Geology and geochemistry of paleoproterozoic magnesite deposits (-1.8Ga), State of Ceara, Northeastern Brazil

Abstract

Five important magnesite mines and small occurrences in the state of Ceara form a sequence of lenses that extend, discontinuously, for over 140km. The magnesite rocks are hosted by metadolomites with lutecite, sulphate nodules pseudomorphosed by fiber-radiated quartz, scapolite and dissolution breccias. This metacarbonate sequence is more voluminous and more calcic in the southwestern extremity ofthe belt, but less voluminous and more magnesian towards the northeastern portion of the belt, the highest Mg contents being observed in the Alencar-Oros region. Magnesite deposits pass gradually into metadolomites and then to almost pure calcitic marbles westward the belt. This group is hosted in a greenschists to amphibolite-facies metavolcanic-sedimentary sequence crosscut by basic sills and granitic intrusions ofvariable size, form, composition and age (middle to late Proterozoic ~550Ma). Two types of magnesite marble may be distinguished: (I) medium-grained (I to 9mrn) and (2) sparry -magnesite marble (I to 15cm). The latter displays wide textural variation (porphyric, rosette, layered and palisadic types) and exhibits remnants of the original sedimentary features. The sparry crystals, in spite oftheir deformation, are hypidiomorphic and pinolitic. The colors vary from white to light or dark gray, or even red. The dark banded term presents traces ofmicrofossils and stromatolites structures. The medium-grained magnesite marble, on the other hand, shows more homogeneous texture and color and anhedral crystals are more abundant. The sparry-magnesite marble is less enriched in Si02, Fep), Alp) and CaO and richer in MgO than the medium-grained ones. The magnesitic marbles display positive Ce, and negative Eu anomalies. This suggests a shallow marine platform environment with continental, reduced influence (Iagunar). These magnesitic marbles also show positive Ce and Eu anomalies in relation to the present seawater, suggesting compositional differences, materialized mainly by an enrichement of these elements in the past seawater. Fluid inclusions in the medium-grained magnesites ofthe Riacho Fundo deposit are aqueous inclusions, while in the sparry magnesite deposits, particularly in Cabeca de Negro, aquo-carbonic inclusions dominate. Hydrocarbons, however, are found in both cases. The calcitic marble, deposited on open-marine environment, displays positive l3C (+0.5 to 2.1 %0 PDB), while dolomitic to dolostone marbles, deposited on less open marine environment, display negative shift (0.7 to -3.2%0 PDB). This l3C fluctuation is within the range for carbonates deposited around 1.8Ga. The depositional environment ofthese carbonates is close to a paralic system, lagoon, with strong evaporitic conditions. The depressions were of variable depth and lengths and could be isolated, in particular by stromatolitic barriers, dried and flooded by seawater with continental inflows. The largest and deepest ones correspond to the sparry magnesite deposits. These magnesites are located in a lateral way to almost pure calcitic marbles, through dolomitic marbles. This points to a process of chemical differentiation within a paralic system, from open sea to landwards, more calcic in the first to more magnesian in the confined environment, in which lagoon waters are progressively purified from Ca through preferential precipitation of calcic carbonates and secondly of gypsum/anhydrite, which increases the Mg/Ca ratio, and lead carbonate deposits towards the magnesite pole. These metacarbonates also reveal a fractionation ofthe light REE, starting from the calcitic, through the dolomitic to magnesitic marbles. In the calcitic marbles, REE are in association with the clay fraction, while in magnesitic marbles, they seem to be in association with organic and/or soluble complexes. The magnesitic marbles are of sedimentary origin and underwent important diagenetic evolution before being metamorphosed during the Brasiliano orogenic cycle.