Using electron probe microanalyzer (EPMA) and laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS), we analyzed major and trace element compositions of iron oxides from Ni-Cu-PGE sulfide deposits hosted by mafic-ultramafic rocks in northern Fennoscandia, mostly focusing on Finland. The main research targets were the Archean Ruossakero Ni-(Cu) deposit; Tulppio dunite and related Ni-PGE mineralization; Hietaharju, Vaara, and Tainiovaara Ni-(Cu-PGE) deposits; and Paleoproterozoic Lomalampi PGE-(Ni-Cu) deposit. In addition, some reference samples from the Pechenga (Russia), Jinchuan (China), and Kevitsa (Finland) Ni-Cu-PGE sulfide deposits, and a barren komatiite sequence in the Kovero area (Finland) were studied. Magnetite and Cr-magnetite show a wide range of trace element compositions as a result of the variation of silicate and sulfide melt compositions and their post-magmatic modification history. Most importantly, the Ni content in oxide shows a positive correlation with the Ni tenor of the sulfide phase in equilibrium with magnetite, regardless of whether the sulfide assemblage is magmatic or post-magmatic in origin. The massive sulfide samples contain an oxide phase varying in composition from Cr-magnetite to magnetite, indicating that Cr-magnetite can crystallize directly from sulfide liquid. The Mg concentration of magnetites in massive sulfide samples is lowest among the samples analyzed, and this can be regarded as a diagnostic feature of an oxide phase crystallized together with primitive Fe-rich MSS (monosulfide solid solution). Our results show that magnetite geochemistry, plotted in appropriate discrimination diagrams, together with petrographical observations could be used as an indicator of potential Ni-(Cu-PGE) mineralization.
Orthomagmatic sulfide deposits are important sources for base- and precious metals, such as Ni, Cu, Co, and PGE. Experimental studies and empirical observations have shown that sulfides in these deposits are products of segregation of an immiscible sulfide liquid from a silicate liquid (e.g., Naldrett 2004; Fonseca et al. 2008). The sulfide liquid sequesters chalcophile metals from its parental silicate melt, which may lead to the formation of an economically viable ore deposit (e.g., Naldrett 2004; Fonseca et al. 2008). The sulfide mineral assemblage in these deposits typically consists of pyrrhotite, pentlandite, chalcopyrite, and pyrite (Naldrett 2004). These sulfides are commonly associated with iron oxides (e.g., magnetite and Cr-magnetite) because of the capability of sulfide liquid to dissolve significant amounts of oxygen, leading to the crystallization of magnetite together with early-forming Fe-rich monosulfide solid solution (MSS) and later, at lower temperatures, Cu-rich intermediate solid solution (ISS) (e.g., Naldrett 2004; Dare et al. 2012). The amount of dissolved oxygen in a sulfide melt is dependent on the conditions and metal contents of the sulfide liquid. Experimental studies have demonstrated that the solubility of oxygen increases with increasing oxygen fugacity and iron content and decreases with increasing nickel (Ni) and copper (Cu) contents, with the role of Ni being more important than that of Cu in reducing the oxygen solubility of the system (e.g., Lee 1999; Fonseca et al. 2008).
In mafic and ultramafic magma and related sulfide systems, spinels show wide ranges in composition that are controlled by several factors (parental magma composition, mineral assemblages, degree of fractionation of sulfide liquid, temperature, and oxygen fugacity). The parental magmas differ in their degree of differentiation and compatible and incompatible trace element contents, which are reflected in the concentrations of, for example, Cr, Ti, Nb, Al, and V in the spinel phase they crystallize (e.g., Barnes and Roeder 2001; Boutroy et al. 2014).
Due to the high Cr contents of komatiitic magmas, the first oxide to crystallize from related sulfide liquids can be expected to be chrome-bearing spinel. Fonseca et al. (2008) concluded that most massive sulfide liquids behave as open systems in relation to their oxygen content and suggested that the diffusion of oxygen out of sulfide liquid can lead to precipitation of magnetite and/or chromite/Cr-magnetite (Cr-spinel) near or at the boundary between sulfide liquid and silicate liquid. Frost and Groves (1989) observed exactly this type of boundary in the Kambalda Ni sulfide ores (Australia) where Cr-bearing magnetite had formed near the magmatic contact between sulfides and their komatiite host rock. Ewers et al. (1976) concluded that Cr-bearing spinel in Kambalda massive sulfides were crystallized directly from the sulfide liquid. Based on these observations, it is apparent that chromite, Cr-magnetite, and magnetite can crystallize as primary minerals from sulfide liquids in mafic-ultramafic systems.
An additional factor that affects the iron oxide content of Ni-Cu-PGE sulfide ores is the degree of post-magmatic hydrothermal oxidation. There are examples where the bulk of the magmatic sulfide mineral assemblage has been altered to secondary magnetite replacing sulfides and Ni-rich sulfide minerals, such as millerite and violarite (e.g., the Vaara Ni-Cu-PGE deposit, Konnunaho et al. 2013; the Jinchuan Ni-Cu deposit, Yang et al. 2018).
The abundance and composition of oxide phases in magmatic Ni-Cu-PGE sulfide deposits have attracted much attention in recent years due to the advent of new accurate analytical tools for in-situ trace element analysis, especially laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS) (e.g., Dupuis and Beaudoin 2011; Dare et al. 2012, 2014; Boutroy et al. 2014). For example, the study of the Sudbury ore deposits by Dare et al. (2012) showed that all lithophile elements (Cr, Ti, V, Al, Mn, Sc, Nb, Ga, Ge, Ta, Hf, W, and Zr) are compatible into Fe oxide crystallized from sulfide liquid. The concentrations of these elements vary as a function of the fractionation of the sulfide melt (MSS to ISS), thus providing evidence that Fe oxide geochemistry can be a sensitive indicator for the degree of fractionation of the sulfide liquid system. Dupuis and Beaudoin (2011) identified differences in the composition of magnetite between Ni-Cu-PGE sulfide deposits and hydrothermal and sedimentary deposits. Magnetite in Ni-Cu-PGE sulfide deposits is characterized by relatively high Ni and Cr contents. Ward et al. (2018) introduced a discrimination diagram to distinguish magnetites from mineralized and barren mafic-ultramafic systems. Nadoll et al. (2014) studied the composition of magnetite from various types of hydrothermal ore deposits and proposed several discrimination diagrams and elemental concentration boundaries to discriminate between hydrothermal magnetite and igneous magnetite.
In this study, we used laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS) and electron probe microanalyzer (EPMA) to study magnetite and Cr-magnetite compositions (Cr content of > 1 wt.%) in different types of Ni-Cu-PGE deposits in Finland (Fig. 1). The following Archean deposits were studied: the Ruossakero Ni-(Cu) deposit, the Tulppio dunite and related low-grade Ni-PGE mineralization, and the Hietaharju, Vaara and Tainiovaara Ni-(Cu-PGE) deposits. The komatiite-hosted Lomalampi PGE-(Ni-Cu) deposit represents the Paleoproterozoic deposits. In addition, some reference samples from the 1.98 Ga Pechenga (Russia), ~ 0.83 Ga Jinchuan (China) and 2.06 Ga Kevitsa (northern Finland) deposits, and a barren Archean komatiite sequence in the Kovero area (eastern Finland) were studied. The studied deposits have various magmatic and post-magmatic histories, providing a good opportunity to investigate the characteristics and composition of oxide phases formed under different geological conditions and from different parental magma compositions.
Ruossakero Ni-(Cu) deposit
The Archean komatiite-hosted Ruossakero Ni-(Cu) sulfide deposit is located in a greenstone belt of the Rommaeno complex in the northwest part of Finland (Fig. 1). The lowermost unit in the belt consists of mafic-ultramafic volcanic rocks, including komatiitic olivine cumulates and non-cumulate rocks and minor ca. 2.93 Ga sulfide-bearing felsic volcanic rocks, and interlayers of banded iron formation (Karinen et al. 2015; Konnunaho et al. 2015; DigiKP 2018). The rocks were metamorphosed under amphibolite facies conditions (Metamorphism of Finland 2018), and the primary silicate minerals have been replaced by secondary metamorphic minerals. The common silicate minerals in the komatiitic non-cumulate rocks are amphiboles, chlorite, serpentine, talc, and olivine (Konnunaho et al. 2015). The Ruossakero komatiitic olivine cumulate body is the largest ultramafic body in the NW Lapland, Finland, and hosts a disseminated Ni-(Cu) sulfide mineralization (Konnunaho et al. 2015). Disseminated sulfides occur mostly in the central and upper parts of the olivine cumulate body. The sulfide assemblage is dominated by pyrite and millerite (±violarite) with small amounts of chalcopyrite, pentlandite, and pyrrhotite, indicating that the primary magmatic sulfides (pyrrhotite-pentlandite-chalcopyrite assemblages) have been oxidized by low-temperature hydrothermal processes (Konnunaho et al. 2015).
Vaara and Hietaharju Ni-(Cu-PGE) deposits
The Vaara and Hietaharju komatiite-hosted sulfide deposits are located in the Archean Suomussalmi greenstone belt in eastern Finland (Fig. 1). The rock types in the Vaara area consist of ultramafic rocks, phyllites, black schists and sulfide-bearing sericite schists, and tholeiitic basalts. The area is deformed and folded, and felsic volcanic rocks are intervened by cumulate rocks (Luukkonen et al. 2002; Papunen et al. 2009).
In the surface projection, the Vaara ultramafic lens is approximately1 km long and 400 m wide (Konnunaho et al. 2013; Konnunaho et al. 2015). The disseminated sulfide mineralization is hosted by metamorphosed Cr-poor komatiitic olivine mesocumulates (Konnunaho 2016). The deposit contains three separate mineralized sulfide zones (Konnunaho et al. 2015), which vary in thickness from a couple of meters (at the northernmost end) up to ~ 50 m (at the southernmost end). The sulfide assemblage consists of pyrite, millerite, violarite, pentlandite, and a minor amount of chalcopyrite. Interstitial sulfides have been extensively replaced by secondary magnetite. The occurrence of abundant secondary magnetite, Ni-rich sulfides (millerite and violarite), and pyrite and the lack of pyrrhotite indicate operation of low-temperature hydrothermal oxidation processes with a significant loss of sulfur, leading to major upgrading of the original metal tenors of the Vaara deposit (Konnunaho et al. 2013).
The Hietaharju deposit is located 18 km southwest of the Vaara deposit. It is hosted by metamorphosed olivine-pyroxene cumulates of komatiitic basalts, which are surrounded by sedimentary schists. The following lithological units occur in the Hietaharju area: felsic to mafic metavolcanic rocks, komatiitic basalts, and sulfide-bearing metasedimentary rocks, such as phyllites and black schists (Konnunaho et al. 2016). The Hietaharju Ni-(Cu-PGE) deposit is mainly composed of disseminated sulfides with some massive to semi-massive veins and breccia-textured sulfides (Konnunaho et al. 2016) occur also. The host cumulate is ~ 100 m thick and ~ 1 km long and its mineralized part is ~ 200 m long along strike and ~ 50 m wide, extending to a depth of at least 200 m (Konnunaho et al. 2016). Pyrrhotite, pentlandite, and chalcopyrite are the most common sulfide minerals at Hietaharju.
Tainiovaara Ni-(Cu-PGE) deposit
The Tainiovaara deposit is hosted by a komatiitic olivine cumulate body located in one small greenstone belt relicts in the Archean Lieksa complex, eastern Finland (Fig. 1). It is about ~ 180 m long and ~ 80 m wide and hosts a Ni-(Cu-PGE) deposit, which was mined in the 1980s (Pekkarinen 1980; Vanne 1981; Konnunaho et al. 2015). It consists of disseminated sulfides in the metamorphosed, totally serpentinized olivine cumulate body. There is also some small massive to semi-massive and net-textured sulfide accumulations occurring in the bottom part of the Cr-poor olivine cumulate body (Vanne 1981; Papunen 1989; Konnunaho et al. 2015). The major sulfide minerals are pyrrhotite and pentlandite with minor chalcopyrite and pyrite, representing a moderately modified magmatic sulfide assemblage. The Tainiovaara deposit is moderately enriched in Cu and PGE, but not as significantly as in some other Finnish PGE-enriched komatiitic deposits (e.g., Lomalampi, Vaara and Hietaharju), (Konnunaho et al. 2015; Konnunaho 2016).
Tulppio Ni-PGE mineralization
The Archean komatiitic Tulppio dunite body is located in eastern Lapland (Fig. 1) in the Tulppio greenstone belt composed of felsic to ultramafic (komatiitic) volcanic rocks and associated mica schists and gneisses (Juopperi and Vaasjoki 2001; Sorjonen-Ward and Luukkonen 2005). The Tulppio dunite has an approximate surface extension of 1.5 × 4.5 km and is composed of medium-grained olivine adcumulates to mesocumulates, with minor peridotitic to gabbroic cumulates at the contacts of the body. Olivine is well-preserved in the central part of the body, being more altered towards its edges. Based on the maximum forsterite content of olivine, Fo ~ 91, the Tulppio dunite was formed from a low-Mg komatiitic parental magma. Exploration drilling has revealed a weak sulfide-mineralized zone in the middle part of the dunite body (Heikura et al. 2009) with a sulfide mineral assemblage consisting mainly of pyrrhotite and pentlandite.
Lomalampi PGE-(Ni-Cu) deposit
The komatiite-hosted Lomalampi PGE-(Ni-Cu) deposit is situated in the Central Lapland greenstone belt (CLGB; Fig. 1) in northern Finland. The CLGB is composed of sedimentary-volcanic rocks, which were formed during rifting of the Archean craton. The deposition of these Karelian supracrustal rocks took place in intracratonic and cratonic margin settings between ca. 2.5 Ga and 2.0 Ga. Multiple metamorphic and tectonic events related to the Svecofennian orogeny (1.91–1.80 Ga) have affected the CLGB (e.g., Lehtonen et al. 1998; Hanski and Huhma 2005; Lahtinen et al. 2005). The Savukoski Group in the upper part of the stratigraphy is characterized by pelitic metasediments and abundant komatiitic and picritic volcanism (Hanski and Huhma 2005) and hosts the Lomalampi and Kevitsa Ni-Cu-PGE sulfide deposits. The Kevitsa intrusion has a U-Pb zircon age of 2058 ± 4 Ma (Mutanen and Huhma 2001), and the komatiites of the Savukoski Group have a Sm-Nd age of 2056 ± 25 Ma (Hanski et al. 2001), which is consistent with the Re-Os age of 2058 ± 93 Ma obtained for the Lomalampi olivine cumulate body by Moilanen et al. (2019).
The Lomalampi area is composed mostly of komatiites and komatiitic basalts. They were metamorphosed under greenschist to lower amphibolite facies conditions, resulting in a mineral assemblage of serpentine-chlorite-talc ± amphibole in ultramafic rocks. Komatiitic rocks occur as volcanoclastic rock units, thin flow facies units, and several olivine ± pyroxene cumulate bodies. One of these bodies is ~ 30 to ~ 65 m thick and ~ 700 m long and hosts the Lomalampi PGE-(Ni-Cu) mineralization. It represents either a subvolcanic sill or a cumulate part of a thick lava flow. The sulfide mineralization is of low-grade disseminated type and forms a zone varying from a few m up to ~ 40 m in thickness (Törmänen et al. 2016). The main sulfide is pyrrhotite with subordinate amounts of pentlandite and chalcopyrite and trace amounts of sulf-arsenides and di-arsenides. Compared to other occurrences of komatiitic Ni-Cu-PGE mineralization in Finland, the Lomalampi deposit has a low Ni content (~ 0.1 to ~ 0.3 wt.%), slightly elevated Cu (~ 0.05 to ~ 0.1 wt.%), and relatively high PGE concentrations (up to ~ 2 ppm). The Pt/Pd ratio is high, averaging ~ 2.2, as opposed to ~ 0.5 in other Finnish komatiite-hosted Ni-Cu-PGE deposits, being also unique among komatiite-hosted sulfide deposits globally (Konnunaho et al. 2015; Törmänen et al. 2016).
The Kovero komatiites occur in the Archean Kovero greenstone belt (Fig. 1) in eastern Finland (Konnunaho 1999; Huhma et al. 2012). These komatiites (olivine cumulates and non-cumulate rocks) occur as lenses within association with tholeiitic volcanic rocks. The komatiitic olivine cumulates at Kovero are highly altered serpentinites and talc-serpentine rocks. To date, no Ni-Cu-PGE mineralization is known to exist in the area.
Samples and iron oxide petrography
Samples were collected from drill cores at the national drill core archive of the Geological Survey of Finland. Also, samples from previous studies and some reference samples from the rock collection of Oulu Mining School, University of Oulu, were used. From each deposit, one to seven polished thin sections or thick sections (~ 100 μm) were prepared for in-situ microprobe or LA-ICP-MS analysis.
Samples from the Ruossakero deposit contain disseminated sulfides (dominated by pyrite and millerite and variable amounts of pyrrhotite, pentlandite and chalcopyrite) with disseminated subhedral-anhedral magnetite and Cr-magnetite, which occur as sulfide-oxide aggregates (Fig. 2e) and individual oxide grains with various sizes (~ 10–200 μm). Oxides also show other modes of occurrence, including remobilized Cr-magnetite veins with Ni sulfides, altered chromite grains with magnetite rims, and mobilized later-stage magnetite veins. We also found small inclusions of millerite and pentlandite-pyrrhotite in Cr-bearing magnetite grains from the Ruossakero deposit.
The samples from the Vaara deposit contain disseminated sulfides as interstitial blebs of sulfide-magnetite aggregates between serpentine pseudomorphs after cumulus olivine (Figs. 2c and 4b). Magnetite forms mostly anhedral crystals in these mineral aggregates. The sulfides are dominated by pyrite and millerite with minor violarite. Magnetite also forms rims around altered chromite grains. Secondary magnetite after serpentinization of olivine, mobilized later-stage magnetite-sulfide veins, and some ilmenite also occur. The Vaara deposit is a special case as a substantial amount of magnetite has been generated via post-magmatic oxidation of sulfide minerals (Konnunaho et al. 2013) (Figs. 2c and 4b).
The samples from the Hietaharju deposit represent both massive and disseminated mineralization. Massive sulfide samples contain euhedral to rounded, subhedral magnetite grains (Fig. 2a) (diameter ~ 100–500 μm) imbedded in a sulfide mass consisting of pyrrhotite, pentlandite, and chalcopyrite with a very small amount of silicates, whereas in slightly less massive sulfide samples with streaks or blebs of silicates, some Cr-magnetite occurs in association with silicates. Disseminated sulfide samples (pyrrhotite, pentlandite, and chalcopyrite) do not appear to contain magnetite but rather subhedral to anhedral Cr-magnetite varying from ~ 10 to 100 μm in diameter (Fig. 2b). Figure 2b shows an example of a sheared pyrrhotite-pentlandite-chalcopyrite assemblage together with Cr-magnetite. In these samples, most of the oxides are Cr-magnetites, which have a dark core and magnetite rim and most likely were chromites originally. The same samples also have homogenous Cr-magnetite grains with no magnetite rims. In the Hietaharju samples (Fig. 4a), we observed rounded pentlandite-pyrrhotite and chalcopyrite inclusions (~ 5 to 100 μm diameter) in magnetite and also recognized tiny (~ 1–2 μm diameter) platinum-group mineral (PGM) inclusions (Pt-As phase).
From the Tainiovaara deposit, we studied disseminated sulfide samples with pyrrhotite and pentlandite and some chalcopyrite. They contain subhedral-anhedral Cr-magnetite and some magnetite (diameter ~50–500 μm), which occur as sulfide-oxide grain aggregates and also as individual grains. Figure 2d shows an example of sheared disseminated sulfides with magnetite grains. Magnetite also occurs around altered chromite grains. Tainiovaara magnetites could have been originally chromites, which are altered to magnetite, because some grains still exhibit a zoned texture with a slightly darker chromium-bearing core (see Fig. 3e in Moilanen et al. 2019). Nickel sulfide and pyrite inclusions were observed in magnetite in the samples from Tainiovaara.
From the Lomalampi deposit, we studied samples with weak sulfide dissemination. Oxides are present as euhedral-subhedral magnetite (diameter ~ 50–200 μm), Cr-magnetite, remobilized magnetite veins, and trace amounts of ilmenite. As illustrated in Fig. 2f, magnetite occurs together with sulfides (pyrrhotite, pentlandite, and chalcopyrite) as sulfide-magnetite aggregates and also as individual euhedral grains. In addition, some remobilized magnetite-sulfide veins and magnetite rims around altered chromite grains occur. There are rounded pentlandite-pyrrhotite inclusions inside magnetite (Fig. 4c).
The samples from the Tulppio mineralization contain trace sulfides with individual subhedral-euhedral Cr-magnetite (Fig. 3a) and magnetite (diameter ~ 50–500 μm) grains. A minor amount of magnetite occurs together with sulfides (pyrrhotite and pentlandite). Magnetite also occurs as rims around altered chromite grains. Remobilized, vein-hosted Cr-rich magnetites and magnetites have rounded pyrrhotite-pentlandite inclusions (Fig. 4d).
The samples from the Kovero komatiites contain disseminated subhedral to anhedral magnetite grains (diameter ~ 50–500 μm) in a chlorite schist (Fig. 3f), representing a metamorphic oxide phase, and Cr-magnetite after extensive alteration of chromite in a serpentine-amphibole rock with a preserved cumulate texture. The samples have only trace amounts of sulfides and some ilmenite.
Some reference samples from the Pechenga and Kevitsa Ni-Cu-PGE deposits were also studied. Of the four samples from Pechenga, two represent massive sulfide ore from the basal part of the Pilgujärvi intrusion (Fig. 3d), containing subhedral-anhedral magnetite grains (diameter ~ 50–200 μm) in massive sulfides with small amounts of sulfide inclusions (Fig. 4e, f). The other two samples are from the Kammikivi sill (Hanski et al. 2011) and represent, respectively, an altered olivine cumulate with disseminated sulfides and magnetite and a relatively unaltered olivine cumulate with Cr-spinel and ilmenite. From the Kevitsa deposit, we studied one sample from each of the three main disseminated ore types, which are called the Normal Ore (Fig. 3b), Ni-PGE Ore (Fig. 3c), and False Ore, with the last one being very low in base metals (Mutanen 1997; Luolavirta et al. 2017). The Normal and False Ore samples contain euhedral-subhedral Cr-magnetite and some magnetite, and the Ni-PGE Ore sample contains mostly subhedral-anhedral magnetite. We also analyzed three samples from a deformed ore body near the margin of the Jinchuan Ni-Cu sulfide deposit, of which two represents Cu-rich remobilized and one a Ni-rich ore (Yang et al. 2018). They contain individual subhedral-anhedral Cr-magnetite grains and magnetite, which occur together with remobilized and sheared disseminated sulfides (Fig. 3e) (Yang et al. 2018). The samples from the Jinchuan deposit were only analyzed with EPMA.
Electron probe microanalyzer (EPMA)
Oxides were analyzed at the Center of Microscopy and Nanotechnology, the University of Oulu, using a Jeol JXA 8200 Superprobe electron probe microanalyzer. In general, 10–30 individual magnetite grains per sample were analyzed. The following analytical conditions were used for oxide analyses: a beam size of 10 μm, an accelerating potential of 15 kV, and a current of 100 nA. A large spot size is necessary to prevent over heating of oxides under the high current and to obtain a representative analysis from heterogeneous oxide mineral grains. The peak counting time was set at 30 s for peaks and 10 s for the background (expect Fe was set for 6 s for peak and 3 s for background). The following 17 elements were analyzed: Fe, Ti, Cr, V, Ni, Cu, Co, Mg, Si, Al, Zn, Mo, Mn, Pb, Pt, Rh, and Ga, with the average detection limits falling in the range of ~ 60–400 ppm. The matrix correction with the ZAF method was applied to all oxide analyses.
Laser ablation-inductively coupled plasma-mass spectrometry (LA-ICP-MS)
Thick (100 μm) polished sections were prepared for LA-ICP-MS analysis although for some deposits, ordinary thin sections were used. In general, 10–30 individual magnetite grains per section were selected for analysis by LA-ICP-MS. The analyses were performed at the Geological Survey of Finland (GTK) in Espoo using a Nu AttoM single collector LA-SC-ICP-MS (Nu Instruments Ltd., Wrexham, UK) and an Analyte Excite 193 ArF laser ablation system (Photon Machines, San Diego, USA). The laser was run at a pulse frequency of 10 Hz and a pulse energy of 5 mJ at 30% attenuation to produce an energy flux of 2.5 J/cm2 on the sample surface with a 40 μm spot size (expect from one sample both from Tulppio and Kovero, where the spot size was 25 μm). Analyses were made using time resolved analysis (TRA) with continuous acquisition of data (20 s of baseline followed by 40 s with laser switched on) for each set of data points (2 standards, 10–20 unknown, 1 quality control standard). The solid synthetic silicate GSE-1G standard was used for external standardization, the synthetic glass standards GSD-1G, BCR2G, and BHVO2G for quality control (Guillong et al. 2005; Jochum et al. 2005), and 57Fe as an internal standard. The value of the internal standard has been re-calculated based on the sum of the two main cations (Fe and Cr), to 100% (Fe-Cr2O3) concentration when the Cr concentrations were too high (totals above 100% when using EPMA data). The measurements were performed over 42 isotopes and 34 elements at low resolution (∆M/M = 300) using the fast scanning mode. The following 42 isotopes were analyzed: 24Mg, 27Al, 29Si, 30Si, 31P, 33S, 34S, 43Ca, 44Ca, 45Sc, 47Ti, 51V, 52Cr, 53Cr, 55Mn, 57Fe, 59Co, 60Ni, 63Cu, 66Zn, 71Ga, 74Ge, 75As, 77Se, 89Y, 90Zr, 91Zr, 93Nb, 95Mo, 97Mo, 105Pd, 117Sn, 118Sn, 119Sn, 139La, 147Sm, 172Yb, 178Hf, 181Ta, 182W, 195Pt, and 208Pb. The following isotopes were selected for elements for which multiple isotopes were measured: 29Si, 33S, 43Ca, 53Cr, 90Zr, 95Mo, and 118Sn. Average detection limits (99% confidence) were the following: 0.001–0.002 ppm for Pd and Pt; 0.01–0.1 ppm for Ta, Pb, Nb, W, Ga, Hf, Y, La, Yb, V, Ge, Sm, Sn, Co, and Sc; 0.1–1 ppm for As, Zr, S, Se, Mo, Mn, Cu, Zn, Mg, P, Cr, and Al; 1–2 ppm for Ni and Ti; and 5–50 ppm for Fe, Si, and Ca. In ESM Table 1B (Electronic Supplementary Material), only the element is shown, not the isotope number. Data reduction was conducted using the GLITTER™ software (Van Achterbergh et al. 2001), which allows baseline subtraction, the integration of the signal over a selected time resolved interval, and quantification using known concentrations of the external and internal standards.
The EPMA data were used to identify and classify different iron oxides and also for calibration of LA-ICP-MS analyses. The LA-ICP-MS method was used for more detailed trace element analysis, because compared to EPMA, it is more accurate for trace elements, and has lower detection limits, and the larger spot size allows determination of a more representative composition. ESM Tables 1A and B list representative compositions of magnetites and Cr-magnetites based on EPMA and LA-ICP-MS analyses, respectively.
In order to compare the magnetite and Cr-magnetite compositions from different deposits, box-whisker percentile plots (Fig. 5) and multi-element variation diagrams (Fig. 6) are utilized. These plots provide a good overview of the data, allowing observations of many elements at the same time. As shown in Fig. 5, in which only oxides with < 1 wt.% Cr are plotted, relatively large variations in the Cr, Ti, V, Ni, Al, Mg, and Ga contents of magnetites from different deposits are observed. High Cr concentrations, mostly above 1000 ppm, are shown by magnetites from the Kovero and the Tainiovaara and Ruossakero deposits. In the Kovero case, the magnetites are most likely primary, as they occur as individual grains without zoning. In the Tainiovaara and Ruossakero deposits, magnetites represent altered chromites, which are now Cr-bearing magnetites. Disseminated magnetites from the Pechenga deposit and Vaara non-mineralized altered cumulates and magnetite veins from the Ruossakero deposit show intermediate Cr concentrations. Magnetites from the Kevitsa Ni-PGE ore, Lomalampi magnetite veins, Hietaharju massive sulfides, and Vaara deposit have low Cr concentrations, generally below 100 ppm.
The highest Ti values in the data set are in magnetite from Pechenga, Lomalampi, Vaara non-mineralized altered cumulate, Kevitsa Ni-PGE ore, and Tainiovaara and Hietaharju deposits, and the lowest values in magnetite veins from Lomalampi and Ruossakero and disseminated sulfide samples from Ruossakero. The highly variable Ti and V concentrations in magnetites from the Pechenga massive sample are due to exsolution of Ti-rich phases in some magnetite grains. The highest V concentrations (generally ~ 300 ppm to ~ 1500 ppm, and as high as 5000 ppm in Pechenga) occur in magnetite from the Lomalampi, Kovero, and Vaara non-mineralized altered cumulates and the Pechenga and Hietaharju deposits. Intermediate V concentrations (~ 100 ppm to ~ 300 ppm) were measured for magnetite from the Kevitsa, Tainiovaara, Ruossakero, and Vaara deposits and low V (mostly below ~ 100 ppm) concentrations for magnetite from both veins type samples from the Lomalampi and Ruossakero deposits.
Nickel shows a wide range of concentrations. High Ni concentrations (mostly ~ 500 to ~ 5000 ppm) were determined from the Ruossakero magnetite veins and Kevitsa, Vaara, Ruossakero, Pechenga, and Tainiovaara deposits. The Ni concentration from magnetite inside pyrrhotite or pentlandite does not vary in the massive sulfide sample from Pechenga, but Cr-magnetites in this sample have lower Ni (avg. Ni ~ 370 ppm). Magnetites from the Kovero non-mineralized altered cumulate and Lomalampi deposit show intermediate Ni concentrations (generally ~ 350 to ~ 600 ppm). The lowest Ni values were measured for magnetite from the Lomalampi magnetite veins, Vaara non-mineralized altered cumulate, and Hietaharju massive sulfides (mostly below ~ 300 ppm). The Ni concentration in magnetite of the Hietaharju massive sulfide samples is low regardless of whether magnetite grains are enclosed in pyrrhotite or pentlandite. Copper occurs mostly as trace amounts (< 100 ppm) in the analyzed magnetite grains, with only the Vaara deposit showing higher Cu contents, averaging ~ 225 ppm. The Kevitsa Ni-PGE ore and Tainiovaara deposit contain magnetite with relatively high Al contents (above ~ 350 ppm) whereas magnetite from the Lomalampi magnetite veins; Vaara and Kovero non-mineralized altered cumulates; Vaara, Lomalampi, and Hietaharju deposits shows intermediate Al values. Magnetite grains from the Ruossakero disseminated sulfide samples, and magnetite veins and Pechenga massive sulfide ore are lowest in Al.
The Mg concentrations in magnetite are highly variable between ~ 20 and ~ 30,000 ppm, being highest in the Ruossakero, Tainiovaara, and the Kevitsa deposits (~ 1000 to 30,000 ppm); intermediate in the Lomalampi and Vaara deposits, Ruossakero magnetite veins and barren cumulates from Kovero and Vaara (mostly ~ 450 to ~ 7000 ppm); and lowest in massive sulfides from the Pechenga and Hietaharju deposits (~ 20 to ~ 400 ppm). Silicon is also low in massive sulfide samples, though it overlaps partly with Si in other sample types. Interestingly, high Ga concentrations were observed in magnetite from massive sulfide samples from Pechenga and Hietaharju, and also magnetites from the Kevitsa deposit and Lomalampi remobilized magnetite. The LA-ICP-MS data show that levels of Pt and Pd are mostly below or very close to the detection limit in the analyzed iron oxides (average detection limits in LA-ICP-MS analysis for Pt and Pd are ~ 0.001 and ~ 0.002 ppm, respectively).
In the multi-element variation diagram of Dare et al. (2014) shown in Fig. 6, trace element compositions are shown separately for magnetites from massive sulfide samples (Fig. 6a), from vein samples (Fig. 6b), magnetites from disseminated sulfide samples and some non-mineralized samples (Fig. 6c), and Cr-magnetites from disseminated sulfide samples and some non-mineralized samples (Fig. 6d). Magnetites from the massive sulfide samples from Pechenga and Hietaharju (Fig. 6a) show very similar patterns, which are enriched in V, Ni, and Cr compared to continental crust. Interestingly, magnetites from Pechenga have the highest Ti, Nb, and Ta concentrations in the data set. Magnetite veins from Lomalampi and Ruossakero (Fig. 6b) have mutually similar trends, but the Lomalampi magnetite veins have more elevated contents of most elements (e.g., Y, Al, Ge, Sc, Nb, Ga). The exceptions to this are higher Cr and Ni contents at Ruossakero. Magnetites from disseminated sulfide samples and some non-mineralized altered samples (Fig. 6c) show relatively uniform trends. They are enriched in V, Ni, and Cr, especially in the mineralized ones. The Vaara magnetites have higher Pb and Cu contents compared to others. Cr-magnetites (Cr > 1 wt.%) in Fig. 6d have relatively similar element distributions between each other. Some differences occur as, for example, the Kevitsa Ni-PGE and Tainiovaara samples have higher Cu concentrations. All Cr-magnetites are enriched in the more compatible elements (Zn, Co, V, Ni, and Cr).
In Fig. 7, magnetite compositions from the studied deposits are compared with the fields showing magnetite compositions in different stages of sulfide fractionation as defined by Dare et al. (2012) and Boutroy et al. (2014) using magnetites from the Sudbury Ni-Cu sulfide deposits. These fields represent early-forming Fe-rich MSS (monosulfide solid solution), evolved Fe-rich, and residual Cu-rich ISS (intermediate solid solution). Dare et al. (2012) observed that in sulfide liquid, lithophile elements (Cr, Ti, V, Al, Mn, Sc, Nb, Ga, Ge, Ta, Hf, W, and Zr) are compatible into iron oxides. In early-forming magnetite, which crystallizes with Fe-rich MSS, lithophile elements occur in the highest concentrations, and when fractionation of sulfide liquid continues towards a Cu-rich ISS, the concentration of these elements in magnetite gradually decrease, becoming low in magnetite, which crystallizes with the residual ISS (Dare et al. 2012). In the Cr vs. V, Ti, and Ni diagrams (Fig. 7a, b, and c), a clear horizontal trend can be observed due to varying Cr concentrations in magnetites, which likely indicates that oxide grains represent highly altered chromites. In the Cr vs. V binary diagram (Fig. 7a), most of the magnetite grains from the Pechenga sample are in the primitive Fe-rich and evolved Fe-rich fields (MSS) (Fig. 7a), and most of the Vaara and Kevitsa magnetite grains plot in the evolved Fe-rich field. Some of the magnetite compositions from the Hietaharju massive sulfide samples are in the primitive and evolved Fe-rich fields. Magnetite from the Lomalampi deposit occurs mostly inside the primitive Fe-rich field. Other compositions from Tainiovaara, Ruossakero, and Kovero are located mostly outside of these fields.
The Cr vs. Ni diagram (Fig. 7b and Fig. 8) shows that most of the magnetite grains analyzed from the mineralized sulfide samples are high in Ni and some are close to the Cu-rich (ISS) field. The Cr vs. Ti diagram (Fig. 7c) indicates similar features to those of the Cr vs. V diagram, mostly due to the positive correlation between Ti and V (Fig. 7d). The variation in Ti and V abundances could be explained by some amount of fractionation of sulfide liquid. It is worth pointing out that in the Pechenga massive ore sample, there is a continuous variation from Cr-magnetite to very Cr-poor magnetite, with Cr varying from ~ 43,000 to ~ 5 ppm (Fig. 7a–c). In the Cr vs. Ti diagram, some of the magnetite compositions from the Hietaharju, Vaara, Kevitsa, and Pechenga deposits plot in the Cu-rich (ISS) field.
Magnetite composition as an indicator of its origin
In Fig. 7, most of the magnetite grains from the massive sulfide samples from the Pechenga and Hietaharju deposits plot in the primitive Fe-rich (MSS) and evolved Fe-rich (MSS) fields, which indicates that they crystallized with MSS, also minor amounts with ISS. These magnetite grains from the massive sulfide samples also show low-Mg contents (Fig. 5). The early-formed magnetites which crystallized with a primitive Fe-rich MSS at Sudbury have similarly anomalously low-Mg concentrations (Dare et al. 2012). Magnetites from disseminated sulfide samples from Vaara and Kevitsa also plot mostly in the Fe-rich (MSS) and evolved Fe-rich (MSS) fields, and some analyses also in the ISS field. Also, some of the magnetites in the disseminated sulfide samples from the Lomalampi deposit plot in the Fe-rich and evolved MSS fields (Fig. 7a). These magnetites from mineralized samples are also enriched in V, Ni, and Cr, which indicates that they crystallized with MSS-ISS.
One difference between magnetites from massive sulfide samples and disseminated sulfide samples is that magnetites in the former have lower Mg and higher Ga (Figs. 5 and 6), similar to magnetites in primitive Fe-rich MSS in the Sudbury ores (Dare et al. 2012). Interestingly, most of the magnetite compositions from the Vaara deposit plot in the evolved Fe-rich (MSS) field (Fig. 7a, c), despite the fact that magnetites are mostly formed in post-magmatic hydrothermal oxidation of sulfides. Also, copper and lead are higher in the Vaara magnetites than in magnetites in the other deposits (Fig. 6c), a phenomenon potentially related to the oxidation of sulfides to magnetite. In contrast, magnetite compositions from post-magmatically altered samples from the Ruossakero and Tainiovaara deposits plot clearly outside of the MSS-ISS fields (Fig. 7), potentially indicating that their original magmatic composition is hydrothermally altered.
Hydrothermal magnetite veins in the Lomalampi and Ruossakero deposits have low Ti and V concentrations compared to other magnetite occurrence styles (Fig. 5). The Lomalampi magnetite veins are also enriched in Ga. Interestingly, magnetite veins from the Ruossakero deposit are highly enriched in Ni. These vein-type magnetites plot in the hydrothermal field in Fig. 9a and have a relatively high Si + Mg content (Fig. 9c).
In general, Cr-magnetites can be formed by different mechanisms, including direct crystallization from a silicate magma or from a sulfide liquid, post-magmatic alteration of Cr-spinel, or during metamorphic and/or hydrothermal redox processes without a Cr-spinel precursor. Cr-magnetites analyzed in this study are enriched in Zn, Co, V, and Ni (Fig. 6d). Most samples with disseminated sulfides contain Cr-magnetites with clear petrographic evidence that they formed by alteration of magmatic Cr-spinel. The contents of Ti, Cr. and V vary in the analyzed Cr-magnetites. The highest Cr concentration occurs in magnetites that are most likely altered from chromites. Cr-magnetites in the massive sulfide sample from Pechenga have the highest V and Ti concentrations among the analyzed Cr-magnetites. Depending on the Cr content and alteration intensity, Zn is relatively high in Cr-magnetites (Fig. 6d), and in this case, the high Zn content is related to chromium spinel alteration (cf. Barnes 2000). The Pechenga massive sulfide samples with a continuous chemical variation between Cr-magnetite and magnetite demonstrate that Cr-magnetite can crystallize directly from sulfide liquid. In contrast to Cr, Ni shows a more constant concentration of around 2000 ppm. The difference in the behavior of these two metals could be related to low-temperature sulfide-oxide equilibration which affected Ni but not Cr.
In several disseminated sulfide deposits, Cr-magnetite occurs as a dissemination together with sulfides (Fig. 2b, d, e). They could have been formed near or at the boundary between sulfide and silicate liquids via diffusion of oxygen out of the sulfide liquid (Frost and Groves 1989; Fonseca et al. 2008), but because of the highly altered and deformed nature of the rocks, this is hard to prove. Cr-magnetites in the Hietaharju sheared and disseminated sulfide sample (Fig. 2b) are low in Ni (avg. ~ 250 ppm). In the Vaara disseminated ore representing complete oxidation of the original sulfide assemblage to Ni-rich sulfides and magnetites, Cr-magnetite does not occur, but the oxide phase (magnetite) is enriched in Ni (avg. ~ 2000 ppm), with the Cr content being generally at a level of 10–100 ppm.
In the komatiite-hosted deposits, such as Vaara, Ruossakero, and Lomalampi, magnetite compositions are low in Nb and Ta (below or very close to the detection limits), which obviously is a consequence of their komatiitic parental magma. In contrast, magnetites from the Pechenga massive sulfide samples show an average concentration of 4.5 and 0.17 ppm for Nb and Ta, respectively, and their Ti concentrations are also high (avg. mean 2300 ppm, Fig. 5), which all can be regarded as reflections of the ferropicritic parental magma with an OIB-type trace element signature (Hanski and Smolkin 1995).
Correlation between Ni tenor and Ni content in magnetite
Figure 8 shows average Ni concentrations of iron oxides compared with the average Ni tenors (percentage of Ni in 100% sulfide) of the corresponding ore deposits, including data from this study and the literature. The Kevitsa Ni-PGE, Vaara, and Ruossakero mineralized samples show the highest Ni contents (LA-ICP-MS data) in the oxides, with the average Ni content being as high as ~ 2900 ppm, ~ 2700 ppm, and ~ 1900 ppm in these three cases, respectively. This is consistent with their high average Ni tenors of ~ 25 wt.%, ~ 38 wt.%, and ~ 23 wt.%, respectively (Mutanen 1997; Yang et al. 2013; Konnunaho et al. 2015). Interestingly, in the Vaara and Ruossakero deposits, magnetite is accompanied with Ni-rich sulfides, such as millerite and violarite (Konnunaho et al. 2015). High Ni sulfides also occur in the Kevitsa deposit in association with ultra-nickeliferous olivine (Mutanen 1997; Yang et al. 2013). Similarly, the Tainiovaara deposit has a relatively high Ni tenor, ~ 20 wt.% (Konnunaho et al. 2015), and relatively high Ni contents (average ~ 1600 ppm) in Cr-magnetite and magnetite. The Raglan, Noril’sk-Talnakh, and Pechenga ore deposits show moderately high average Ni tenors, ~ 12 wt.%, ~ 5 wt.%, and ~ 12.5 wt.%, respectively, and their average Ni contents in oxides are also moderately high, ~ 1500 ppm, ~ 1500 ppm, and ~ 1700 ppm, respectively (Osmond et al. 2002; Boutroy et al. 2014; Naldrett 2004). The Jinchuan deposit has an average Ni tenor of ~ 9 wt.% (Naldrett 2004) and an average Ni concentration in Cr-magnetites of ~ 1150 ppm, whereas magnetite is very low in Ni (below the EPMA detection limit; the average detection limit for Ni varied from ~ 50 to ~ 200 ppm). The Tulppio Cr-magnetites have an average Ni content of ~ 1300 ppm and an average Ni tenor of the Tulppio mineralization is ~ 12 wt.%. Cr-magnetites could in some cases represent chromite alteration products, and therefore, the Ni concentrations do not necessarily represent those of magnetite or Cr-magnetite that crystallized from a sulfide liquid. The oxide phase in the Lac Des Iles (Canada), Sudbury and Kevitsa Normal Ores has an average Ni concentration of ~ 500–600 ppm, with the corresponding Ni tenors being ~ 4 wt.%, ~ 4.5 wt.%, and ~ 8 wt.%, respectively (Mutanen 1997; Naldrett 2004; Yang et al. 2013; Boutroy et al. 2014; Duran et al. 2016; Djon et al. 2018). The Lomalampi and Hietaharju deposits show generally lower Ni tenors, averaging ~ 6 wt.% and ~ 3 wt.%, respectively, and their magnetites are also lower in Ni, averaging 400 ppm and 250 ppm, respectively. Of the studied deposits, the Kevitsa False Ore has the lowest average Ni concentration in magnetite (~ 150 ppm), which is coupled with the lowest Ni tenor of ~ 0.5 wt.% (Mutanen 1997; Yang et al. 2013).
In Fig. 8, average Ni tenors obtained from the literature for each deposit as a whole were used, though the tenor can vary much within a deposit and between different types of ores within a deposit. Nevertheless, this plot shows a relatively good positive correlation between the average Ni tenor of sulfides and the average Ni content of oxides. Furthermore, the diagram demonstrates that the correlation is valid regardless of the post-magmatic history of the deposits, as a high Ni content of magnetite can be both due to post-magmatic oxidation of sulfides (as in the case of the Vaara, Ruossakero, and Tainiovaara deposits) or a primary feature related to a high Ni content of the silicate magma and consequently that of the sulfide liquid from which these Fe oxides crystallized (as exemplified by Kevitsa). It may be that in both cases, late sulfide-magnetite equilibration took place at relatively low temperatures.
In considering the relationship between the Ni tenor and the Ni content of associated oxides, we used average Ni tenors from the literature. This phenomenon should be examined further employing controlled sampling in detailed scale, with the tenor calculated and magnetite composition measured from the same sample, potentially also involving other elements, such as Co and Cu.
Application to mineral exploration
Several recent studies have focused on attempts to employ the magnetite trace element composition as an exploration tool for Ni-Cu-PGE deposits and as a key to the origin of magnetite. Dare et al. (2014) presented a Ni/Cr vs. Ti diagram, which can discriminate between magmatic and hydrothermal magnetite, and Dupuis and Beaudoin (2011) introduced a Cr + Ni vs. Si + Mg diagram to discriminate magnetite between Ni-Cu-PGE deposits and hydrothermal and other types of magmatic ore deposits. Ward et al. (2018) showed that the Cr/V ratio vs. Ni diagram can be used to distinguish magnetite generations that were formed in mineralized and barren systems. Liu et al. (2015) introduced a Ga + Co vs. Ge diagram, which can discriminate magnetite from Ni-Cu deposits, massif-type anorthosites, and evolved parts of mafic-layered intrusions. In addition to magnetite, the chemical composition of chromite can be useful in mineral exploration for magmatic sulfide deposits. For example, the recent study by Locmelis et al. (2018) demonstrated that the Ru (or other PGE) content in chromite is indicative of the presence or absence of a sulfide liquid during the crystallization of chromite.
In Fig. 9, our magnetite data are plotted on the four discrimination diagrams mentioned above. It is important to note that all the studied samples are more or less altered, and therefore, these discrimination diagrams cannot be used to directly discriminate their origin but, instead, can be used to discuss the variation in the chemical composition of iron oxides during alteration. We filtered out Cr-bearing magnetites from these plots (exclusively plotting magnetites with Cr < 1 wt.%) to exclude the grains that may have originally been chromites. Figure 9a presents the Ni/Cr vs. Ti diagram (Dare et al. 2014), where most of the magnetite compositions from Tainiovaara and Lomalampi together with non-mineralized altered cumulates from Vaara and Kovero plot in the magmatic magnetite field. The magnetite composition from the Pechenga and Hietaharju deposits fall both in the magmatic and hydrothermal field. Instead, due to their high Ni concentrations, most of the magnetite analyzed from Vaara, Ruossakero, Kevitsa, and Lomalampi magnetite veins plot in the hydrothermal field.
In the Cr + Ni vs. Si + Mg diagram (Dupuis and Beaudoin 2011), most magnetite from Pechenga and Ni-rich magnetite veins from Ruossakero plot in the Ni-Cu sulfide ore field (Fig. 9c). Some magnetite from Hietaharju, Vaara, and Kovero are also in the Ni-Cu field. However, other compositions are outside of the Ni-Cu field due to their relatively high Si and Mg concentrations. This is most likely because of the alteration of the samples. In the Cr/V vs. Ni diagram (Ward et al. 2018), all the magnetite compositions from the Lomalampi, Kevitsa, Vaara, Pechenga, and Tainiovaara deposits are inside the ore-related field (Fig. 9b). Interestingly, magnetites from Kovero occur also in this field, though currently no Ni-Cu sulfide mineralization is known to exist in the Kovero area. Most of the analyzed magnetites from the Hietaharju deposit plot in the barren field, with only two compositions being located in the ore-related field. This is because of their anomalously low Ni concentrations, which is an enigmatic feature given the fact that magnetite occurs in massive Ni-rich ore. Also, the magnetite grains from Lomalampi and magnetite veins and a non-mineralized altered cumulate sample from Vaara are in the barren field. Using the Ga + Co vs. Ge diagram of Liu et al. (2015), the analyzed magnetites from Pechenga, Tainiovaara, Hietaharju, and Kevitsa deposits plot in the Ni-Cu field (Fig. 9d). Magnetites from Ruossakero, Lomalampi, and Vaara and Kovero non-mineralized samples occur mostly outside of this field. Magnetites from non-mineralized altered cumulate from Vaara are located in both the Ni-Cu and layered intrusion fields and magnetites from magnetite veins from Lomalampi plot in both the Ni-Cu field and anorthosite field. In general, because of alteration, our data show a large scatter in these discrimination diagrams, and therefore, the magnetite compositions cannot necessarily be used to discriminate their origin but rather give information on the changes in the composition of iron oxides during alteration.
Mineral inclusions in magnetite grains could also provide information on phases which crystallized before, or together with, magnetite. We found that some magnetites in the mineralized samples host base metal sulfide inclusions (Fig. 4). This indicates that the oxide phase is segregated and crystallized at the same time or later than the sulfide phase. From the mineral exploration point of view, this is a good indication of sulfide formation, especially if there is magnetite with Ni-bearing sulfide or platinum-group metal (PGM) inclusions.
Studying indicator minerals from till is a useful and widely used exploration tool in glaciated terrains, indicating a potential existence of occurrences of mineral deposits, such as those of diamond, gold, and various base and precious metals (e.g., Sarala 2015 and references therein). Till geochemistry and indicator-mineral signatures have also been utilized in exploration for magmatic Ni-Cu-PGE deposits, especially in Canada (e.g., McClenaghan et al. 2011 and references therein). Ward et al. (2018) successfully used magnetite as a geochemical indicator for a Ni-Cu-PGE deposit in the Munali area, Zambia by sampling and analyzing soil overburden samples. A methodology of extracting magnetite grains from till samples, analyzing their composition with EPMA and LA-ICP-MS, applying selected discrimination diagrams to the resulting data, and studying mineral inclusions within the grains could be developed into a sound exploration strategy for discovering new magmatic Ni-Cu deposits. Nevertheless, it is important to note that the magnetite compositions from barren rocks and alteration effects on magnetite composition have yet to be studied in sufficient detail, and in the future, a more comprehensive data set of magnetite compositions from a wider range of rock types, including barren rocks, could improve the quality of the discrimination diagrams. Because of this, magnetite compositions as a Ni sulfide exploration tool for samples that are highly altered by post-magmatic processes should be applied with caution.
Our results indicate that the trace element concentrations in oxide phases vary from two to three orders of magnitude, reflecting both the silicate (e.g., magnetites in the massive sulfide sample from Pechenga have high Ti, Nb, and Ta) and sulfide melt compositions from which they have crystallized, and post-magmatic modification processes (magnetites in the Vaara deposit, which were formed from post-magmatic oxidation of sulfides are high in Ni, Cu, and Pb).
The massive ore samples from Pechenga contain an oxide phase varying in composition from Cr-magnetite to magnetite, indicating that Cr-magnetite can crystallize directly from sulfide liquid.
The Ni concentration of magnetite is a function of the average Ni tenor of the sulfide phase with which magnetite is associated, regardless of whether the sulfide phase is magmatic or post-magmatic in origin. This indicates that a high Ni concentration of magnetite could be a primary feature, which is related to a high Ni content of sulfide or silicate liquid from which these Fe oxides crystallized, or it can reflect to post-magmatic oxidation of sulfides, and formation of secondary magnetite.
The Mg concentration of magnetite in massive ore samples (Pechenga and Hietaharju) is clearly lowest among the analyzed samples and can be regarded as a diagnostic feature of an oxide phase crystallized together with primitive Fe-rich MSS in a microenvironment more or less isolated from associated silicate magma.
Results indicate that the magnetite composition (e.g., high Ni and relatively low Mg and high Ga in magnetites from massive sulfide) together with petrographical observations (especially Ni-bearing sulfide inclusions inside magnetite) could be potentially used as an exploration tool for new Ni-Cu-PGE deposits in glaciated terrains, including Fennoscandia.
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Open access funding provided by University of Oulu including Oulu University Hospital. This research was supported by the Academy of Finland (grant #281859), K.H. Renlund Foundation and Tauno Tönning Foundation. We thank Leena Palmu for guidance with electron microprobe analysis. Two anonymous reviewers are acknowledged for their helpful comments, which significantly improved the manuscript. We are grateful to Bernd Lehmann and Pasi Eilu for their useful comments and editorial work.
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Moilanen, M., Hanski, E., Konnunaho, J. et al. Composition of iron oxides in Archean and Paleoproterozoic mafic-ultramafic hosted Ni-Cu-PGE deposits in northern Fennoscandia: application to mineral exploration. Miner Deposita (2020) doi:10.1007/s00126-020-00953-1
- Fe oxide
- Trace element
- Ni-Cu-PGE sulfide deposit
- Fennoscandian Shield