Detailed field and laboratory studies indicate the Shaw Dome area of the Abitibi greenstone belt, Ontario, contains a lower horizon of intrusive komatiitic rocks (LKH), komatiitic dykes, and an upper horizon of extrusive komatiitic rocks (UKH). The LKH is 500–1000 m thick and consists of undifferentiated dunite (45–50% MgO), laterally equivalent wehrlite (20–50% MgO), and differentiated wehrlite–amphibole gabbro sills. A differentiated wehrlite–amphibole gabbro dyke intrudes calc-alkalic volcanic rocks and iron-formation. Undifferentiated wehrlite dykes (17–25% MgO) intrude calc-alkalic volcanic rocks and sulphide iron-formations stratigraphically underlying the LKH and contain xenoliths of those rocks. The UKH is 500–3000 m thick and consists of up to 50 m thick, weakly differentiated komatiites that grade laterally and vertically to thinner, undifferentiated and spinifex textured komatiite (20–35% MgO) and komatiitic basalt (5–20% MgO) flows, and host minor nickel sulphide mineralisation. These vertical and lateral variations are interpreted to be primary komatiitic lithofacies variations in a single intrusive–extrusive stratigraphic sequence. This sequence represents a dyke–sill–lava complex and constrains facies models for komatiitic magmatism–volcanism. The vertical and lateral transition from LKH dunite to wehrlite to wehrlite–amphibole gabbro sills represents the transition from proximal dynamic flow conduits to more static, ponded distal facies in a sub-volcanic magma chamber. The LKH is underlain by a largely hidden system of wehrlite dykes, possibly feeders to the overlying sills. The distribution of UKH undifferentiated, spinifex textured, and brecciated komatiite and komatiitic basalt flows represents the transition from proximal channel to distal sheet flow volcanic facies. Geochemical modelling utilising MELTS suggests that the LKH and UKH are related by liquid–crystal fractionation and accumulation of olivine±clinopyroxene from magma that assimilated variable amounts of calc-alkalic volcanic rocks±iron-formation. Furthermore, the modelling results suggest derivation of dunite and wehrlite and komatiite flows from uncontaminated magma and differentiated wehrlite-amphibole gabbro units and komatiitic basalt flows from contaminated magma. This contrast in degree of contamination is explained by intrusion and eruption of uncontaminated komatiite followed by assimilation of fused crustal material adjacent to magma conduits, fractional crystallisation, and eruption of the contaminated magma as komatiitic basalt. Given the generally accepted relationship of contamination and dynamic/static flow transitions to nickel sulphide mineralisation, komatiitic dyke/sill contacts should be sought and targeted in nickel sulphide exploration.
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