Carbonatites are defined as igneous rocks containing more than 50% carbonate minerals. They are divided into four classes: (1) calcic, (2) dolomitic, (3) ferrocarbonatite, and (4) natrocarbonatite. Carbonatites are characteristically associated with ijolites, but not all carbonatites are entirely magmatic. Many centres show metasomatic replacement features, referred to as fenitization. Most subvolcanic and volcanic carbonatite centres are calcic, but trapped fluids as inclusions in apatite crystals indicate that the bulk composition was alkalic and chemically comparable to natrocarbonatite. Experimental evidence suggests that parental carbonatite magma is the product of immiscibility from an alkali silicate liquid of phonolitic or nephelinitic composition. Alkali loss from the bulk carbonatite magma caused fenitization represented by zones of sodic and potassic metasomatism. Sodic metasomatism is more frequently located at deeper eroded centres and is characterized by the occurrence of albitite. Potassic metasomatism is more common in many carbonatite centres and is represented mineralogically by alkali feldspar and phlogopite. Many fenites carry an alkaline ferromagnesian assemblage consisting principally of alkali amphibole (eckermannite-magnesioarfvedsonite) and/or aegirine. Carbonatites have igneous isotopic ratios and distinctive contents of incompatible trace elements. Associated fenites have elevated Sr isotopic ratios and selected TE enrichment pertinent to the dominant metasomatism. Carbonatites exhibit REE, Nb, U, Th mineralization and, more rarely, sphalerite, galena, and chalcopyrite mineralization. Both disseminated and vein-controlled mineralization are found in many carbonatite centres. The most important economic products of carbonatites include pyrochore, columbite, monozite, apatite and zirconium minerals. The alkaline syenites and alkaline granites as ring complexes have textural, petrological and chemical characteristics which are distinctly different from I and S type granitoids. The characteristics of A-type granites are dominated by the separation of an (immiscible?) fluid phase which caused limited sodic and potassic metasomatism. Greisenization by acid metasomatism has played a critical role in several anorogenic provinces producing important UNb, ZnSn mineralization. In the fayalite granites, ferrohedenbergite breaks down to sodic-calcic amphibole as iron-rich olivine is destabilized under the influence of the fluid phase. Facies with aegirine and arfvedsonite can develop to give peralkaline granites. Relative loss of the peralkaline fluid phase results in the development of peraluminous biotite granites. The most significant chemical feature of anorogenic granites is that slight differences in the proportions of Na, K and Al can produce striking changes in the mineralogy of the A-type suite. The most characteristic feature of peralkaline granites is the anomalous enrichment in Zr, Zn, Nb, Y, Th, U, LREE, HREE, coupled with high Rb/Sr ratios. Some of these features are found in biotite granites but with dramatically less Zr, Hf, Nb and HREE. The primary mantle origin of syenitic magmas parental to intraplate alkalien granites is well established from isotope studies. The role of the continental crust is implemented by elevated initial 87Sr/ 86Sr ratios. The lower crust in Africa is thought to be lower Proterozoic in age from NdSrPb isotopic data. Fenitization is not only associated with carbonatite centres but also to a limited extent with alkaline granites. The evolution and separation of a peralkaline fluid phase from A-type granites has been experimentally demonstrated, and can be recorded by distinctive suites of subsolidus minerals and specific geochemical changes. From the mineralization viewpoint there are many parallels with the carbonatites, particularly with the abundance of sphalerite, rare-earth minerals, zircon and complex titanium-zirconyl silicates, uranium and thorium, columbite and pyrochlore. Such a distinctive alkaline mineralization suite, possibly related to an alkali carbonate fluid phase, is superimposed on a more normal, less alkaline group of ore minerals such as cassiterite, wolframite, chalcopyrite, and galena.
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