About 20 mafic-ultramafic layered intrusions in the northern Fennoscandian shield were emplaced during a widespread magmatic event at 2.5–2.4 Ga. The intrusions host orthomagmatic Ni-Cu-PGE and Cr-V-Ti-Fe deposits. We update the magmatic stratigraphy of the 2.44-Ga Näränkävaara mafic-ultramafic body, northeastern Finland, on the basis of new drill core and outcrop observations. The Näränkävaara body consists of an extensive basal dunite (1700 m thick), and a layered series comprising a peridotitic–pyroxenitic ultramafic zone (600 m thick) and a gabbronoritic–dioritic mafic zone (700 m thick). Two reversals are found in the layered series. The composition of the layered series parental magma was approximated using a previously unidentified marginal series gabbronorite. The parental magma was siliceous high-Mg basalt with high MgO, Ni, and Cr, but also high SiO2 and Zr, which suggests primary magma contamination by felsic crust. Cu/Pd ratio below that of primitive mantle implies PGE-fertility. The structural position of the marginal series indicates that the thick basal dunite represents an older wallrock for the layered intrusion. A subeconomic reef-type PGE-enriched zone is found in the border zone between the ultramafic and mafic zones and has an average thickness of 25 m with 150–250 ppb of Pt + Pd + Au. Offset-type metal distribution and high sulfide tenor (50–300 ppm Pd) and R-factor (105) suggest reef formation by sulfide saturation induced by fractional crystallization. The reef-forming process was probably interrupted by influx of magma related to the first reversal. Metal ratios suggest that this replenishing magma was PGE-depleted before emplacement.
The Paleoproterozoic mafic-ultramafic Näränkävaara layered intrusion, northern Finland, is the easternmost member of the Tornio-Näränkävaara layered intrusion belt, which comprises six mafic-ultramafic layered intrusions with an average age of 2440 Ma (Fig. 1) (Alapieti 1982; Iljina & Hanski 2005). The intrusions were emplaced during widespread mantle-driven igneous activity related to extension and rifting of the Archean nucleus of the Fennoscandian shield (Amelin & Semenov 1996; Tiira et al. 2014; Huhma et al. 2018). In total, approximately 20 early Paleoproterozoic layered intrusions with associated dyke swarms have been found in the NW region of the Fennoscandian shield (Finland, Russia, and Sweden), all with ages between 2.53–2.39 Ga (Alapieti et al. 1990; Amelin et al. 1995; Vuollo & Huhma 2005; Bayanova et al. 2009).
The intrusions at the Archean-Proterozoic boundary in northern Finland have significant exploration potential for orthomagmatic mineral deposits, and have been shown to host reef-, contact-, and offset-type PGE(±Ni-Cu) deposits and Cr-Fe-Ti-V deposits (Huhtelin 2015; Iljina et al. 2015; Karinen et al. 2015; Makkonen et al. 2017). Mafic-ultramafic layered intrusions elsewhere with similar structure and composition as the Näränkävaara intrusion, e.g., the Great Dyke of Zimbabwe (Wilson 1996) and the Munni Munni complex in Western Australia (Hoatson & Keays 1989), also host high-grade PGE reefs.
Geological mapping and exploration projects have been conducted in the Näränkävaara intrusion since the 1950s (Auranen 1969; Piirainen et al. 1978; Alapieti 1982; Iljina 2003; Vesanto 2003; Lahtinen 2005; Akkerman 2008; Halkoaho et al. 2019). The recent discovery of a ~ 2-km-thick homogeneous unit of dunite along the southern contact of the Näränkävaara layered series highlights the need to re-evaluate the structure, composition, and exploration potential of the Näränkävaara body (Lahtinen 2005; Halkoaho et al. 2017, 2019).
In this study, we refine the magmatic stratigraphy of the Näränkävaara mafic-ultramafic body, originally presented by Alapieti (1982). We also discuss the parental magma composition of the intrusion as inferred from the newly found marginal series gabbronorite. We also describe a new uneconomic sulfide-associated stratiform (reef-type) PGE-enriched zone, located in the contact between the ultramafic and mafic zones of the Näränkävaara layered series, and present a model that explains the low grade of the PGE mineralization.
Tornio-Näränkävaara layered intrusion belt
The intrusions of the Tornio-Näränkävaara belt (Fig. 1) are typical mafic-ultramafic layered intrusions with marginal and layered magmatic series (Alapieti & Lahtinen 2002). The intrusions were emplaced within Archean granitoids along the rifting craton margin, and are now located along the contact between the Archean granite-gneiss basement and Karelian Paleoproterozoic supracrustal rocks (Iljina & Hanski 2005). The zircon U-Pb ages of the intrusions range between 2.45 and 2.43 Ga (Alapieti 1982; Huhma et al. 1990; Iljina 1994; Mutanen & Huhma 2001; Perttunen & Vaasjoki 2001; Maier et al. 2018).
The layered intrusions of the Fennoscandian shield have been classified into three compositional types: (1) mafic-ultramafic (e.g., Kemi, Näränkävaara), (2) mafic (Akanvaara, Koitelainen, Koillismaa), and (3) megacyclic (Portimo, Penikat) (Alapieti & Lahtinen 2002). The parental magmas have been thought to be (boninite-like) siliceous high-Mg basalts (SHMB), usually classified into high-Cr and low-Cr types (Alapieti et al. 1990; Iljina & Hanski 2005). The high-Cr and low-Cr magma types may be related by fractional crystallization (Maier et al. 2018). Whole-rock and isotope geochemical results (average ƐNd of − 2) point to crustal contamination of primary magmas from mantle plume sources (Puchtel et al. 1997; Hanski et al. 2001; Vuollo & Huhma 2005; Yang et al. 2016; Maier et al. 2018).
Näränkävaara mafic-ultramafic body
The Näränkävaara intrusion was emplaced into the Taivalkoski block of the Western Karelian subprovince of the Fennoscandian shield. Unlike other intrusions of the Tornio-Näränkävaara belt, Näränkävaara is surrounded on all sides by Archean (~ 2.8 Ga) granitoids (Fig. 2) (Hölttä et al. 2012). The N-S trending 2.9–2.8 Ga Suomussalmi greenstone belt terminates about 10 km south of the Näränkävaara body (Fig. 2) (Lehtonen et al. 2017), and the recently discovered (likely Archean) Takanen greenstone belt also borders the body 2 km to the NW (Iljina 2003). The large SW-NE trending Oulujärvi shear zone crosscuts the NW side of Näränkävaara.
Historically, the Näränkävaara layered intrusion has been included as part of the Koillismaa Layered Intrusion Complex (KLIC) (Alapieti 1982). The KLIC comprises (1) the tectonically dismembered western intrusion blocks, (2) the eastern Näränkävaara intrusion, and (3) a strong positive gravity and magnetic anomaly that connects the first two (Fig. 1 and inset in Fig. 2). Alapieti (1982) interpreted the Koillismaa and Näränkävaara intrusions to be co-genetic, with the Näränkävaara intrusion representing the lowest stratigraphic level of the complex. The connecting geophysical anomaly was interpreted as a magmatic conduit that fed the two intrusions.
Based on geophysical observations, the Näränkävaara mafic-ultramafic body is about 30 km long and 5 km wide and extends to a depth of 5–10 km with steep outer contacts (Elo 1992; Salmirinne & Iljina 2003). It has been considered to represent a 2436 ± 5 Ma mafic-ultramafic layered series, composed of a peridotitic-pyroxenitic ultramafic zone, and a gabbroic-dioritic mafic zone (Fig. 2) (Alapieti 1982). Later studies have shown that the Näränkävaara body includes two other distinct ultramafic cumulate units (Iljina 2003; Lahtinen 2005). Firstly, an extensive, up to 2 km thick basal dunite, composed of homogeneous olivine meso- and adcumulate, borders the layered series along its southern contact. In recent drilling, the dunite was also discovered on the northern side of the layered series and so may partly envelop it (Fig. 2; Akkerman 2008). Secondly, a series of smaller elongate intrusions, composed of harzburgite with coarse poikilitic orthopyroxene, are found crosscutting the basement complex parallel to the northern contact of the layered series (”northern ultramafics” in Fig. 2). These two cumulate units have only been described in mineral exploration reports (Iljina 2003; Vesanto 2003; Lahtinen 2005; Akkerman 2008; Halkoaho et al. 2019) and a thesis (Telenvuo 2017), and their petrogenetic relationship to the layered series remains to be determined.
The strike of the igneous layering in the pyroxenites of the Näränkävaara layered series is generally parallel to the long axis of the intrusion (Fig. 3a). A large SW-NE fault separates the intrusion into two main blocks, with the NW block dipping about 15–25° to the NE, and the SE block dipping 5–20° to the SW (Fig. 2) (Alapieti et al. 1979). Complex block faulting is present throughout the intrusion with several smaller strike-slip faults that have strikes along the short axis of the intrusion and dip-slip faults that have strikes along the long axis. The layered series is mostly undeformed and unaltered by post-magmatic processes, whereas the basal dunite is thoroughly serpentinized.
Materials and methods
A large part of the materials in this study were compiled from previously unpublished results of exploration projects conducted by the Geological Survey of Finland (GTK) and private exploration companies in 1966–2008 (Auranen 1969; Iljina 2003; Akkerman 2008). Most important results originate from 22 drill holes (named in Fig. 2) drilled or revisited by Outokumpu Mining Oy in 2001–2003 (Vesanto 2003; Lahtinen 2005). These form a profile across the NW block of the Näränkävaara body. New drilling was conducted in the SE block of the Näränkävaara body by the GTK in 2017–2018 (Halkoaho et al. 2019), and one drill hole intersecting a marginal series melagabbronorite is included in this study (R1 in Fig. 2). Five representative outcrop samples collected during this time are also included. Drill logs can be found in Appendix 1.
Whole-rock compositions were determined by X-ray fluorescence (XRF) from pressed powder pellets at Labtium Oy laboratories (method code 175/176X), and at the University of Oulu, Finland. Some base metals and trace elements were determined by inductively coupled plasma optical emission spectrometry (ICP-OES) following Aqua Regia digestion (Labtium Oy, method code 510P). The REE were determined by inductively coupled plasma mass spectrometry (ICP-MS) following HF–HClO4 digestion and lithium metaborate–sodium perborate fusion (Labtium Oy, method code 308 M); some trace elements were analyzed by ICP-OES after the same digestion and fusion procedure (Labtium Oy, method code 308P). Precious metals (Pt, Pd, Au) were determined by graphite furnace atomic absorption spectroscopy (GFAAS) or by ICP-OES following Pb-fire assay fusion at Labtium Oy (method code 705 U/P); with some analyses (Pt, Pd, Au, Ru, Rh, Ir, Os) made by ICP-MS following NiS-fire assay fusion at Labtium Oy (method code 714 M) or at Intertek Laboratories (method code NS25/MS), Australia. Major oxides were normalized to volatile-free 100%. All iron is presented as FeOtot. Whole-rock analyses comprise 1242 XRF, 1519 Au + Pd + Pt (2PGE + Au) and 22 REE analyses. All analytical data and detailed descriptions of methods and detection limits (Labtium Oy 2015) can be found in Appendix 2.
Mineral chemistry was determined for four thin sections from the PGE-enriched zone using wavelength dispersive spectroscopy of a Cameca SX100 electron microprobe at the Finnish Geosciences Research Laboratory in Espoo, with a total of 129 analyses from 58 mineral grains (Appendix 2). Mineral abbreviations used according to Whitney & Evans (2010).
Revised magmatic stratigraphy of the NW block of the Näränkävaara body
A new cross section across the NW block the Näränkävaara mafic-ultramafic body was constructed based on compilation and interpretation of historical drill core logs, new thin section studies, and correlation of whole-rock compositions between drill hole intersections (Fig. 4). A new stratigraphic column based on this cross section is presented in Fig. 5. The stratigraphy consists of a 1700 m thick basal dunite (purple in Fig. 5); and a layered series consisting of a 600-m-thick ultramafic zone (gray) and a 700-m-thick mafic zone (brown), with two compositional reversals found in the layered series (green).
Drill hole spacing leads to stratigraphic gaps of up to 500–600 m in the basal dunite, but the layered series is intersected completely up to a quartz-dioritic unit at the top. The contact between the layered series and the basement complex on the northern side of the body is not intersected. A large oblique fault causes the southern side of the cross section to be uplifted 300 m in relation to the northern side, allowing a stratigraphic section of about 1300 m of the layered series to be observed (Fig. 4).
Lithology and petrography
In general, the basal dunite is composed of fine- to medium-grained olivine adcumulate and lesser olivine mesocumulate with coarse poikilitic orthopyroxene. Chromite is found in trace amounts in both cumulus and intercumulus (poikilitic) habits. The dunite is completely serpentinized but pseudomorphs after olivine and pyroxenes commonly exhibit undeformed cumulate textures and conventional igneous classification terminology for the rocks can thus be used. Proterozoic diabase dykes up to 100 m thick cut the unit.
The basal dunite has been divided into three units based on lithology and whole-rock composition. The first unit consists of dunite and harzburgite (BD-1 in Figs. 4 and 5, 250–500 m thick). The unit forms a marginal or transition zone against the basement complex, with olivine adcumulate grading into harzburgites towards the basement contact. The harzburgites nearest to contact also contain trace amounts of clinopyroxene, plagioclase and phlogopite. The unit BD-1 contains the single olivine analysis made from the basal dunite formation with composition Fo87.5 (Alapieti 1982). The basement contact is tectonized with the basal dunite truncating foliation in the foot wall. Near to the contact, the unit contains xenoliths of Archean basement rocks.
The second, volumetrically largest dunite unit (BD-2 in Figs. 4 and 5, 1000–1500 m thick) is composed of massive olivine adcumulates with minor mesocumulate interlayers. This unit contains poikilitic chromite, which is typically only described from komatiites (Barnes & Hill 1995).
The third unit (BD-3 in Figs. 4 and 5, 50–100 m thick) consists of olivine adcumulates with patches of olivine mesocumulates with up to 20 vol% coarse poikilitic pyroxene. The contact of the basal dunite (unit BD-3) and the basal peridotite of the layered series (unit PER-1) is intersected by two drill holes (Fig. 4). Still, the exact location and nature of the contact is ambiguous due to strong alteration and decomposition of the basal dunite and the lowermost section of the basal peridotite. There is an approximately 50-m-thick and strongly altered contact zone, where the basal dunite transitions into harzburgite as the amount of orthopyroxene increases from 5–10 vol% to 40–60 vol%, coinciding with fining of orthopyroxene grain size from coarse poikilitic to granular. Grain boundaries between olivine and orthopyroxene are commonly embayed. After the transition zone, the degree of serpentinization decreases, with the cumulates of the overlying layered series being relatively unaltered.
Marginal series gabbronorite
In the SE block of the Näränkävaara body, a marginal series gabbronorite was found in the contact of the basal dunite and the layered series, on the side of the layered series (drill hole R1 in Fig. 2). Contact of the basal dunite and the layered series is sharp, tectonized, and subvertical, with surface magnetometry indicating a lateral extent of 5–6 km. The basal dunite near the contact consists of serpentinized olivine mesocumulates with 10–20 vol% coarse poikilitic pyroxene. The marginal series is about 10 m thick and composed of non-cumulus textured melagabbronorite with up to 5 vol% biotite and < 1 vol% chalcopyrite and pyrrhotite. The marginal series grades into the pyroxenites of the layered series over a distance of 1–2 m. Marginal series has not been found from the NW block of the intrusion (that is, in Figs. 4 or 5).
Ultramafic zone of the layered series
Along the NW cross section the contact between the basal dunite and the ultramafic zone of the layered series dips about 45 ° to the NNE (Fig. 4). The peridotitic-to-pyroxenitic ultramafic zone is about 600 m thick (~ 1750–2350 m in Fig. 5). The cumulates are generally well preserved and exhibit magmatic layering with a dip of 15–20° NNE (Fig. 3a).
Above the transitional contact zone with the basal dunite, the layered series begins with harzburgitic to olivine pyroxenitic unit (PER-1 at height ~ 1750 m in Fig. 5). The unit consists of olivine-bronzite adcumulates with up to 60 vol% olivine. Disseminated chromite is found in trace amounts throughout the ultramafic zone of the layered series (Alapieti 1982; Telenvuo 2017). The rocks gradate from harzburgite to olivine bronzitite within a distance of 50 m. The last 20 m of the olivine-pyroxenite contains up to 3 vol% pyrrhotite-dominated interstitial sulfides (note S in Fig. 5) (Telenvuo 2017).
The following 120-m-thick pyroxenitic unit PX-1A is composed of bronzitite and websterite (Fig. 4; note CaO-rich websterite interlayers in Fig. 5). The lower half of the unit contains massive and almost monomineralic bronzitites with minor intercumulus augite and trace plagioclase. In the upper half of the unit, rhythmic interlayers of websterite appear, composed of coarse grained bronzite-augite adcumulates, some with trace olivine. The overlying 250-m-thick pyroxenitic unit, PX-1B, is composed of rhythmic (plagioclase)-websterites; these are bronzite-mesocumulates with 5–20 vol% poikilitic augite and 1–5 vol% intercumulus plagioclase. The amount of plagioclase increases upwards in stratigraphy. About 70 m before the next unit (the PER-2 reversal) there is a 20-m-thick bronzite-augite adcumulate interlayer, after which the amount of intercumulus plagioclase again increases to 5–10 vol%. This last plagioclase-websteritic subunit hosts a PGE-enriched intersection with up to 200 ppb of Pd + Pt + Au (2PGE + Au; see Fig. 5 at height ~ 2150 m) similar to the main PGE-enriched zone hosted in the unit PX-2 after the PER-2 reversal.
The reappearance and rapid increase in the amount of cumulus olivine at a stratigraphic height of 2200 m marks the beginning of the unit PER-2, which is the first of the two lithological reversals within the layered series. The unit is about 120 m thick, and includes two roughly 50 m thick subunits composed of lherzolites and olivine pyroxenites separated by a olivine free pyroxenitic interlayer similar in composition to unit PX-1B. The lherzolites are composed of olivine-bronzite ortho- and mesocumulates with up to 60 vol% olivine, coarse (up to 1–2 cm in diameter) poikilitic augite, and up to 10 vol% intercumulus plagioclase. Chromite and phlogopite appear in trace amounts. The unit is generally sulfide-poor with occasional grains of trace pyrrhotite, but intersections with up to 1 vol% of disseminated pyrrhotite with minor pentlandite and chalcopyrite are found in drill hole R5 (Fig. 2).
The ultramafic zone ends with the 50–60 m thick pyroxenitic unit PX-2, composed of rhythmic websteritic mesocumulates, similar to those in unit PX-1B. Augite is typically found as relatively scarce and coarse oikocrysts (Fig. 3b). Over the last 20–30 m, the amount of augite and intercumulus plagioclase increases (Fig. 3c) and the cumulates grade into melagabbronorites of the mafic zone. This last gradational subunit of the ultramafic zone contains < 0.5 vol% of disseminated sulfides, and hosts a reef-type PGE-enriched zone that will be described in detail later (highlighted in Fig. 5).
Mafic zone of the layered series
The gabbronoritic-to-dioritic mafic zone is about 700 m thick (~ 2350–3000 m in Fig. 5). The zone is defined by the appearance of cumulus plagioclase, which increases upwards from 20 to 50 vol% in the melagabbronorites and pyroxenites to 50–70 vol% in the gabbronorites (note Al2O3 in Fig. 5). The plagioclase-dominated gabbroic cumulates of the mafic zone are generally more massive and have less well developed magmatic layering compared to the cumulates of the ultramafic zone.
In the first 200 m of the mafic zone, plagioclase alternates between cumulus and intercumulus. The first unit of this melagabbronoritic subzone (MGBNOR-1A) is a 40-m-thick melagabbronorite composed of plagioclase-augite-bronzite adcumulate. It is followed by a 20-m-thick pyroxenitic unit (PX-3, note Cr and Ni in Fig. 5) composed of augite-bronzite mesocumulate with 5–25 vol% intercumulus plagioclase. The subzone ends with two 60-m-thick melagabbronoritic units composed of augite-bronzite mesocumulates with 30–50 vol% intercumulus plagioclase (MGBNOR-1B and -1C), with the latter unit richer in bronzite making it relatively Ni- and Cr-rich (Fig. 5; labeled as olivine melagabbronorite in Fig. 4). First disseminated ilmenite grains appear in the last few meters of unit MGBNOR-1C. All four units contain up to 1 vol% of fine grained disseminated intercumulus pyrrhotite, chalcopyrite and pentlandite.
Increase in cumulus plagioclase to > 50 vol% and decrease in the amount of pyroxene marks the beginning of the 120-m-thick gabbronoritic unit GBNOR-1 at the stratigraphic height of ~ 2550 m (note increase in Zr in Fig. 5). Plagioclase is found as a cumulus phase until the last lithologic reversal (unit PER-3), and the lower half of the unit is composed of homogeneous plagioclase-augite-broznite cumulates. Disseminated magnetite appears 50 m from the base of the unit increasing upwards in stratigraphy. Minor amounts of interstitial biotite, as well as up to 1 vol% of trace sulfides, are found throughout this unit. From halfway up the unit heterogeneity increases with the occurrence of 0.20- to 2-m-thick leucopegmatoidal (anorthositic) layers and sparse coarse-grained plagioclase-quartz-(calcite) veining; quartz and localized coarse-grained sulfides and oxides are variably associated with the pegmatoidal layers. Biotite increases upwards in stratigraphy (note K2O in Fig. 5), appearing as evenly distributed 2–5 mm clumps, equigranular to plagioclase and pyroxenes; based on texture it is interpreted as magmatic (i.e., not potassic alteration). The gabbronorites end in a 20-m-thick Fe-Ti-oxide-rich gabbronorite with up to 10 vol% biotite and leucopegmatoidal interlayers.
The second and last compositional reversal is at the stratigraphic height of ~ 2650 m (unit PER-3 in Figs. 4 and 5). The lower contact is a 1-m-thick pegmatoidal melagabbro with up to 5 vol% coarse pyrrhotite and chalcopyrite (see S in Fig. 5). The contact is followed by the 30- to 40-m-thick unit PER-3 comprising olivine-pyroxenitic and minor lherzolitic ortho- and mesocumulates containing up to 30–40 vol% olivine. The unit is strongly altered (serpentinized) and disequilibrium textures are common, with, e.g., pyroxene exsolution, embayed and intergrown grain boundaries, and secondary tremolite-rims found on augite grains. The unit is also distinctly phlogopite-rich (5–15 vol%) with poikilitic phlogopite enclosing pyroxenes and olivine. The amount of olivine decreases upwards as cumulates grade into the last pyroxenitic unit PX-4. This unit is relatively altered, consisting of bronzite-augite ortho- and mesocumulate with up to 20 vol% intercumulus phlogopite and trace plagioclase.
As plagioclase increases upwards, the rocks are first melagabbronorites of the unit MGBNOR-2, and then, with plagioclase again becoming a cumulus mineral, the last 130-m-thick gabbronorites of the layered series (unit GBNOR-2 in Figs. 4 and 5). These follow roughly the same trend as the previous gabbronoritic unit, with irregular gabbropegmatoidal layers, trace amounts of disseminated sulfides, and appearance of disseminated ilmenite soon followed by magnetite. The gabbronorites grade into a light colored quartz dioritic unit composed first of ferrodiorite and then granodiorite (Figs. 4 and 5).
Whole-rock compositional variations
Type samples reflecting the calculated average whole-rock compositions of the units comprising the basal dunite and the layered series are presented in Table 1. Variations in whole-rock compositions are illustrated in Figs. 5, 6, and 7.
In general, the serpentinized basal dunite is geochemically homogeneous and poor in most elements except Ni and Cr. On average, the Mg#Footnote 1 is 88, with normalized MgO between 40 and 47.5 wt% and SiO2 between 39 and 43 wt%. Exception is the unit BD-1, that contains a transitional zone with increasing SiO2, TiO2, Al2O3, V, and Zr towards the basement contact (e.g., up to 5 wt% Al2O3 with 41 wt% MgO; see Fig. 5). Unit BD-2 is the most MgO-rich with 45–47.5 wt% MgO; and it also has a lower Cr contents of 1000–1500 ppm, compared to the other two dunite units with 2000–4000 ppm Cr. Ni varies between 1600 and 2900 ppm in units BD-1 and BD-2, decreasing to less than 1500 ppm in unit BD-3. Variable Ni content at constant MgO (see Fig. 6) implies extraction of Ni-sulfides, but the basal dunite samples along the NW profile are very sulfide poor. PGEs in the basal dunite are typically below the detection limit of 2 ppb (66 out of 74 samples) with the highest assay being 15 ppb Pt + Pd. High Cl concentrations of 1000–4500 ppm are present throughout the basal dunite. Moving from the basal dunite into the layered series there is an approximately 4–5 wt% decrease in MgO and 5–6 wt% increase in SiO2.
Marginal series gabbronorite
The composition of the marginal series gabbronorite intersected in drill hole R1 is presented in Table 2 and plotted in Figs. 6 and 7. The composition is characterized by high SiO2 (54–55 wt%) relative to MgO (14–15 wt%) (Fig. 6), and low CaO (6.5–7.5 wt%) and TiO2 (0.4 wt%); Ni (300–500 ppm) and Cr (1450–1750 ppm) are also relatively high. The Mg# is 77, Al/Ti ratio is 20, and Ca/Al ratio 0.7. According to IUGS classification, the composition is boninitic, with SiO2 > 52 wt%, MgO > wt.8%, and TiO2 < 0.5 wt% (Le Bas 2000); and according to the Jensen cation diagram the composition is of a komatiitic basalt (Jensen 1976).
The general magmatic evolution of the layered series is reflected in variations of MgO and Mg# with height (Fig. 5). There is a stepwise descent from the ultramafic to the mafic zone through the melagabbronoritic transition zone, followed by a gradual decrease into the dioritic unit. This trend is interrupted by the two peridotitic reversals. Compositions continue to become more evolved after each reversal, and cumulate sequences after each successive peridotite plot on a similar (tholeiitic) fractionation trend as seen in the Mg-Fe-Al plots in Fig. 7a–c.
Variations in whole-rock compositions correlate well with changes in mineral abundances determined by thin section petrography. The ultramafic zone is characterized mainly by the accumulation of orthopyroxene and clinopyroxene, and also olivine associated with the peridotitic units PER-1 and PER-2. Clinopyroxene contains up to 0.5–1 wt% Cr2O3, and orthopyroxene about half of this. Olivine usually contains > 2000 ppm Ni, with the highest measured Ni-contents of 3128 ppm (Alapieti 1982; Telenvuo 2017). This leads to high MgO, Cr, and Ni concentrations in the ultramafic zone (Fig. 5, Table 1). The websteritic interlayers are geochemically distinct, with up to 17 wt% CaO (Figs. 5 and 6). Increase in modal intercumulus clinopyroxene and plagioclase causes a steady increase of CaO and Al2O3 towards the mafic zone (Fig. 5), with the last plagioclase-pyroxenites of unit PX-1B containing up to 4.4 wt% Al2O3.
Zirconium concentrations correlate with observed cumulate textures. In the ultramafic zone, the primitive adcumulate pyroxenites of unit PX-1A contain < 10 ppm Zr, that increases to 20–40 ppm in the mesocumulatic pyroxenite and melagabbronorite units above (Fig. 5). Zirconium concentrations stay around this level, until increasing sharply to 100–250 ppm at the beginning of the first homogeneous gabbronorite unit GBNOR-1. This indicates a change in crystallization into strongly orthocumulate or even liquid compositions, with a higher fraction of trapped Zr-enriched residual melt present in the rocks. Increasing K2O contents towards the top of unit GBNOR-1 appears to be associated with increase in modal biotite.
Whole-rock compositional differences between units PER-1 and PER-2 are relatively small compared to PER-3. Average MgO content decreases from 41 wt% in PER-1, to 33 wt% in PER-2, and to 24 wt% in PER-3 (Fig. 6 and Table 1). Concentrations of incompatible elements are similarly much higher in PER-3 (e.g., Al2O3 in Fig. 6). In relation to the low MgO contents, PER-3 contains high Ni (average 850 ppm) and Cr (average 3000 ppm), similar to the other two peridotitic units (Fig. 6). These characteristics correlate with available olivine analyses: average olivine in PER-1 is Fo87 with 2000 ppm Ni; in PER-2 it is Fo84 with 1800 ppm Ni (Alapieti 1982; Telenvuo 2017); and in PER-3 it is Fo82 with 3000 ppm Ni (from author, unpublished data).
The transition from the ultramafic to mafic zone of the layered series comprises a 200 m interval from the top of unit PX-2 to the bottom of unit GBNOR-1. This melagabbronorite subzone includes several smaller reversals in which compositions of, e.g., CaO, FeOtot, MgO, Al2O3, Ni, and Cr oscillate by up to 10% (Figs. 5 and 7b). The compositional fluctuations get smaller with height and decreasing Mg#, ceasing at the beginning of the relatively homogeneous gabbronorite unit GBNOR-1. The most distinct lithological change in this transition zone is plagioclase becoming a cumulus phase, which causes a sharp rise in Al2O3, from 7.5 wt% in unit PX-2 to 15–17 wt% in MGBNOR-1A.
In the ultramafic zone, two relatively S-rich zones with 200–1300 ppm S are found approximately 50 m above and below the unit PER-2. The zone above PER-2 hosts a continuous reef-type PGE-enriched zone (highlighted in Fig. 5), described in detail below. Both zones are enriched in PGEs with 100–500 ppb of 2PGE + Au, with the zone below PER-2 also containing slightly elevated Cu contents of 500–1100 ppm.
Trace disseminated Fe-Cu sulfides are common in the mafic zone, with S concentrations fluctuating around 500 ppm (Fig. 5). The first gabbronorite (GBNOR-1) marks the beginning of Fe-Ti-oxide accumulation. Two minor oxide related peaks in Fe-Ti-V concentrations are found, both with < 700 ppm V. The second peak is found in the gabbronorite-diorite contact, and is associated with disseminated oxides and sulfides. This contact zone contains on average 1700 ppm S but no appreciable PGE (~ 2850 m in Fig. 5), and probably signifies terminal sulfide saturation caused by increasing SiO2 and decreasing FeOtot concentrations.
REE and other lithophile elements
The chrondrite-normalized (CN) REE pattern (Fig. 8a and Table 2) of the marginal series gabbronorite is LREE enriched, with a gentler slope after Sm. LaCN/YbCN is 5.7, LaCN/SmCN is 3.2, and GdCN/YbCN is 1.3, with a slight negative Eu-anomaly (Eu/Eu* = 0.85–1). The trace element pattern (Fig. 8b) is strongly fractionated relative to primitive mantle (PM). The mobile large ion lithophile elements (LILE; Rb, Ba, Sr), and Th and U, are enriched 40–60 times relative to PM (e.g., 200–600 ppm Sr). Both Nb and Ta are below detection limits (Nb < 3 ppm or NbPM < 4.5; Ta < 1 ppm or TaPM < 25). The immobile and less incompatible high field strength elements from La onward have concentrations 2–10 times those of PM with a gently falling slope that is interrupted by negative Ti and P anomalies.
Whole-rock samples from units BD-3, PER-1, PX-1A, PER-2, PX-2, and MGBNOR-1 have been analyzed for REE (Fig. 8c, Table 2). REE values in all cumulate units are below those of the marginal series gabbronorite. Analyses from units BD-3 and PER-1 are generally below detection limits. REE values in bronzitites and websterites of unit PX-1A are close to chondritic, with flat or weakly LREE-enriched patterns. REE concentrations and LREE-enrichment increase from PER-2 upwards, with units PER-2 and PX-2 containing LaCN of ~ 10 on average. Total REE values correlate with whole-rock Zr, suggesting that the REE values of the ultramafic cumulates mainly indicate the relative amount of trapped intercumulus melt.
Characteristics of trace element patterns of cumulate samples (Fig. 8d) are similar to the marginal series gabbronorite, showing enrichment in Th and U, and depletion in Nb, Ta, Ti, and P. The cumulates are Hf-rich with 2–3 ppm Hf (~ 10 times PM), which leads to, e.g., conspicuously high HfN/ZrN (3–9). This characteristic is not present in the marginal series gabbronorite.
Reef-type PGE-enriched zone
The highest concentration of PGEs in the Näränkävaara layered series is found along the border zone between the ultramafic and the mafic units, at a stratigraphic height of about 2350–2400 m (highlighted in Fig. 5). This PGE-enriched zone is intersected by four drill holes (MUV-6, − 16, − 19, − 22) and has a continuous strike of at least 5 km (Fig. 2). Intersections through the zone range from 20 to 85 m in thickness (typically 25 m), with continuous anomalous 2PGE + Au concentrations in the 50–500 ppb range (Fig. 9). Even though this PGE-enriched zone may not merit the term PGE reef, we refer to it as the Salmilammit reef (SL reef) coined after the location of discovery.
Petrography of the Salmilammit reef (SL reef)
The SL reef is hosted in the unit PX-2, which exhibits a series of transitional mineral assemblages and textures between the serpentinized olivine-rich cumulates of unit PER-2 below, and the gabbronoritic units above. The PGE enrichment is typically confined to the upper half of the unit PX-2, beginning 10–20 m after the disappearance of olivine (i.e., end of unit PER-2, see Fig. 9). The footwall rocks are composed of medium-grained, equigranular olivine websterite and plagioclase websterite. These contain approximately 25 vol% of sparse but coarse subspherical poikilitic augite up to 2 cm in diameter, with intercumulus plagioclase increasing to 5–15 vol% after olivine disappears (Fig. 3b). The texture of the mineralized plagioclase websterite is distinct from the pyroxenitic unit below, marked by an increase in the amount of intercumulus augite to approximately 40 vol%, associated with general fining of grain size (Fig. 3c). Fine-medium-grained tabular orthopyroxene grains define lamination in some samples, with rare needle-like grains up to 3 cm long. Biotite appears in trace amounts, and minor quartz is found in drill hole MUV-16. Intercumulus plagioclase increases towards the top of unit to 10–30 vol%. Melagabbronorite with cumulus plagioclase and minor anorthosite form the hanging wall.
In SL reef samples, Ca-poor pyroxene is enstatite (En80, Fs17, Wo3), Ca-rich pyroxene is augite (En49, Fs9, Wo42), and plagioclase is An60. Mineral compositions in drill hole MUV-16 are slightly more evolved with approximately 10% lower An and 5% lower En. Two grains of apatite have been analyzed from drill hole MUV-19, both being chlorapatites with 4–6.5 wt% Cl.
The same sequence of cumulates is found in all examined drill holes, but the PGE enrichment is somewhat erratic in its distribution. In the easternmost drill hole (MUV-22) the PGE enrichment extends 2 m into the poikilitic augite containing subunit below (Fig. 9), which in the other intersections is barren of PGEs. In the westernmost drill hole (MUV-16), the enrichment extends about 10 m into the first melagabbronorites of the mafic zone reaching a total thickness of 85 m.
Another PGE enrichment is found in the unit PX-1B, about 150 m below the SL reef. This lower PGE-enriched zone is about 5–20 m thick, and is hosted in plagioclase-bearing pyroxenite, 30 m below the lower contact of unit PER-2 (intersected by MUV-1 and MUV-3 in Fig. 4). Only three assays are available from this intersection, with grades of 100–250 ppb 2PGE + Au (~ 2150 m in Fig. 5). The host whole-rock compositions are slightly more primitive compared to the SL reef.
Chalcophile element geochemistry
Chalcophile element concentrations of SL reef samples are presented in Table 3. Intersections through the SL reef have an approximately 10 m thick Pd-rich peak with an average of 200–300 ppb Pd (highest 423 ppb) with Pd values tailing off to background values above and below (Fig. 9). The PGE enrichment is clearly Pd-dominated, with the Pd/Pt ratio varying between 0.5–8 (average 2.9). Normalized to 100 wt% sulfide, Pd contents varies between 50 and 300 ppm (Table 3). In drill hole MUV-22, the PGE enrichment begins in the poikilitic augite subunit below the typical host rock with a thin 200 ppb Pt-peak offset about 10 m below the Pd-peak found in other sections (Fig. 9); this is the highest Pt concentration found in the SL reef. Au contents are low with an average of 15 ppb.
Highest base metal and S concentrations are typically offset above the Pd-peak (see MUV-6 in Fig. 9). Even though the PGE enrichment is associated with base metal sulfides, the PGE-enriched samples are low on sulfur with 480 ppm S on average. Highest S in a PGE-enriched sample is 1870 ppm in drill hole MUV-6 (Fig. 9). The eastern drill holes MUV-19 and MUV-22 are very S-poor with an average 250 ppm (Fig. 9). Average Cu is 105 ppm (highest 262 ppm) and average Ni is 370 ppm (highest 573 ppm), with Ni/Cu ranging between 2 and 14 (3.2 on average). The stratigraphically lower PGE enrichment in the unit PX-1B (~ 2150 m in Fig. 5) has higher average Cu (300 ppm) and S (1300 ppm) compared to the SL reef.
The PM-normalized metal pattern of SL reef samples defines a bell-shaped curve typical for PGE-reefs in layered intrusions (Fig. 10). Ru, Ir, and Os (IPGE) are depleted in comparison to the Pd, Pt, and Rh (PPGE), with a distinct Pd-peak, and a slight negative Ru-anomaly. Pd/Ir ratios form two groups which range between 20–80 and 140–160, with an average of 99. Cu/Pd ratios in the ultramafic zone are generally below 5000–8000, in the SL reef between 100 and 500, and increase to 10,000–100,000 immediately above the reef (Fig. 5).
Sulfides and PGM
The SL reef is sulfide-poor with generally less than 0.5 vol% sulfides, but in small localized patches or layers sulfide proportions may reach 1 vol%. Sulfides consist of pyrrhotite intergrown with lesser chalcopyrite and pentlandite. These are found as small, usually less than 0.5 mm anhedral grains interstitial to silicates, typically in contact with plagioclase or augite (Fig. 11a). In the western drill holes (MUV-6 and MUV-16 in Fig. 2), the host pyroxenites and melagabbronorites are variably altered to chlorite and amphiboles, with sulfides partly altered to pyrite and disaggregated by secondary amphiboles. The eastern drill cores (MUV-19 and MUV-22) are unaltered.
In SEM scanning, platinum group minerals (PGM) were only found in drill hole MUV-19, appearing as distinct sub-micrometer scale grains on sulfide grain boundaries and within silicates (Fig. 11b). The largest PGM grain (5 μm) was found in a sulfide–silicate grain boundary. The PGM have been too small for reliable identification, but the most common phases appear to be composed of Pd and Pt sulfides and arsenides. Singular qualitative analyses also include PdGe (marathonite) and an unknown PdSnAuAsFe mineral. PGE contents of the associated sulfide grains have not been determined.
Marginal series as indicator of parental magma composition
Estimation of the parental magma composition of the Näränkävaara layered series was undertaken for two reasons: to facilitate future studies on the petrogenetic relationship between the layered series and the basal dunite, and to better estimate the mineral potential of the layered series.
The melagabbronorite unit intersected in the contact of the Näränkävaara basal dunite and the layered series represents a marginal series, because it exhibits a fine-grained, non-cumulate, heterogeneous texture, with a gradual change into the homogeneous equigranular bronzitite of the layered series. Similar, poorly developed < 20 m thick marginal series are found in the 2.44 Ga Kemi, Tornio, and Penikat intrusions and in the Portimo complex (Fig. 1) (Iljina & Hanski 2005). An average composition of the layered series was calculated by weighting average unit compositions according to their stratigraphic heights (calculations in Appendix 3)—the basal dunite was excluded as discussed later. The weighted average composition was found to be quite similar to the marginal series composition (Table 2; plotted in Fig. 7). Both have high Ni and Cr contents relative to MgO compared to the typical gabbronorites of the layered series (Fig. 6).
To further test this marginal series parental magma hypothesis, we compared the observed crystallization sequences to the results of a fractional crystallization model performed with MELTS for the marginal series gabbronorite composition (rMELTS 1.2.0; Gualda et al. 2012; Ghiorso & Gualda 2015). In the model, the system was assumed to be dry and FeO/FeOtot was assumed to be 0.85 (average FeO/Fe2O3 from Alapieti 1982). Crystallization sequence, as inferred from the relationships of the cumulus phases in the layered series, proceeds in the order: Ol→Opx→Cpx→Pl→Ilm→Mag→Qz. The model results in the same crystallization sequence, with Opx preceding Cpx, when P is 1–4 kbar. Modeled mineral compositions fit measured mineral compositions (Alapieti 1982; Telenvuo 2017) best at P of 2 kbar (Fig. 6). In the 2 kbar model, the first olivine to crystallize is Fo91 at 1400 °C. Orthopyroxene joins the liquidus at 1300 °C after 12 wt% fractionation of olivine. The most primitive olivine suggested by the MELTS model (Fo91) has not been found in the analyzed cumulate rocks of the layered series. This may be due to (1) bias in sampling or mineral analyses, or (2) primitive olivine having accumulated elsewhere (e.g., deposits similar to the basal dunite, as discussed later). At the modeled Ol–Opx boundary, however, the modeled mineral compositions (Fo87.5 and En86) are very close to the compositions measured from the base of unit PER-1 (En87.5 and En85.3; Telenvuo 2017). The modeled temperature for the Opx–Cpx transition (~ 1230 °C) is also similar to that modeled with two-pyroxene thermometry (1200–1100 °C; Alapieti 1982).
As shown in the inset in Fig. 7a, the average olivine composition extrapolated to the Mg-Fe join from the PER-1 and PX-1 cumulates is approximately Fo87. The ultramafic cumulates of units PER-1 and PX-1 can be modeled as mixtures of approximately Fo87 olivine, orthopyroxene ± clinopyroxene, and a liquid corresponding to the marginal series composition (Fig. 6 and 7a), although the actual interstitial liquid is likely to be more evolved.
In summary, the MELTS modeling results and the similarity of the marginal series gabbronorite to the weighted average composition suggest that the marginal series represents a reasonable approximation of the parental magma composition of the Näränkävaara layered series.
Geochemical characteristics of the parental magma
Within the Fennoscandian shield, the parental magmas of the 2.5–2.4 Ga layered intrusions have been interpreted as siliceous high-Mg basalts, sourced from the asthenospheric mantle, with the magmas having incorporated substantial amounts of felsic continental crust during ascent (Amelin & Semenov 1996; Puchtel et al. 1997; Hanski et al. 2001; Yang et al. 2016; Maier et al. 2018). A crustal contamination signature is evident in the intrusions as LREE-enrichment with LaN/YbN of 3–10; and in fractionated PM-normalized trace element patterns, variably enriched in LILE, Th, and U, with prominent negative Nb, Ta, Ti, and P anomalies (Iljina & Hanski 2005; Vuollo & Huhma 2005; Maier et al. 2018).
The parental magma of the Näränkävaara layered series displays all the characteristics of a crustal signature described above (Fig. 8a–b), with slightly more pronounced enrichment in LILE, Th and U compared to other Finnish ~2.45 Ga layered intrusions and dykes. Similar levels of enrichment are found in the komatiitic basalts of the Vetreny belt and in the Bushveld B1 magma, both of which show signs of contamination by up to 15–20 wt% of crustal or sub-continental lithospheric mantle (SCLM) material (Puchtel et al. 1997; Barnes et al. 2010; Kulikov et al. 2010; Günther et al. 2018). The Näränkävaara parental magma also displays a notable positive Sr anomaly with 200–600 ppm Sr (Fig. 8b), similar to average concentrations of Sr in continental crust (300 ppm; Rudnick & Fountain 1995).
Major element concentrations in the Näränkävaara parental magma also point to a relatively high degree of contamination with felsic materials. Its primitive characteristics—high MgO (14–15 wt%), Ni (300–500 ppm), and Cr (1450–1750 ppm)—are concurrent with untypically high SiO2 (54–55 wt%) compared to the other Finnish layered intrusions (Alapieti & Lahtinen 2002; Iljina & Hanski 2005). The Vetreny belt komatiitic basalts are described as having high MgO of 9–18 wt%, but contain < 53 wt% SiO2 (Kulikov et al. 2010). A group of fractionated ~ 2.45 Ga boninite-norite dykes with MgO between 3 and 20 wt% (Vuollo & Huhma 2005) covers the compositional range of the inferred parental magmas of the Finnish layered intrusions. The Näränkävaara parental magma plots in the outer limit of the compositional field of these dykes in regard to the concurrently high SiO2, MgO, and Cr.
Implications of the marginal series for the basal dunite
If the Näränkävaara layered intrusion magma developed a marginal series against the basal dunite, then the basal dunite must predate the emplacement of the layered series (2436 ± 5 Ma; Alapieti 1982) and thus belong to an earlier magmatic event. The petrogenesis of the Näränkävaara basal dunite has not been studied in detail, however, and the absolute age difference is not known. Taking into account the sheared contact between the basal dunite and the layered series, and the ubiquitous faulting present in the intrusion—with dislocations up to several hundred meters—it is conceivable that the marginal series was originally emplaced against a roof wall of Archean basement, and later faulted into its current position.
The Näränkävaara basal dunite is distinctly more extensive, magnesian, and homogeneous in composition compared to other dunitic or peridotitic units in ~ 2.45 Ga Finnish intrusions. Dunitic cumulates can be formed by accumulation of olivine in basal sections of (rhythmic) mafic intrusions, but continuous, up to 2 km thick dunites in layered intrusions are rare. The mafic-ultramafic Burakovsky intrusion in Russian Karelia (Fig. 1) hosts an up to 3- to 6-km-thick relatively homogeneous basal dunite (Chistyakov & Sharkov 2008), but the exact method of its formation has not been worked out. Dunitic cumulates up to 1 km thick are present in the Great Dyke of Zimbabwe, where they are found interlayered with chromitite seams and minor harzburgites, having formed over several magma pulses (Wilson 1996). Formation of an extensive olivine adcumulate from a parental magma with 14–15 wt% MgO would likely require repeated recharge or flow-through. If the Näränkävaara basal dunite belongs to the same ~ 2.45 Ga magmatic event as the layered series, then it would probably represent an open system feeder channel similar to the Great Dyke, having fed volcanic systems such as the 2.44 Ga komatiitic basalts described from the Vetreny belt (Kulikov et al. 2010).
Thick dunite successions may also represent Archean komatiitic environments such as portions of lava flow channels (Barnes et al. 1988). Therefore, another possibility is that the basal dunite represents an older, Archean komatiitic wall rock to the layered intrusion, a segment of a greenstone belt that are common in the Archean of the Fennoscandian shield. The petrogenesis of the basal dunite is beyond the scope of this article and will be assessed in future studies.
Magmatic evolution of the layered series
The general magmatic evolution of the Näränkävaara layered series has been inferred from variations in cumulate whole-rock compositions (e.g., Figs. 5 and 7). These give the impression of mostly closed system fractionation of a large initial batch of magma, interrupted by open system recharge: first before the onset of plagioclase fractionation (i.e., the PER-2 reversal and the melagabbronorite subzone); and later in the gabbronorites of the mafic zone (i.e., the PER-3 reversal). The Fe-enrichment in the gabbronorites caused by late crystallization of magnetite indicates a tholeiitic fractionation trend (Fig. 7).
Petrography indicates that crystallization in the ultramafic and melagabbronoritic zones is controlled by cumulus processes. The sharply increasing Zr contents to about 100–200 ppm provide strong evidence that the gabbronorites from unit GBNOR-1 upwards represent orthocumulate or melt compositions (Fig. 5). MELTS modeling of the parental magma shows that plagioclase begins to crystallize after about 50% fractionation. Assuming Zr was completely incompatible, this would correspond to doubling of the Zr in the parental magma to 80–120 ppm in the residual melt (cf. marginal series composition in Table 2). This suggests a near-liquid composition for the gabbronorites, although cumulus plagioclase is observed in drill core throughout the unit.
Some of the more evolved gabbronoritic rocks are untypically biotite- and alkali-rich (Figs. 5 and 7b). No xenoliths or other direct evidence of in-situ wall-rock assimilation has been found, so any possible assimilant has completely mixed with the magma (whether before or after emplacement), with the incompatible elements enriched in the residual melt from which the gabbronorites crystallized.
Evidence for magma replenishment
Two abrupt reversals restart differentiation from more primitive compositions (units PER-2 and PER-3 in Figs. 7a–b). The reversals are interpreted as new pulses of relatively primitive magma into a partly differentiated and consolidated magma chamber. This is supported by the reappearance of cumulus olivine after a series of lower temperature cumulates, and increase in MgO, Ni, and Cr in whole-rock compositions (Figs. 5 and 6). Chromitite seams are not found anywhere in the layered series, the formation of which could be expected at the lower contacts of the peridotitic reversals (Irvine 1975). At the base of unit PER-2, orthopyroxene En-contents increases by 1–2 mol% compared to the unit below (Telenvuo 2017). This increase is similar in scale as in the rhythmic reversals in the pyroxenite successions of the Great Dyke, attributed to influxes of primitive magma (Wilson 1996).
A weakly PGE-enriched tail following the PER-3 reversal (~ 50 ppb 2PGE + Au; Fig. 5) suggests influx of new comparatively PGE-rich magma. The Fe-Ti-oxide-bearing gabbronorites immediately below PER-3 are geochemically similar to those found at the gabbronorite-diorite contact (Fig. 5). Modeling indicates Fe-Ti oxide and sulfide saturation occur after about 70–80% fractional crystallization of the parental magma, suggesting that differentiation of the residual magma may have advanced quite far at the time of the PER-3 reversal. The alteration textures and high modal biotite found in the PER-3 peridotites and pyroxenites are likely related to mixing of the incipient PER-3 magma with the volatile and incompatible element enriched residual magma.
Petrographical and compositional similarities (e.g., trace element ratios) between the three peridotitic units point to a single parental magma type. They all contain high Cr, so none of them represent the low-Cr magma type described from the mafic and megacyclic layered intrusions of the Tornio-Näränkävaara belt (Iljina & Hanski 2005). For PER-1 and PER-2, there is a strong positive correlation between whole-rock (and olivine) MgO and Ni (Fig. 6), implying a shared parental magma with its composition controlled by olivine fractionation. The decreasing olivine Fo contents between the reversals suggests progressive fractionation in a parallel staging magma chamber before emplacement in the layered series (similar to Penikat intrusion, Maier et al. 2018). The gradual increase in incompatible elements with stratigraphic height from PER-1 to PER-2 to PER-3 (Fig. 6) is at least partially explained by increasing intercumulus material. This may also, at least in part, explain the decrease in Fo content between the reversals, because increase in modal intercumulus facilitates post-cumulus re-equilibration of olivine to a lower Fo content (the ”trapped liquid shift”; Barnes 1986). The higher Ni-content in the PER-3 olivine at a lower Fo content compared to PER-2 suggests a less fractionated source for PER-3.
Transition zone between ultramafic and mafic zones
The transition zone from the ultramafic to the mafic zone (melagabbronorite subzone) includes several smaller alternating reversals between pyroxenite and melagabbronorite (note Ni between units PER-2 and GBNOR-1 in Fig. 5; also smaller reversals in Fig. 7b). Whole-rock compositions of the alternating units evolve towards a lower Mg# upwards in stratigraphy, with the compositional changes getting progressively smaller, until reaching the homogeneous unit GBNOR-1. The origin of these compositional oscillations is not known. It can be speculated that at least the unit PX-3 is related to magmatic replenishment, based on the slight PGE enrichment associated with it (Fig. 5). It is possible that the melagabbronorite subzone represents a series of small replenishments of primivite magma, followed each time by fractionation and deposition of a relatively primitive basal cumulate unit (high-Ni units in Fig. 5), followed by consequent convective overturn (mixing) and deposition of a more evolved cumulate layer (Huppert & Sparks 1984).
The chemical composition of the lowermost melagabbronorite unit (MGBNOR-1A) is distinct, with the lowest FeO/Al2O3 ratios (0.2–0.3) relative to Mg# (75–80) in the layered series. Outcrop samples from the SE block of the layered series (Heinivaara gabbronorites in Fig. 2) fall into the same limited compositional range, some with anomalous 2PGE + Au of 100–200 ppb. These outcrops very likely represent the stratigraphic level of the transition zone in the SE block.
Classification, characteristics, and comparisons
The uneconomic PGE enrichment in the Näränkävaara layered series (SL reef) can be classified as a stratabound sulfide-associated PGE-mineralization, i.e. reef type. The SL reef can also be classified as an offset-reef, because the highest Cu, S, and Au concentrations are offset about 10 m above peak PGE concentrations (Fig. 9) (Mungall 2007). High-grade offset-type PGE reefs in a similar stratigraphic position are found in, e.g., the Great Dyke (Lower and Main Sulfide Zones; Wilson 1996, 2001) and the Munni Munni complex (Ferguson reef; Hoatson & Keays 1989; Barnes & Hoatson 1994). The low-grade SL reef is similarly found in a relatively thick and homogeneous cumulate unit towards the top of the ultramafic zone, 5–20 m below the first appearance of cumulus plagioclase. For some reason, the processes that produced high-grade mineralization in the other two intrusions did not occur in Näränkävaara.
PGE reefs in a similar stratigraphic position as the Näränkävaara SL reef have not been described from other 2.44 Ga mafic-ultramafic layered intrusions of the Tornio-Näränkävaara belt. The Sompujärvi (SJ), Paasivaara (PV) and Ala-Penikka (AP) reefs of the Penikat intrusion, and the Siika-Kämä (SK) and Rytikangas (RK) reefs of the Portimo complex (Fig. 1) are located in megacyclic intrusions (Alapieti & Lahtinen 2002; Iljina et al. 2015 and references therein). The stratigraphically lowermost PGE reefs are found near the bases of megacyclic units (SJ, SK) at a level where the high-Cr megacyclic units transition into low-Cr units. In addition, reefs are found within the megacyclic units in variable gabbroic and anorthositic units from this stratigraphic position upwards (AP, PV, RK) (Iljina et al. 2015). As described previously, the Näränkävaara SL reef apparently does not occur at a level where there was influx of a Cr-poor magma. In the Western Intrusions of the KLIC, the low-grade Römetölväs (RT) reef is associated with an influx of primitive magma into evolved gabbroic cumulates (Karinen 2010).
Sulfide tenors and metal ratios in the SL reef samples attest of a high R-factor PGE reef forming event. Large inaccuracies are introduced when compositions with less than 2–3 wt% sulfide are normalized to 100 wt% sulfide (Barnes & Lightfoot 2005). The SL reef is sulfide-poor, and the calculations regarding sulfide tenor and R-factor are provided only to estimate their order of magnitude. The high PGE tenors found in the SL reef sulfides (50–300 ppm Pd normalized to 100 wt% sulfide) are slightly lower—but in a similar range—as those described from other sulfide associated PGE reefs in 2.45 Ga Finnish layered intrusions (see Table 3). The SL reef sulfide tenors correspond to R-factors (Campbell & Naldrett 1979) in the 105 range using marginal series from Table 2 as the original composition, and a Pd Dsil/sulf of 105 (Mungall & Brenan 2014). Primitive mantle normalized metal patterns in Fig. 10 are also similar in shape between the SL reef and other sulfide associated PGE reefs from Finnish 2.45 Ga layered intrusions, except for the lower amounts of PGE in Näränkävaara.
Recalculating the 2PGE + Au grades of the on average 25 m thick SL reef to a vertical thickness of 1 m corresponds to concentrations of 2.5–4.5 ppm 2PGE + Au, depending on cutoff. By comparison, the Merensky reef is approximately 1 m thick with an average of 5 ppm of 2PGE + Au (Bristow et al. 1993). This implies at least a moderate PGE budget in the SL reef-forming magma; however, the concentrations have been diluted over a large vertical extent. On the Cu/Pd vs. Pd diagram in Fig. 12, samples from the SL reef plot on a similar trend as other Finnish PGE reefs (except RT) that indicates high R-factors in the 105 range (Barnes et al. 1993). However, the highest Pd concentrations in the SL reef (~ 0.5 ppm Pd) are much lower in comparison to those of the other Finnish PGE reefs (5–10 ppm Pd). According to the model, this is a function of the other reefs having formed more sulfides in the 1 vol% range, compared with the < 0.1 vol% of SL reef. This suggests that the SL reef sulfides were formed from a relatively PGE-fertile magma under high-R factor conditions, but that the low amount of precipitated and accumulated sulfides at the time of reef forming may have been a limiting factor for the formation of a high-grade PGE reef.
Sulfur saturation and hypothesis for origin of SL reef
The SL reef sulflides and PGM exhibit textures commonly found in primary magmatic sulfides formed through cooling and fractionation of sulfide solid solutions (Barnes & Lightfoot 2005). It is possible that some post-cumulus remobilization of sulfides and PGEs has occurred (drill holes MUV-6 and MUV-16), but it is thought to be minor on the scale of the whole layered series, and not a primary mechanism for the formation of the PGE-enrichment.
Significant changes in the Cu/Pd ratio through the magmatic stratigraphy of a layered intrusion can indicate sulfide saturation and reef-forming events (Barnes et al. 1993). The Cu/Pd ratios of the marginal series (~ 8000) and the weighted average of the layered series (~ 5000) are below primitive mantle ratios (8000–10,000), implying a PGE-fertile melt (Barnes & Lightfoot 2005). The Cu/Pd ratios in the ultramafic zone also generally remain below 5000–8000 (Fig. 5), suggesting that significant sulfide saturation has not occurred below the SL reef level. The SL reef is associated with a major change in Cu/Pd, from < 5000 to 30,000–50,000 (highest 200,000) in the melagabbronorites above the reef. This suggests that formation of the SL reef was the first major sulfide saturation event in the layered series magma. Rocks of the mafic zone above the SL reef are commonly sulfide-bearing with about 500 ppm S but are almost barren of PGEs (Fig. 5). This suggests that formation of the SL reef depleted the residual magma of PGEs.
The offset-type metal distribution in the SL reef and high sulfide tenor and R-factor suggest that after precipitation the sulfides equilibrated in contact with a large body of (convecting) magma with the PGEs concentrated into the first formed sulfides by the higher distribution coefficients (Barnes 1993; Wilson 2001) and higher rates of diffusion (Mungall 2002) of the PGEs compared to base metals. The first sulfides would thus deplete the remaining magma of PGEs. The offset-distribution also suggests that the sulfides were accumulated and disconnected from the melt-interface relatively quickly, thus prohibiting further equilibration. The same argument would also imply only minor redistribution of sulfides after precipitation, as this would be assumed to homogenize the metal distribution. Rather, these observations point to continuous in-situ formation of sulfides in contact with a convecting magma (see Latypov et al. 2015).
Excluding samples with > 20 ppb Pd, the peridotites and pyroxenites below PER-2 have a combined average Cu/Pd ratio of approximately 5000, whereas from PER-2 upward peridotitic and pyroxenitic samples have a higher average of approximately 10,000 (Fig. 12). This implies that the magma associated with the PER-2 reversal may have already been PGE-depleted by the time of its emplacement in the layered series, relative to the original parental magma. Whether this had some impact on the low grade of the SL reef is not known.
It seems that PGE enrichment similar to the SL reef began to develop already about 50 m below the PER-2 reversal near the top of the unit PX-1B, and was probably halted by the PER-2 reversal (Fig. 5). This lower PGE enrichment is associated with similar changes in Cu/Pd ratios as the SL reef (Fig. 12). Perhaps the PER-2 magma was denser compared to the residual magma in the chamber, and, instead of causing turbulent pluming and mixing upon emplacement (like in Munni Munni; Barnes & Hoatson 1994), it spread out along the base of the chamber (like hypothesized for the Merensky Reef; Latypov et al. 2015). The high FeO and low SiO2 contents would have inhibited sulfide saturation, possibly leading to reabsorption of existing sulfides. After deposition of olivine and pyroxene cumulates, the magma would have again reached S-saturation, possibly related to a FeO minima on the liquid line of descent caused by fractionation of mafic silicates (see Li & Ripley 2005). During the SL reef formation, silicates and a relatively small amount of sulfides fractionated continuously and simultaneously and both were accumulated more or less in-situ leading to the silicates ”diluting” and extending the reef (Fig. 9). The first precipitated sulfides efficiently scavenged the magma of PGEs and formed the offset-type metal distribution. The magma continued to crystallize at sulfide saturation almost throughout the mafic zone, with a slight recharge of PGEs brought in by the PER-3 magma (Fig. 5). Terminal sulfide saturation, barren of PGEs, was reached at the gabbronorite-diorite contact, probably brought on by a decrease in FeO related to Fe-Ti oxide fractionation.
Our data and observations lead to the following conclusions:
The 2.44 Ga Näränkävaara layered intrusion represents a mafic-ultramafic layered series with a thick peridotitic-to-pyroxenitic ultramafic zone, and a gabbronoritic-to-dioritic mafic zone. The cumulates are relatively unaltered, and follow a tholeiitic fractionation trend with two reversals back to Mg-rich compositions. The reversals are thought to be caused by replenishment with magmas of broadly similar composition as the original parental magma of the layered series, but in different states of fractionation.
Below the layered series is an extensive, approximately 2-km-thick basal dunite mostly composed of serpentinized olivine ad- and mesocumulates. The layered series includes a marginal series emplaced against the basal dunite, indicating that the basal dunite is older than the layered intrusion. By how much is not known.
Layered series parental magma composition has been inferred from a marginal series melagabbronorite. It contains 54.6% SiO2, 0.4% TiO2, 11.0% Al2O3, 14.1% MgO, 8.6% FeO, 500 ppm Ni, 1750 ppm Cr, 6.1 ppb Pd, and 8.2 ppb Pt. The similarity of major and trace element concentrations between the Näränkävaara parental magma and other intrusions of the 2.44 Ga Tornio-Näränkävaara belt indicate that they belong to the same large scale magmatic event. The Näränkävaara parental magma represents a relatively primitive but highly contaminated end-member in the context of the early Paleoproterozoic Fennoscandian SHMB magmatism.
The layered series hosts an uneconomic offset-type PGE reef (SL reef) along the mafic-ultramafic transition zone, in a similar stratigraphic location as in the Munni Munni and the Great Dyke intrusions. Metal ratios and sulfide tenors give evidence of a high R-factor PGE reef forming event, similar to those interpreted for other sulfide associated PGE reefs in 2.45 Ga Finnish layered intrusions.
Low whole-rock PGE grades of the SL reef seem to be caused by low rate of sulfide accumulation relative to simultaneous silicate accumulation, leading to dilution of high-grade sulfides over an average thickness of 25 m. Influx of new, possibly PGE-depleted magma at the onset of sulfide saturation may have halted the reef-forming process and diluted the residual magma in regard to PGE.
Formula used for calculation of Mg#: 100 × ((XMgO/40.3044)/((XMgO/40.3044) + (0.9 × (XFeOtot/71.8464)))); where X is wt% oxide.
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We would like to thank the reviewers Shenghong Yang and Stephen J. Barnes for valuable comments that greatly improved the manuscript and guest editor Ferenc Molnár for editorial handling of the manuscript. We would also like to thank the K.H. Renlund Foundation for providing a Ph.D. research grant to V. Järvinen. This work was also supported by Academy of Finland Grants 295129 and 306962 (J. Heinonen). The GTK projects linked to Ni-Cu-Co-PGE potential in Finland are thanked for providing the historical data and new analyses required for completion of this study. Lassi Pakkanen and Bo Johanson from GTK mineral laboratory are thanked for mineralogical analyses and guidance. Marko Moilanen and Leena Palmu from the University of Oulu are thanked for their help with historical XRF analyses. Pentti Järvinen is thanked for reviews of early versions of this manuscript. Special thanks to everyone involved with the GTK–University of Helsinki Eastern Lapland Komatiite project for establishing a fun, energetic, and highly motivated research team.
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Järvinen, V., Halkoaho, T., Konnunaho, J. et al. Parental magma, magmatic stratigraphy, and reef-type PGE enrichment of the 2.44-Ga mafic-ultramafic Näränkävaara layered intrusion, Northern Finland. Miner Deposita 55, 1535–1560 (2020). https://doi.org/10.1007/s00126-019-00934-z
- Layered intrusion
- Magmatic stratigraphy
- Parental magma
- PGE reef