Тезисы международной конференции

Рудный потенциал щелочного, кимберлитового

 и карбонатитового магматизма

Abstracts of International conference

Ore potential of alkaline, kimberlite

and carbonatite magmatism

Mineral association of alkaline metasomatic rocks and carbonatites of Gremyakha Vyrmes massif, the Kola Peninsula.
Shpachenko A.K.*, Sorokhtina N.V.**, Zakharov D.O.***

* GI KSC RAS, Apatity, Russia; ** Vernadsky Institute, Moscow, Russia; *** MGRI-RSGPU, Moscow, Russia

            Proterozoic alkaline ultramafic massif Gremyakha-Vyrmes consists of different rock complexes: 1) ultramafic-mafic rocks 2) foidolites 3) alkali granites and syenogranites [Polkanov et al., 1967]. Interpretation of sequence is complicated because of late tectonic and metamorphic processes that are occurred here intensive. Alkaline complex rocks and carbonatites replaced protolite whose interpretation is incomplete still. In this case it is important to explore their mineral composition and sequence of crystallization of phases in appropriate degree. Particularly it is valuable due to rare-metal mineralization occurs in the complex [Sorokhtina et al, 2010]. The rare-metal metasomatic rocks occur as submeridionally orientated zones extending up to 6-8 km and have several hundred meters thickness. They exist in form of plate and lenticular bodies in varying degrees of altered ore (ilmenite) pyroxenites and foidolite, syenogranites.

Basically, alkaline metasomatic rocks are albitites, aegirinite. Their composition varies a lot depending on the protolith composition range. We believe that due to hard tectonics especially tectonic blocks shifting different complexes of  rocks were involved in metasomatic processes. The rocks that were altered are: 1. ore pyroxenites ultrabasite-mafic complex, 2. microcline syenites, alkali granites complex syenogranites 3. urtites, foyaites and nepheline-aegirine pegmatite foidolite complex.
            Despite large range of minerals in rocks the main constituents are albite, aegirine, phlogopite-annite series, microcline, accessories are calcite, sulfides, graphite, pyrochlore group, zircon. Rarely in albitized microcline syenites quartz and fluorite could be found. Sometimes in the aegirine-albite metasomatic rocks arfvedsonite and biotite replace aegirine and titanite replaces ilmenite. In thin sections calcite occurs as rare grains and aggregates, small veins. In this case we suppose that the protolith was a basic rock (Fig. 1a). Also there are nepheline relicts replaced by cancrinite, natrolite, prehnite and secondary mica aggregate.

            Calcite carbonatites occur as concordant and semi-concordant viens in the metasomatic rocks. The veins are few tens of centimeters thick. Rock has a fine-grained and medium grained texture. Uneven distribution of carbonatite veins was discovered during the drilling. Under microscope carbonatites have a hypidiomorphic texture and contains 80-90%vol. of calcite (Fig. 1b). The texture of calcite aggregate is homoblastic. Signs of strain effects on the whole rock have not been identified. Apatite, aegirine, phlogopite-annite minerals, albite, microcline are also found here. Titanite, ilmenite, prehnite, graphite, pyrite, ferrialanite-(Ce), serpentine occur here in less quantity.

Calcite forms polyhedral well-shaped crystals, without traces of corrosion, the faces of adjacent grains are often found at an angle of 120 º. Twins are very common in the calcite and shown in form of flat parallel bands or rhomb system. Sometimes curved cleavage cracks and fine-grained aggregates of calcite are found here. Apparently this could be a result of later deformations. Graphite forms microspherulites aggregates in carbonate or tabular crystals in albitite matrix Mineral is also found as inclusions or intergrowth with pyrochlore, zircon, biotite. Aegirine occurs in single elongated prismatic crystals (1-2 mm on average) in calcite matrix; sometimes twins are shown here. Small cracks inside the crystals contain calcite, sulfides and fibrous silicate mineral which is less common. The common mica constituent is a phlogopite-annite series. Mineral forms a large (up to 1.8 mm) tabular crystals that are intergrown with albite and are often bent and has split edge areas that are replaced by chlorite group minerals. Albite and calcite occur along cleavage fractures in phlogopite. Albite forms large relic poikiloblasts  up to 3 mm, with a characteristic albite twinning. The twins are dislocated, separate blocks of crystals are shifted here. Aegirine, mica, calcite, sulfides, and graphite are found here as the inclusions in poikiloblast. Orthoclase usually forms xenomorphic relict grains. The size varies up to 1.5mm. Distribution of potash feldpar in calcite matrix is extremely uneven. The inclusions of calcite, albite, and zeolites are identified in relict crystals of potassium feldspar. Fluorapatite occurs in the calcite matrix in the form of a large (up to 1.5 mm) elongate-prismatic crystals with smooth outlines and strong fracturing, inclusion of calcite also develops in cracks. In thin sections fluorapatite crystals are oriented in one direction. Titanite forms large metacrystals several centimeters long as well as in albitites. Almost all minerals of carbonatite are established as inclusions in titanite crystals. Sulfides such as pyrrhotite and chalcopyrite form small flattened grains and aggregates which develop in the interstices of calcite.
            Proceedings of the petrographic study of thin sections allow us to conclude that formed metasomatites were involved in carbonatization process intensively and microcline, aegirine, phlogopite-annite, ilmenite, titanite were saved here as a relicts. Fluorapatite and graphite are syngenetic to calcite, other accesory minerals formed on final stages of crystallization.

Generally, alkaline metasomatic rocks could be classified as fenites-nepheline type of metasomatism [Zharikov et al, 1998]. The process described as apomagmatic without regard to the granite or gneisses and the composition of paragenetic association varies depending on what kind of the block was involved in metasomatism. The process appeared on the final stage of foidolite intrusion and was formed by residual alkaline-carbonate fluid. Rocks of foidolite group and associated with them syenogranites, hyperbasic rocks were involved in process of metasomatic alteration. That caused forming of different and complicated mineral associations and several generations of forming minerals such as microcline, albite, aegirine, micas.

REFERENCES

Zharikov V.А., Rusinov V.L., Marakushev А.А., Zaraisky G.P., Omelianenko B.I., Percev N.N., Rass I.T., Andreeva O.V., Abramov C.C., Podlesskii K.V. Metasomatism and metasomatic rocks / М.: Nauchnii mir, 1998. 492 p.

Polkanov A.A., Eliseev N.A., Eliseev N.E., Kavardin G.I. Massif Gremyakha-Virmes, Kola peninsula. М., Nauka, 1967. p.236.

Sorokhtina N.V., Kogarko L.N., Shpachenko A.K. New geochemical and mineralogical data about rare-element occurrence on Gremyakha-Virmes massif // Docladi RAN. 2010. Т. 434. № 2. p. 243–247.