Geology and genesis of Nalunaq Palaeoproterozoic shear zone-hosted gold deposit, South Greenland

Abstract

The Nalunaq deposit is a shear zone-hosted gold deposit characterized by very high grades (up to 5240 g Au/t over 0.8 m). The host rocks are Palaeoproterozoic metabasic rocks of the Nanortalik Nappe, which is part of the Ketilidian Mobile Belt. The Nanortalik Nappe consists of bedded massive pyrrhotite/graphitic chert horizons overlain by fine-grained metabasalts with pillow structures and metadolerites followed by metatuffs and meta-agglomerate. This sequence was intruded by a porphyritic biotite granite (ca 1755-1725 m.y.) and subsequently by rapakivi granites. The gold mineralization occurs in a 0.5-2.0 m wide shear zone consisting of sheeted quartz veins with associated calc-silicate alteration. The mineralized shear zone is exposed for 800 m on the east face and 1200 m on the north face of Nalunaq Mountain. Surface mapping, diamond drilling (78 holes totalling 11 452 m) and adit development (288 m) have shown that the shear zone that hosts the gold-bearing Main Vein is a continuous structure. This structure was subsequently displaced by slightly rotating dextral strike-slip faults. Gold is present mainly as native gold and as minor maldonite. Free gold appears mainly as inclusions in quartz, diopside, plagioclase and as minor inclusions in löllingite and arsenopyrite. Gold also occurs in fractures and at grain boundaries of quartz, löllingite and arsenopyrite. These occurrences of gold indicate that several influxes of gold and/or stages of remobilization took place. The gold grains vary in size from 1 µm to 4 mm and their distribution is irregular, which makes it difficult to estimate the grade of the deposit from 1.5-to 5-kg samples. Fluid inclusions associated with gold in quartz and diopside contain three types of fluids: aqueous, carbonic and mixed carbonic-aqueous. Moderate to highly saline (14-26 wt% NaCl+CaCl 2 equivalent) aqueous fluids with the inferred composition H 2 O-NaCl-CaCl/MgCl±LiCl predominate. The average homogenization temperature is 201°C. The carbonic fluid contains less than 5 mol% CH 4 and has densities in the range 45-60 cm 3 /mole.The proximal alteration minerals (e.g. diopside, Ca-rich amphibole and Ca-rich plagioclase) and opaque assemblages (e.g., löllingite, arsenopyrite and pyrrhotite) show that the deposit was formed under upper greenschist-to amphibolite-facies conditions. The texture of löllingite rimmed by arsenopyrite suggests that the deposit was formed at high temperatures and the gold-mineralized structure was subsequently also active at lower temperatures.The shear zone was formed under ductile conditions and the major emplacement of quartz veins occurred in the subsequent brittle-ductile regime during multiple influxes of fluids. The shear zone clearly postdates the amphibolite-facies regional metamorphism as it is discordant to the metamorphic foliation. This mineralization, together with the similar hypothermal shear zone-hosted gold mineralization at Xutseq on the southeast coast and stream sediments that are generally highly anomalous in gold, indicates that a wi...

Metallogeny of Greenland

“…inclusions (Kaltoft et al, 2000), but a clear distinction between different inclusion generations has not been made.…”

“…18). The shear zones dip moderately to the SE and show a down-dip mineral stretching lineation (Kaltoft et al, 2000;Bell and Kolb, 2013). They record a complex history of early NW-vergent reverse deformation contemporaneous with peak amphibolite facies metamorphism, overprinted by normal deformation during hydrothermal gold mineralization and re-introduction of NW-vergent shearing in discrete duplex structures, displacing the auriferous veins (Bell and Kolb, 2013).…”

“…Arsenopyrite geochemistry is variable, leading to imprecise temperature estimates of 300-600°C (Kaltoft et al, 2000). Along faults and in proximity to felsic dikes, zoisite-muscovite-hematite-pyrite or epidote-calcite alteration assemblages are developed, replacing earlier mineral assemblages during retrograde greenschist facies conditions (Bell and Kolb, 2013).…”

“…18;Kaltoft et al, 2000). The hydrothermal alteration history is complex and starts with an early clinopyroxene-garnetplagioclase-chalcopyrite stage surrounding a system of conjugate 2-10 cm wide felsic veins (Bell and Kolb, 2013).…”

“…The majority of the gold is native (98%), but it also occurs in maldonite (Au 2 Bi) and a number of other gold-bearing sulfosalts (Kaltoft et al, 2000). The gold-quartz veins are controlled by a shear zone system in amphibolite (Fig.…”