Samples were taken from Hole 1134A at a rate of one sample per core over the upper 15 cores, and every other core thereafter (recovery permitting). Samples were analyzed according to the procedures outlined in "Inorganic Geochemistry" in the "Explanatory Notes" chapter. These data are presented in Table T7 and Figures F12, F13, and F14.
Salinity shows a rapid increase at Site 1134, rising to 97 at a depth of 65.9 mbsf (Fig. F12). The rate of increase in salinity is significantly greater than at the shallow-water sites and is similar to Sites 1126 and 1130. Concentrations of Na+ and K+ are conservative with respect to Cl-, and Na+/Cl- values are relatively constant throughout the cored interval. Between 304.5 and 352 mbsf, the concentrations of Cl-, Na+, and K+ decline slightly. Whether this decrease is real and may therefore indicate the limits of the saline brine observed at this and other sites, or whether it is the result of contamination by seawater, is not known.
The concentrations of Mg2+ and Ca2+ increase with depth associated with the change in salinity. The concentration of Mg2+ rises to ~120 mM between 46.9 and 206.1 mbsf (Fig. F13). Toward the bottom of the cored interval, the concentration of Mg2+ decreases slightly to 110.3 mM. Although Mg2+ concentration increases with depth, the concentration normalized to Cl- actually decreases, reaching a maximum depletion of 13 mM at 46.9 mbsf. The decrease in Mg2+ is possibly associated with the formation of dolomite, which is present throughout the upper 40 mbsf (Table T8, also in ASCII format). In contrast, the normalized concentration of Ca2+ increases by 6 mM over the same interval, indicating a net dissolution of carbonate. Recrystallization is also evident in the concentration of Sr2+ in the pore fluids, which rises rapidly to 364 µM at 37.4 mbsf. However, below this depth, the concentration decreases to 243 µM and subsequently declines more slowly to the bottom of the cored interval. The concentration of Li+ increases slightly relative to Cl-, associated with the recrystallization of calcium carbonate (Fig. F13).
The extent of organic reactions at Site 1134 are minimal compared to many of the other sites drilled during Leg 182. Alkalinity reached a maximum of 4.21 mM at 27.9 mbsf, slightly deeper than (1) the maximum in the concentration of dissolved Sr2+, (2) the maximum depletion in the normalized concentration of SO42- (4 mM), and (3) the highest concentration of NH4+ (Table T7; Fig. F14). The lack of sulfate depletion and the high alkalinity probably result from the relative absence of organic material caused both by oxidation of the organic material before burial and by the low rate of sedimentation at this site (see "Biostratigraphy"). The absence of H2S, combined with a pH slightly lower than seawater, makes Fe2+ more soluble in interstitial waters than in normal marine fluids. As a consequence, the concentration of Fe2+ is higher than that observed at other H2S-rich sites cored during Leg 182, exceeding values of 80 µM (Fig. F14).
The sediments at Site 1134 are composed of low-Mg calcite (LMC), high-Mg calcite (HMC), quartz, aragonite, and dolomite (Table T8). In the uppermost portion of Site 1134, the sediments are composed of aragonite, HMC, LMC, quartz, and dolomite. However, HMC rapidly disappears with increasing depth, and aragonite vanishes coincident with the boundary between the middle and upper Miocene (see "Biostratigraphy"). Below 55.6 mbsf, the sediments appear to contain only LMC and a small amount of quartz, together with 5% and 10% insoluble material (see "Organic Geochemistry"). A small amount of aragonite accompanied by high concentrations of quartz was detected between 167.2 and 189.1 mbsf in sediments of middle Miocene age (see "Lithostratigraphy").