Origin of saline fluids in sedimentary basins

Abstract

Subsurface saline waters in sedimentary basins can be divided into three groups based on their anionic composition and salinity: (1) Waters with anions other than Cl dominant. These include Na-HCO 3 and Na-acetate waters. Most such waters have salinities of less than 10 000 mg 1 −1 ; (2) Cl-dominated, halite-undersaturated waters having salinities between 10 000 and 250 000–300 000 mg l −1 . These include Na-Cl waters and, at higher salinities, Na-Ca-Cl waters; (3) Cl-dominated, halite-saturated waters with salinities typically in excess of 300 000 mg 1 −1 . Ca and K become increasingly dominant and Na decreases with increasing salinity. Subaerial evaporation of marine and continental waters and the subsurface dissolution of evaporites both have the potential for producing the range of salinities and dissolved chloride concentrations observed for most subsurface brines, but not their major cation compositions. The broad systematic increase in dissolved Na, K, Mg, Ca, and Sr and decrease in pH and alkalinity with increasing salinity support the hypothesis that the approach toward thermodynamic buffering by silicate-carbonate ± (halide) mineral assemblages is a first-order control on subsurface fluid compositions, even at temperatures well below 100°C. The chemical potential of chloride or, alternatively, the aqueous concentration of anionic charge, is a master variable which ranks in importance with such other variables as pressure and temperature in driving fluid-rock exchange and controlling bulk fluid compositions. This variable is in turn controlled largely by physical processes of fluid advection and dispersion. Dissolved organic acid anions are associated primarily with low salinity waters, but dissolved metals, such as Cu, Pb, and Zn are preferentially found in brines having salinities in excess of 200 g 1 −1 . The high chloride concentration and low pH of these saline waters may enhance solubilization of metals through chloride complexing.

Origin and evolution of oilfield brines from Tertiary strata in western Qaidam Basin: Constraints from 87Sr/86Sr, δD, δ18O, δ34S and water chemistry

“…Fisher and Boles (1990) also reported that hydrocarbon-water interaction can cause light δD. Hanor (1994) reported that sulfate reduction can produce H 2 S gas, then H 2 S+O 2 =SO 2 +2H + . These H + can accelerate water-rock interaction and result in positive shift in δ 18 O.…”

Fluids in the Continental Crust

“…The first issue is the extent to which fluid compositions reflect chemical equilibrium as opposed to responding only to the fastest reacting phases. Looked at from the perspective of newly deposited sediments, it is clear that early diagenetic changes will be dictated to a significant degree by kinetics (Coleman et al, 1985), but when the chemical composition of mature formation waters has been evaluated, there is equally good evidence that it is in equilibrium with the host minerals (Hanor, 1994). These chemical controls are considered in more detail below.…”

Chaotic thermohaline convection in low-porosity hydrothermal systems

“…rain) while diagenetic, metamorphic and/or magmatic £uid sources lead to high concentrations of dissolved elements (up to saturation level) deeper within the crust, e.g. [10]. Advection of the saline £uids through the rocks has implications for many geological processes, such as heat transport, ore genesis, metasomatism and metamorphic petrology, and including the diagenetic history of sediments in subsiding basins [11^16].…”