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• W2493552004 abstract "Secondary carbonate minerals were recovered within the basalts at both ODP Sites 768 and 770 in the Sulu and Celebes seas. Petrographic and X-ray diffraction analyses indicate that the carbonates are calcites. Other alteration products recognized in the thin sections are smectites, iron oxides, and gypsum. The C values of carbonates from both sites range from 1.6 %o to 2.3 %o, which are indicative of inorganic carbonate formation with no contributions from C-depleted sources such as oxidized organic carbon or methane. The oxygen isotopes at Site 770 range from 30.8%e to 31.6%c, which indicates a pervasive circulation of cold seawater (9° to 12°C) during alteration of the Celebes Sea basalts. In contrast, carbonates associated with Site 768 basalts have less positive δ 1 8 θ values (21.0 %c to 27.3 ‰). A lighter O isotopic signature indicates the formation of secondary calcite at either higher temperatures or in a system closed to seawater. The rapidly deposited pyroclastic flows at Site 768 would have limited water access to the crust very soon after its formation, which leads us to speculate that the carbonates in the Sulu Sea basalts were formed by isotopically modified fluids resulting from basalt alteration in a closed system. INTRODUCTION In the last decade, geochemical assessments of the heat loss from the oceanic crust has reinforced the view that large-scale mass transport through the crust is required to explain the large water/rock ratios inferred from chemical water-rock interactions (Sclater et al., 1976; Anderson and Hobart, 1976) The analysis of vein-filling material in drilled basalts have led to a good understanding of the basaltseawater, post-deutiric alteration reactions. These studies have shown that such interactions have taken place to at least 500 m depth in the oceanic crust, and are at least in part controlled by the availability of fluid circulation through the crust. Such factors as the rate of sediment accumulation and the nature of the basalt (i.e., massive flow vs. pillow lavas), play a crucial role in controlling access of seawater to the oceanic crust. Effective water/rock ratio and extent of exchange between circulating seawater and young crust, influence the rate of heat loss and the chemical evolution of both fluid and rock (Staudigel and Hart, 1983). The timing, duration, and chemical evolution of hydrothermal solutions have been fairly well established for oceanic crust generated at slow spreading ridges in the Atlantic. Based on the Sr/Sr ratios in smectites, celadonites, analcites, and carbonates in the vein materials from drill holes ranging in age from 3.5 to 110 m.y. and the known variation of the ^Sr/^Sr with time, Hart and Staudigel (1978) and Richardson et al. (1980) have concluded that most reactions in the crust take place over a fairly short time. They have suggested four major low-temperature alteration stages that are thought to occur in characteristic temperature succession: Stage 1: formation of palagonites, Stage 2: formation of smectites, Stage 3: formation of carbonates, and Stage 4: compaction and dehydration of the crust. 1 Silver, E. A., Rangin, C , von Breymann, M. T., et al., 1991. Proc. ODP, Sci. Results, 124: College Station, TX (Ocean Drilling Program). 2 Ocean Drilling Program, Texas A&M University, 1000 Discovery Drive, College Station, TX 77845. 3 Bundesanstalt fur Geowissenschaften und Rohstoffe, Stillweg 2, 3000 Hannover 51, Federal Republic of Germany. Drilling and recovery of basaltic crust from both the Atlantic and Pacific oceans has provided new insights into the timing and duration of crustal alteration, and the chemical evolution of hydrothermal solutions. Two basic types have been described: seawater-dominated and rock-dominated systems. The abundance of massive flows and the thin sediment cover in fast-spreading centers are thought to result in high formation permeabilities and seawater-dominated hydrothermal solutions. Oxygen isotope data on the calcite veins at DSDP Site 597 in the Pacific Ocean reflect a low temperature of alteration, and the Sr/Sr isotopic ratios and the Sr/Ca ratio of vein carbonates imply that the hydrothermal solutions at this site were not significantly altered from the interaction with the basalts (Staudigel et al., 1986). On the other end of the spectrum, Hole 504B provides the first evidence that vein carbonates can in fact be deposited from solutions which are markedly different from ambient seawater. Based on Sr and Sr/Sr data for carbonates from DSDP Hole 504B, Staudigel and Hart (1983) conclude that carbonate precipitattion occurred in a basalt-dominated, hightemperature system, where rapidly depositing sediments have sealed the crust form exchange with the overlying water column. Staudigel and Hart (1985) suggest that the calcium necessary for the precipitation of carbonates in DSDP Hole 504B must be derived from the alteration of basaltic glass and the breakdown of anorthic feldspar. Complex basalt alteration reactions and precipitation of secondary phases from fluids isolated from the overlying water column result in an hydrothermal solution that differ significantly from the composition of the original seawater. To evaluate conditions of crustal alteration in two western Pacific basins, we have analyzed secondary vein carbonates of basalts from the Sulu and Celebes seas. Basement rocks from these two sites appear to have been formed in different tectonic settings and at different times. The Sulu Sea originated as a back-arc or intra-arc basin in the late early to early middle Miocene, the Celebes Sea originated in an open ocean setting in the middle Eocene (Rangin, Silver, von Breymann et al., 1990). Structural differences resulting from mechanisms of crust emplacement will have an effect on the amount of water flow. The" @default.
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• W2493552004 date "1991-09-01" @default.
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• W2493552004 title "Isotopic Characterization of Secondary Carbonates from Sulu and Celebes Sea Basalts: Contrasting Scenarios of Basalt-Seawater Interaction" @default.
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• W2493552004 doi "https://doi.org/10.2973/odp.proc.sr.124.174.1991" @default.
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