BURIAL DIAGENESIS AND PORE-FLUID EVOLUTION IN A MESOZOIC BACK-ARC BASIN - THE MARAMBIO GROUP, VEGA ISLAND, ANTARCTICA

UPPer Cretaceous shallow-marine sediments from Vega Island, Antarctica , contain five major authigenic phases; glauconite, pyrite, a zeolite mineral of the clinoptilolite-heulandite group, chlorite, and calcite. The framework sediment composition changes from quartzose at the base of the measured succession to volcaniclastic at the top. The petroene sis of individual samples reflects the local controls on diagenesis of depositional environment and sediment composition, combined with the effects of burial to no more than 1 km. Calcite cements are the most a bundant precipitates. Marine carbonate cements include acicular and ot her fringing cements that commonly are present within bioclasts. Early -burial micritic to sparry calcite cements include both concretionary and nonconcretionary forms. Burial calcites occlude residual porosity, replace detrital grains and form veins with fibrous and cone-in-cone textures. The stable-isotope composition of the carbonate cements is v ery variable, with deltaO-18 ranging from 0.60 parts per thousand to - 19.93 parts per thousand PDB and deltaC-13 of -133 parts per thousand to -28.09 parts per thousand. PDB. The stable-isotope data reflect the initial conditions of mineral precipitation in oxic and anoxic marine pore waters, together with the effects of subsequent fluid/rock inter action through both recrystallization and cementation. The latest prec ipitates, thought to have been formed during over pressuring, define a vertical field for burial calcite on an isotope cross plot, suggestin g that late fluids responsible for cementation and alteration of earli er precipitates had negative deltaO-18 and contained carbon with varia ble deltaC-13. The oxygen values are compatible with either influx of high-latitude meteoric water or intense fluid-rock interaction with re active volcanic detritus, or a combination of the two processes. The v ery variable carbon signatures probably reflect dissolution of bioclas ts and earlier diagenetic precipitates. Only by identifying possible e nd-member compositions for both early and late diagenetic precipitates can most of the isotopic data be interpreted correctly.