Kola

Rare-metal ore occurrences, related to the Late Archean A-type granites from the Keivy zone (NE Fennoscandian shield)

Zozulya, D. and Eby, N.

The Keivy alkali granite complex consists of 2650-2660 Ma aegirine-arfvedsonite granites (six sheet-like massifs of a few hundred meters thickness and a total exposure area of ca. 2500 km²), 2670 Ma aegirine-augite-lepidomelane-ferrohastingsite syenogranites that occur in the margins of some massifs, and 2680 Ma lepidomelane-ferrohastingsite syenite dykes that intrude the TTG basement of the Central Kola terrane (NE Fennoscandian shield). Small dike-like bodies of 2610 Ma nepheline syenite cut the West Keivy alkali granite massif. On standard trace element discriminant diagrams (Whalen et al., 1987; Pearce et al., 1984; Eby, 1990) the Keivy alkali granites plot as within-plate or post-collisional A-type granitoids. The least evolved syenogranites plot in the EM2-field on the εSr - εNd diagram. The low Y/Nb and Yb/Ta ratios for the associated nepheline syenite indicate an OIB affinity. The rocks of the Keivy complex are extremely enriched in Zr (300-5000 ppm), Y (40-500 ppm), Nb (20-600 ppm), Rb (160-900 ppm), REE (100-1000 times chondrites). The numerous associated Zr-Y-REE-Nb ore occurrences and deposits are associated with different lithologies and formed by different genetic processes (Fig.; Table). The Keivy alkali granite complex is the only known Archean fertile A-type granite in the world.

Fig. 1. Location of the Keivy alkaline granite complex (top) and geological structure of the Rovozero rare-metal deposit related to the West Keivy alkali granite massif (bottom), NE Fennoscandian shield. Key to the legend: 1 – silexite; 2 – mineralized granite; 3 – aegirine-arfvedsonite granite; 4 – Keivy gneiss complex; 5 – dip, strike, linearity.

Table 1. Typology, geological position, mineralogy and geochemical specialization of the rare-metal ore occurrences related to the Keivy A-type alkali granite complex from the NE Fennoscandian shield [some data for amazonite pegmatite and silexite were compiled using (Bel’kov et al., 1988; Voloshin, Pakhomovsky, 1986)].

Genetic type	Geological position	Main rock-forming minerals	Rare-metal mineralization	Geochemical specialisation and type by Cherny (1991)
Mineralised granites-I	Apical parts of massifs	Quartz, albite, microcline, magnetite, aegirine	Zircon, thorite, chevkinite, allanite, fergusonite, britholite-(Y), bastnäsite	Zr, Y, HREE, Th, Nb (Nb/Ta>15) NYF-type
Mineralised granites-II	Bottom parts of massifs	Quartz, microcline, magnetite, chlorite, ±hematite	Zircon, thorite, fluorite, cassiterite, pyrochlore	Zr, REE, Th, Nb (Nb/Ta=8-10), Sn, Li, F NYF-LCT-type
Albitites	Exocontact zones	Quartz, albite, aegirine, arfvedsonite	Zircon, thorite, titanite, aeshynite-(Y), thalenite, britholite-(Y)	Zr, Y, HREE, Th, Nb (Nb/Ta=20), Ti NYF-type
Microclinites	Bottom and inner parts of massifs	Microcline, quartz, protolithionite	Zircon, thorite, pyrochlore-(W), cassiterite	Zr, REE, Th, Nb (Nb/Ta=8), Sn, W, Li NYF-LCT-type
Apobasic metasomatite	Contact zones of granites with basic rocks	Quartz, albite, microcline, aegirine, arfvedsonite, ferrohastingsite, lepidomelane	Zircon, thorite, epidote-(REE), fergusonite, chevkinite, gadolinite, pyrochlore, fluorite, cassiterite, danalite, monazite	Zr, REE, Th, Nb (Nb/Ta=10 -24), Sn, F, Be, W NYF-LCT or NYF type
Silexites-I	Exocontact zones	Quartz, arfvedsonite, aegirine, ilmenite, lepidomelane, magnetite, albite	Zircon, fergusonite, britholite-(Y), chevkinite, bastnäsite, thorite, fluorite	Zr, Y, HREE, Nb (Nb/Ta=15 -20), Th, Ti, F NYF-type
Silexites-II	Endocontact zones	Quartz, aegirine, arfvedsonite, magnetite, ilmenite, ±microcline	Zircon, fergusonite, britholite-(Y), chevkinite, yttrialite, thorite,	Zr, Y, HREE, Nb (Nb/Ta> 20), Th, Ti NYF-type
Quartz-feldspar-astrophylite pegmatites	Apical parts of massifs	Quartz, microcline, arfvedsonite, ±albite	Astrophyllite, gadolinite	Y, HREE, Ti, Be NYF-type
Quartz-microcline pegmatites	Contact zones	Quartz, microcline, magnetite, ±albite, ±aegirine	Fergusonite, chevkinite, britholite-(Y), aeshynite-(Y), gadolinite	Y, Nb (HREE, Be) NYF-type
Amazonite pegmatites	Roof country rocks (gneiss of Keivy complex)	Amazonite, quartz, albite, lepidomelane	Microlite, betafite, pyrochlore-(W), keyviite, fluorite-(Y), xenotime, gadolinite, genthelvite, polylithionite, kainosite, cassiterite, galena, molybdenite	Y, Yb, Nb, Ta, F, Li, Sn (Pb, W, Mo) NYF-LCT-type
Hydrothermal veins	Apical parts of massifs and roof country rocks	Quartz, riebeckite, ±microcline	Zircon, ilmenite, fluorite, astrophyllite	(Zr, Ti, F) NYF-type
Mineralised nepheline syenites	Linear zones in magmatic body	Nepheline, aegirine, microcline, albite, lepidomelane	Zircon, britholite-(Y), pyrochlore, fluorite, meliphanite, behoite	Zr, Y, REE, Nb, F, Be

References:

Bel’kov, I.V., Batieva, I.D., Vinogradova, G.V., Vinogradov, A.N., 1988. Mineralization and fluid regime of the contact zones in the alkali granite intrusions. Apatity: Kola Science Centre. (in Russian)

Černy, P., 1991. Rare-element granitic pegmatites. Part I: anatomy and internal evolution of pegmatite deposits. Geosciences Canada 16 (2), 49-67.

Eby, G.N., 1990. The A-type granitoids: a review of their occurrence and chemical characteristics and speculations on their petrogenesis. Lithos 26, 115-134.

Pearce, J., Harris, N., Tindle, A., 1984. Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. Journal of Petrology 25, 956-983.

Voloshin, A.V., Pakhomovsky, Ya.A., 1986. Minerals and evolution of mineral genesis in amazonite pegmatites of the Kola Peninsula. Leningrad, Nauka. (in Russian)

Whalen, J., Currie, K., Chappell, B., 1987. A-type granites: geochemical characteristics, discrimination and petrogenesis. Contributions to Mineralogy and Petrology 95, 407-419.

Electronic version of paper

Back to publications.

Geochemistry and mantle sources for Archean alkaline rocks from Greenland, the Baltic and Northern Norway

Zozulya, D., Bayanova, T., Eby, N., Kullerud, K., and Ravna, E.

Archean alkaline complexes are extremely rare but are of particular interest because the magmas have a mantle origin. Given their high Sr and Nd contents, crustal contamination has only a minor impact on the mantle-derived isotopic signatures. Therefore, they can provide valuable information on the isotopic composition of the subcontinental mantle and geodynamics in Archean. The previously reported Late Archean alkaline complexes (2.7-2.6 Ga) from the Canadian and Australian shields belong to the potassic series, are depleted in LIL and HFS elements, and are related to subduction, thereby forming in a compressive tectonic environment and having a depleted mantle source. The absence of Archean sodic alkaline complexes forming in extensional environments was mainly ascribed to the absence of metasomatic processes in the mantle and lower lithosphere (Blichert-Toft et al., 1996).

Greenland Archean alkaline complexes (2698-2664 Ma syn- to post-kinematic pyroxenites, hornblendites, norites and diorites, monzodiorites, monzonites, syenites, nephelenitic rocks and carbonatites) are found in the Skjoldungen province in the SE Nain craton (Blichert-Toft et al., 1995). The Baltic examples are the 2610 Ma Siilinjarvi carbonatite-glimmerite intrusion, SW Karelian craton, and the Keivy alkaline province (2670-2654 Ma anorogenic peralkaline granites, syenogranites, syenites and massif-type anorthosites; 2610 Ma OIB-like nepheline syenites and essexites), Kola craton. The 2695 Ma Mikkelvik nepheline syenite stock was recently identified in the West Tromso Archean basement, Northern Norway.

The alkaline rocks mostly show high contents of some incompatible elements (REE, Zr, Y, Nb, and Rb, high Ga/Al (for granite) and low Y/Nb and Yb/Ta (for syenite) ratios) characteristic of an enriched mantle source. Near chondritic and negative eNd (0 to -5) and near chondritic and positive eSr (0 to +50) suggest the mantle source is transitional between the chondritic and enriched mantle (EM2) reservoirs. From the similar geochemical signatures it is suggested that the Archean alkaline magmatism from Greenland, the Baltic and Northern Norway resulted from plume development in a sub-lithospheric mantle having enriched characteristics due to subduction. The observed differences in geochemical features are in accordance with a sequence of magmatic events during the plume development: 2.70-2.66 Ga - initiation, near chondritic and slightly enriched reservoir due to subducted and recycled oceanic crust, mafic shoshonitic parental magma; 2.65-2.61 Ga - evolved enriched reservoir, OIB-like and Na-rich parental magma.

Electronic version of paper

Back to publications.

The anorthosite - A-type peralkaline granite connection: a case study from the Keivy Terrane, Baltic Shield

Zozulya, D.R. and Eby, G.N.

A suite of massif-type anorthosites and peralkaline granites is found in the Archean Keivy terrane of the NE Baltic shield. The 2660-2680 Ma Keivy anorthosite complex consists of several large (up to the 170 km²) lopoliths composed mainly of anorthosite and gabbro-anorthosite and marginal gabbro-norite and titanomagnetite-rich troctolite bodies. The Keivy anorthosites have low REE abundances (Ce 5-23 and Yb 1.5-6.8 times chondrites), fractionated REE distributions (chondrite-normalized La/Yb ratios are 4-10) and positive Eu anomalies. The comagmatic gabbro-norites have similar REE patterns, but no or negligible positive Eu anomalies. The rocks show high compatible element (Sc, 25-40 ppm and Sr, 460-670 ppm) abundances. As the chondrite-normalized La/Yb ratios do not correlate with REE abundances, an enriched source for the primary magmas is proposed. The enriched source for the Keivy anorthosites has low e_Nd (-0.15 to -0.24) and low Y/Nb ratios (0.6-1.3). From the geochemical data it is inferred that the primary magma was an alkaline/subalkaline basalt magma forming in a within-plate setting.

The Keivy peralkaline granite complex consists of 2650-2660 Ma peralkaline granites, 2670 Ma syenogranites, and 2680 Ma alkaline syenites. The granites form sheet-like bodies with thicknesses of a few hundred meters, but have vast exposed areas (100-1200 km²). They are metamorphosed to amphibolite facies and are bounded by gabbro-anorthosite. The rocks of the Keivy complex are extremely enriched in Zr (300-1900 ppm), Y (40-150 ppm), Nb (20-150 ppm), REE (100-1000 times chondrites) and Rb (160-900 ppm), have associated Zr-REE ore occurrences, are very low in Sc (0.3-1.3 ppm) and Sr (10-30 ppm), show negative Eu anomalies, have normalized La/Yb ratios of 1.5-13 and high Ga/Al ratios. On standard trace element discriminant diagrams the Keivy peralkaline granites plot as within-plate or post-collisional A-type granitoids. The low Y/Nb and Yb/Ta ratios for associated alkaline syenites point to their OIB affinities. The least metamorphosed and least evolved rocks plot in the EM2-field on the e_Sr - e_Nd diagram.

The close temporal and spatial association of the gabbro-anorthosites and the peralkaline granites and their similar magma sources suggest a genetic relationship. One possible model is protracted fractional crystallization of a primary alkaline basalt magma with removal of plagioclase during the early stages of crystallization (forming a Ca- and Al-enriched cumulate, anorthosite) and alkali, iron and HFSE enrichment of the residual melt leading to the peralkaline granites.

Electronic version of paper

Back to publications.

Geology and age of the Late Archaean Keivy alkaline province, NE Baltic Shield

Zozulya, D. R., Bayanova, T. B., and Eby, G. N.

The Keivy alkaline province, Kola Peninsula, consists of six peralkaline granite bodies, alkaline syenogranite dikes, and two nepheline syenite intrusions emplaced between the tonalite-trondhjemite-granodiorite basement and the supracrustal Keivy terrane. U-Pb zircon ages for the Keivy alkaline province range from 2613 to 2682 Ma and, for the spatially associated gabbro-anorthosite complexes, from 2659 to 2668 Ma. The Keivy alkaline granitoids are geochemically different from other Late Archean alkaline rocks inferred to have been emplaced in subduction zone settings. The Keivy alkaline province may represent the earliest example of magmatism associate with continental rifting and the involvement of a mantle plume with oceanic island basalt-like characteristics.

Request electronic reprint

Back to publications.

Late Archean Felsic Alkaline Magmatism: Geology, Geochemistry, and Tectonic Setting

Zozulya, D. and Eby, N.

The oldest known examples of felsic alkaline magmatism are from the Superior province, Yilgarn Craton, and Fennoscandian Shield. These are the 2680-2670 Ma alkaline granites and associated nepheline syenite stocks of the Abitibi greenstone belt (Sutcliffe et al., 1990; Corfu et al., 1991): the 2650-2630 Ma alkaline granites and syenites of the Mount Monger, Emu, Claypan, and Ninnis suites of the Eastern Goldfields granite-greenstone terrane (Libby, 1989; Smithies, Champion, 1999): and the 2610-2680 Ma alkaline granites, syenogranites, and nepheline syenites of the Keivy complex of the Central Kola granite-greenstone domain (Mitrofanov et al., 2000; Zozulya et al., 2001). The Superior and Yilgarn felsic alkaline rocks form small (10-90 km²) stocks that are spatially and temporally associated with potassic volcanics and lamprophyres. The Kola examples form sheet-like bodies with thicknesses of a few hundred meters, but have vast exposed areas (100-1300 km²). They are metamorphosed to amphibolite facies and are closely associated with large gabbro-anorthosite bodies. While the various provinces have the common mineralogical (anhydrous primary phases, Fe- and Na-rich mafic silicates) and petrochemical (low Ca, Mg, Al, and high total alkalis) characteristics of alkaline granites they show different trace element characteristics and mineralization types. The Superior and Yilgarn alkaline granites and syenites have extremely low Ga/Al and high (La/Yb)n ratios, no Eu anomaly, and related Au mineralization. Based on these geochemical features the granites were formed in a subduction environment and correspond to volcanic arc granites. In contrast, the rocks of the Keivy complex are extremely enriched in Zr, Y, Nb, REE, and Rb, have associated Zr-REE ore occurrences, are very low in Ba and Sr, show distinct negative Eu anomalies, and have low (La/Yb)n and high Ga/Al similar to A-type granitoids forming in within plate settings. The low Y/Nb and Yb/Ta ratios for the associated nepheline syenites point to their OIB affinities. The felsic alkaline magmatism of the Superior and Yilgarn provinces is related to the final stages of greenstone-belt formation (the ages are 2725-2680 Ma and 2720-2675 Ma, respectively). The Keivy complex was formed long after the development of the adjacent greenstone belt (the formation age is 2920-2830 Ma) and reflects the influence of a mantle plume.

Electronic version of paper

Back to publications.


Kola Science Centre, Apatity.	Field transport. Truck and tracked vehicle.	Field camp in the Keivy terrane.	The evening fish run.

Lunch in the field. Sasha Yefimov (l) and Dmitry Zozulya (r).	In the field. Gremayka pluton.	Keivy terrane. Pana intrusion in the background.	Fall in the Kola Peninsula.

Getting ready for late evening baseball. Sasha Yefimov (l), Valentina Basalayera (c), and Dmitry Zozulya (r).	Baseball above the Arctic Circle.