Major- and trace-element chemistry of DSDP Leg 70 Holes basalts and their alteration products

Major and trace element compositions of basalts from the lower part of Hole 504B indicate their cogenetic nature. The cored sequence of interlayered pillow lavas and massive lava flows was produced by eruption of lavas, slightly variable in composition. Plagioclase and olivine crystallization in a shallow magma chamber, followed by small-scale fractionation at higher levels, is responsible for these variations. Except in highly fractured zones within the basement, there are systematic variations in the style and degree of rock alteration with depth. Trace element characteristics of altered rocks and secondary minerals indicate that progressive changes in sea water composition occurred as it reacted with basaltic crust.

Carbon chemistry of ODP Leg 105 sites

The quantity and quality of organic carbon of Eocene to Holocene sediments from ODP Sites 645, 646, and 647 were investigated to reconstruct depositional environments. Results were based on organic-carbon and nitrogen determinations, Rock-Eval pyrolysis, and kerogen microscopy. The sediments at Site 645 in Baffin Bay are characterized by relatively high organic-carbon values, most of which range from 0.5% to almost 3%, with maximum values in the middle Miocene. Distinct maxima of organic-carbon accumulation rates occur between 18 and 12.5 Ma and between 3.4 and 0 Ma. At Sites 646 and 647 in the Labrador Sea, organic-carbon contents vary between 0.1% and 0.75%. Cyclic 'Milankovitch-type' changes in organic-carbon deposition imply climate-controlled mechanisms that cause these fluctuations. The composition of organic matter at Site 645 is dominated by terrigenous components throughout the entire sediment sequence. An increased content of marine organic carbon was recorded only in the late-middle Miocene. At Sites 646 and 647, the origin of the organic matter most probably is marine. Oceanic paleoproductivity values were estimated, based on the amount of marine organic carbon. During most of the Neogene time interval at Site 645, productivity was low, i.e., similar or less than that measured in Baffin Bay today. Higher values of up to 150 (200) gC/m**2/y may have occurred only in the Miocene. At Sites 646 and 647, mean paleoproductivity values vary between 90 and 170 gC/m**2/y; i.e., these are also similar to those measured in the Labrador Sea today. Lower values of 40 to 70 gC/m**2/y were estimated for the early Eocene and (middle) Miocene.

Chemistry of pore water and solids, formation factors and salt-corrected porosities of DSDP Site 68-503

Recent discoveries relating to the circulation of fluids within the oceanic crust include the finding of both important fluxes of elements and isotopes into the oceans by ridge-crest hydrothermal convection and important fluxes of heat out of the oceanic crust by convection at ridge crests and at some distance from ridge crests. In the present chapter, I present isotopic, chemical, and physical data from sediments and pore waters of Deep Sea Drilling Project (DSDP) Holes 503A and 503B. These results are modeled in terms of pore-water diffusion, advection, and production to ascertain the relative contribution of these processes at this location, 7.5 m.y. removed from ridge-crest hydrothermal activity. The observations made here contribute to the understanding of chemical and heat transport in oceanic crust of moderate age.

Chemistry of smectite and volcanic glass of ODP Site 159-959

The Ocean Drilling Program (ODP) Site 959 was drilled in the northern border of the Côte d'Ivoire-Ghana Ridge at a water depth of 2100 m. Pleistocene total thickness does not exceed 20 m. Winnowing processes resulted in a low accumulation rate and notable stratigraphic hiatuses. During the Late Pleistocene, bottom circulation was very active and controlled laminae deposition (contourites) which increased the concentration of glauconitic infillings of foraminifera, and of volcanic glass and blue-green grains more rarely, with one or several subordinate ferromagnesian silicates. Volcanic glass generally was X-ray amorphous and schematically classified as basic to intermediate (44-60% SiO2). Opal-A or opal-CT suggested the beginning of the palagonitisation process, and previous smectitic deposits may have been eroded mechanically. The blue-green grains presented two main types of mineralogic composition: (1) neoformed K, Fe-smectite associated with zeolite (like phillipsite) and unequal amounts of quartz and anorthite; (2) feldspathic grains dominated by albite but including quartz, volcanic glass and smectites as accessory components. They were more or less associated with the volcanic glass. On the basis of their chemical composition, the genetic relationship between the blue-green grains and the volcanic glass seemed to be obvious although some heterogeneous grains seemed to be primary ignimbrite and not the result of glass weathering. The most reasonable origin of these pyroclastic ejecta would be explosive events from the Cameroon Volcanic Ridge, especially from the Sao Thome and Principe Islands and Mount Cameroon area. This is supported both by grain geochemistry and the time of volcanic activity, i.e. Pleistocene. After westward wind transport (some 1200 km) and ash fall-out, the subsequent winnowing by bottom currents controlled the concentration of the volcanic grains previously disseminated inside the hemipelagic sediment. Palagonitisation, and especially phillipsite formation, may result from a relatively rapid reaction during burial diagenesis (<1 m.y.), in deep-sea deposits at relatively low sedimentation rate. However, it cannot be excluded that the weathering had begun widely on the Cameroon Ridge before the explosive event.

Water chemistry of lakes from the Antarctic

This paper reviews Japanese limnological studies mainly in the McMurdo and Syowa oases, with special emphasis on the nutrient distribution. Generally, the chemical composition of the major ionic components in the coastal lakes and ponds is similar to that in seawater, while that in inland Dry Valley lakes and ponds of the McMurdo Oasis is abundant in calcium, magnesium and sulfate ions. The former can be explained by the direct influences of sea salts, while the latter is mainly attributable to the accumulation of atmospheric salts. Most saline lakes are meromictic. Dissolved oxygen concentrations in the upper layers are saturated or supersaturated, but the bottom layers are anoxic and often hydrogen sulfide occurs. The concentrations of nutrients vary largely not only among the lakes but also with depth. Silicate-Si, which is generally abundant in all freshwater and saline lakes, may be due to erosions of soils and rocks. Nitrite-N concentrations in both freshwater and saline lakes are generally low. Nitrate-N concentrations in the oxic layers of the inland saline lakes in the McMurdo Oasis arc often high, but not high in the coastal saline lakes of the Syowa and Vestfold oases. The abundance of phosphate-P and ammonium-N in the bottom stagnant layers of saline lakes can be explained by the accumulation of microbially released nutrients due to the decomposition of organic substances. Nutrients are supplied mainly from meltstreams in the catchment areas, and are proved to play an important role in primary production.

Mineral chemistry of basalts at DSDP Leg 55 Holes

Microprobe mineral compositions of olivine, plagioclase, clinopyroxene, chrome spinel, ilmenite, and titanomagnetite are presented for 7 samples from 4 flows of hawaiite and one flow of tholeiitic basalt from Hole 430A at Ojin Seamount, 4 samples from 3 flows of alkalic basalt from Hole 432A at Nintoku Seamount, and 29 samples from 2 flows of alkalic basalt and 24 flows of tholeiitic basalt from Holes 433A, 433B, and 433C at Suiko Seamount. The four hawaiite flows from Hole 430A on Ojin Seamount have nearly identical mineralogy. The plagioclase phenocrysts and calculated equilibrium olivine appear to have crystallized at about 1175°C; the groundmass plagioclase crystallized from about 1135° to 1010°C; and the Fe-Ti oxides equilibrated at temperatures from 1000°C to 720°C under oxygen fugacities of 10**-11 to 10**-17. The single tholeiitic flow contains glomerocrysts of plagioclase (An80 to An65) and clinopyroxene (Wo43En46Fsn to Wo42En45Fs13). The plagioclase phenocrysts give calculated temperatures as high as 1400°C, indicating that they were not equilibrated with a magma having the bulk rock composition. The plagioclase groundmass crystallized at 1120° to 1070°C, and the Fe-Ti oxides equilibrated at 1070° to 930°C under oxygen fugacities of 10**-10 to 10**-12. Using mineral compositions of Hawaiian basalts as a guide, we infer that the hawaiite flows were erupted during the post-caldera alkalic eruptive stage and the tholeiite was erupted during the shield-building or caldera collapse stage. The three alkalic basalt flows from Hole 432A on Nintoku Seamount have similar mineralogy, although Flow Units 1 and 2 contain much more abundant plagioclase phenocrysts. The groundmass plagioclase crystallized at temperatures between 1175° and 1000°C. The olivine and plagioclase phenocrysts do not appear to be in equilibrium with the enclosing magmas. The mineral compositions suggest that these samples are intermediate between alkalic basalt and hawaiite; they probably erupted during the post-caldera alkalic stage of eruption. The two analyzed alkalic basalt flows are the two youngest flows recovered at Holes 433A, 433B, and 433C. Flow Unit 1 contains abundant sector-zoned clinopyroxene, and Flow Unit 2 contains rare kink-banded olivine xenocrysts. The plagioclase phenocrysts yield calculated temperatures of 1440° to 1250°C, indicating that they are probably not cognate. Calculated-equilibrium olivine indicates crystallization of olivine at about 1170°C. The Fe-Ti oxides equilibrated at temperatures of 1140° to 870°C under oxygen fugacities of 10**-9 to 10**-14. The groundmass plagioclase crystallized at temperatures of 1178° to 1035 °C. The mineral compositions indicate that these alkalic basalts erupted during the post-caldera alkalic eruptive stage. The 24 analyzed tholeiitic basalts are subdivided on the basis of phenocryst abundances into olivine tholeiites, plagioclase tholeiites, and tholeiites. The crystallization sequence appears to have been chrome spinel, olivine, plagioclase, and clinopyroxene as phenocryst phases, followed by and overlapping with groundmass crystallization of plagioclase (1180° to 920°C), clinopyroxene, and Fe-Ti oxides (1140° to 670°C). At least three flows contain pigeonite. The mineral compositions indicate that all the samples from Flow Unit 4 downward are tholeiitic basalts, although Flow Unit 64 has mineral compositions transitional to those in alkalic basalts.

Carbon chemistry of oceanic crust

Carbonate mineral precipitation in the upper oceanic crust during low-temperature, off-axis, hydrothermal circulation is investigated using new estimates of the bulk CO2 content of seven DSDP/ODP drill cores. In combination with previously published data these new data show: (i) the CO2 content of the upper ~ 300 m of the crust is substantially higher in Cretaceous than in Cenozoic crust and (ii) for any age of crust, there is substantially more CO2 in Atlantic (slow-spreading) than Pacific (intermediate- to fast-spreading) crust. Modelling the Sr-isotopic composition of the carbonates suggests that > 80% of carbonate mineral formation occurs within < 20 Myr of crust formation. This means that the higher CO2 content of Cretaceous crust reflects a secular change in the rate of CO2 uptake by the crust. Oxygen isotope derived estimates of carbonate mineral precipitation temperatures show that the average and minimum temperature of carbonate precipitation was ~10 °C higher temperatures in the Cretaceous than in the Cenozoic. This difference is consistent with previous estimates of secular change in bottom seawater temperature. Higher fluid temperature within the crust will have increased reaction rates potentially liberating more basaltic Ca and hence enhancing carbonate mineral precipitation. Additionally, if crustal fluid pH is controlled by fluid-rock reaction, the higher Ca content of the Cretaceous ocean will also have enhanced carbonate mineral precipitation. New estimates of the rate of CO2 uptake by the upper ocean crust during the Cenozoic are much lower than previous estimates.

Pore-water chemistry of ODP Leg 115 samples

Analyses of the Sr2+ concentrations of interstitial fluids obtained from sediments squeezed during Leg 115 were used to estimate the rates and total amount of recrystallization of biogenic carbonates. The total amount of recrystallization calculated using this method varies from less than 1 % in sediments at Site 706 to more than 40% at Site 709 in sediments of 47 Ma. Five of the sites drilled during Leg 115 (Sites 707 through 711) were drilled in a depth transect within a restricted geographic area so that theoretically they received similar amounts of sediment input. Of these, the maximum rate of recrystallization occurred in the upper 50 m of Site 710 (3812 m). The amount of recrystallization decreased with increasing water depth at Sites 708 (4096 m) and 711 (4428 m), presumably as a result of the fact that most of the reactive calcium carbonate was dissolved before burial. We also observed significant alkalinity deficits at many of these sites, a condition which most likely resulted from the precipitation of calcium carbonate either in the sedimentary column, or during retrieval of the core. Precipitation of CaCO3 as a result of pressure changes during core retrieval was confirmed by the comparison of Ca2+ and alkalinity from water samples obtained using the in-situ sampler and squeezed from the sediments. At Sites 707 and 716, the shallowest sites, no calcium or alkalinity deficits were present. In spite of our estimations of as much as 45% recrystallization at Site 709, all the carbonate sites exhibited what would be previously considered conservative Ca2+/Mg2+ profiles, which varied from -1 to -0.5. By virtue of the position of these sites relative to known basaltic basement or through the actual penetration of basalt (i.e., Sites 706, 707 and 712), these sites are all known to be underlain by basalt. Our results suggest, therefore, that more positive Ca2 + /Mg2+ gradients cannot necessarily be used as indicators of the nature of basement material.