theassessment panel decided not to assess thepotential for undiscovered tungstendeposits. For more information on thetungsten occurrences in the Nuuk regionplease refer to Appel (1990).
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Concluding remarks
Greenland comprises geological environ-ments that are highly prosperous for tung-sten mineralising processes. Consideringthe historically limited exploration activitiesthat have been carried out in many partsof Greenland and the limited amount ofdata and information available, the assess-ment still resulted in an estimate of undis-covered tungsten deposits and an associ-ated tungsten endowment that can beconsidered significant and warrants fur-ther opportunities and exploration.
Key references
Appel, P.W.U. 1990: Tungsten mineralization in
the Nuuk region, West Greenland, GGU Open
File Series 90/4, 51 pp.
Baker, T., Pollard, P.J., Mustard, R., Mark, G. &
Graham, J.L. 2005: A comparison of granite-
related tin, tungsten, and gold-bismuth deposits:
Implications for exploration. Society of Economic
Geologists Newsletter 61, 5–17.
Cox, D.P. 1986: Descriptive model of W skarn
deposits. In: Cox, D.P. & Singer, D.A. (eds): Mineral
deposit models: U.S. Geological Survey Bulletin
1693, 55–57.
Cox, D.P. & Bagby, W.C. 1986: Descriptive model
of W veins. In: Cox, D.P. & Singer, D.A. (eds):
Mineral deposit models: U.S. Geological Survey
Bulletin 1693, 64–66.
Hallenstein, C.P., Pedersen, J.L. & Stendal, H.
1981: Exploration for scheelite in East Greenland
– a case study. In: Rose, A.W. & Gundlach, H.
(eds): Geochemical Exploration 1980. Journal of
Geochemical Exploration 15, 381–392.
Hallenstein, C.P. & Pedersen, J.L. 1983: Scheelite
Mineralization in Central East Greenland.
Mineralium Deposita 18, 315–333.
Harpøth, O., Pedersen, J.L., Schønwandt, H.K.
& Thomassen, B. 1986: The mineral occurrences
of central East Greenland, Geoscience 17, 139 pp.
Kalsbeek, F., Thrane, K., Higgins, A.K., Jepsen,
H.F., Leslie, A.G., Nutman, A.P. & Frei, R. 2008:
Polyorogenic history of the East Greenland
Caledonides. In: Higgins, A.K., Gilotti, J.A. &
Smith, M.P. (eds): The Greenland Caledonides:
Evolution of the Northeast Margin of Laurentia:
Geological Society of America Memoir 202, 55–72.
Pedersen, J. & Stendal, H. 1987: Geology and
geochemistry of tungsten-antimony vein miner-
alization on Ymer Ø, East Greenland. Transactions
of the Institution of Mining and Metallurgy 96,
B31–B36.
Pitfield, P. & Brown, T. 2011: Tungsten com-
modity profile. British Geological Survey, 34 pp.
http://www.bgs.ac.uk/mineralsuk/statistics/mineral
Profiles.html
SIDEX 2002: Table of Economic and geologic char-
acteristics of the two main types of tungsten (W)
deposits. www.sidex.ca
Stendal, H., Grahl-Madsen, L., Olsen, H.K,
Schønwandt, H.K. & Thomassen, B. 1995:
Gold Exploration in the Ketilidian Orogen, South
Greenland. Exploration Mining Geology Journal
4, 307–315.
Stendal, H. & Frei, R. 2000: Gold occurrences
and lead isotopes in Ketilidian Mobile Belt, South
Greenland. Transactions of the Institution of
Mining and Metallurgy 109, B6–B13.
Stendal, H. & Frei, R. 2008: Mineral occurrences
in central East Greenland (70°N–75°N) and their
relation to the Caledonian orogeny–A Sr-Nd-Pb
isotopic study of scheelite. In: Higgins, A.K.,
Gilotti, J.A. & Smith, M.P. (eds): The Greenland
Caledonides: Evolution of the Northeast Margin
of Laurentia: Geological Society of America
Memoir 202, 293–306
Thomassen, B. & Lind, M. 1998: Karrat 97: Mineral
exploration in the Uummannaq area, central West
Greenland. Danmarks og Grønlands Geologiske
Undersøgelse Rapport 1998/62, 63 pp.
Front cover photographClose-up of the tungsten deposit loca -ted at South Margerie Dal/Colinedal onYmer Ø in central East Greenland. Thelayered coloured sequence in the back-ground is the sandstones, mudstonesand carbonates of the Ymer Ø Groupwhich forms the upper part of the Neo -proterozoic Eleonore Bay Super groupwhich hosts the tungsten mineralisa-tion on Ymer Ø. Photo: 21st North.
Ministry of Industry and Mineral Resources (MIM)
Postbox 1601Imaneq 1A, 201
3900 NuukGreenland
Tel: (+299) 34 50 00Fax: (+299) 32 43 02E-mail: [email protected]
Internet: www.govmin.glwww.naalakkersuisut.gl
Geological Survey of Denmark and Greenland (GEUS)
Øster Voldgade 10DK-1350 Copenhagen K
Denmark
Tel: (+45) 38 14 20 00Fax: (+45) 38 14 20 50E-mail: [email protected]: www.geus.dk
AuthorsLars Lund Sørensen,
Bo Møller Stensgaard & Diogo Rosa,GEUS
EditorLars Lund Sørensen, GEUS
Graphic ProductionAnnabeth Andersen, GEUS
PrintedFebruary 2014 © GEUS
PrintersRosendahls • Schultz Grafisk a/s
ISSN2246-3372
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View from Blomsterbugten at Noa Dal on Ymer Ø. Copyright John Pedersen.
