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Volcanism mass balance

The flow of hydrothermal solutions iato the oceans from hydrothermal vents, ie, springs coming from the sea floor ia areas of active volcanism, and the chemical reactions occurring there by high temperature alteration of basalts ate of significance ia the mass balance of and. Eurthermore,... [Pg.216]

Bulk rock chemistry of hydrothermally altered midoceanic ridge basalt has been well studied and used to estimate the geochemical mass balances of oceans today (Wolery and Sleep, 1976 Humphris and Thompson, 1978 Mottl, 1983). In contrast, very few analytical data on hydrothermally altered volcanic rocks that recently erupted at back-arc basins are available. However, a large number of analytical data have been accumulated on the hydrothermally altered Miocene volcanic rocks from the Green tuff region in the Japanese Islands which are inferred to have erupted in a back-arc tectonic setting (section 1.5.3). [Pg.407]

Elucidation of the origin of sulfur in volcanic systems is complicated by the fact that next to SO2, significant amounts of H2S, sulfate and elemental sulfur can also be present. The bulk sulfur isotope composition must be calculated using mass balance constraints. The principal sulfur gas in equilibrium with basaltic melts at low pressure and high temperature is SO2. With decreasing temperature and/or increasing... [Pg.122]

Von Damm and Edmond (1984) utilized the lakes of the Ethiopian and northern Kenya rift zones to examine reverse weathering (the formation of authigenic clay minerals), because here evaporative concentration had not proceeded to the extent that salt precipitation interfered with a mass balance approach. They found that —60% of an alkalinity deficit could be accounted for by processes other than carbonate precipitation, and concluded that solute magnesium was lost as rapidly to clay as solute calcium was to carbonate. This situation, particularly in volcanic terrain, was also initially recognized at saline Lake Abert, Oregon, by Jones and VanDenburgh (1966). [Pg.2658]

Input is balanced by output in a steady-state system. The concentration of an element in seawater remains constant if it is added to the sea at the same rate that it is removed from the ocean water by sedimentation. Input into the oceans consists primarily of (1) dissolved and particulate matter carried by streams, (2) volcanic hot spring and basalt material introduced directly, and (3) atmospheric inputs. Often the latter two processes can be neglected in the mass balance. Output is primarily by sedimentation occasionally, emission into the atmosphere may have to be considered. Note that the system considered is a single box model of the sea, that is, an ocean of constant volume, constant temperature and pressure, and uniform composition. [Pg.897]

There are, however, two main reasons why this must be a minimum estimate of the amount of sediment recycled into the mantle over geological time. These are, first, reintroduction of CO2 into the atmosphere via arc volcanism, and second, the fact that purely clastic sediments are ignored in this mass balance. CO2 is reintroduced into the atmosphere as a result of decarbona-tion reactions in calc-silicate rocks (the reverse Urey reaction ), requiring further weathering and photosynthesis to remove it. Fluxes associated with these processes over Phanerozoic time have been reviewed by Berner et al. (1983) and Berner (1991), who concluded that such addition of CO2 by (mainly arc) volcanism and its drawdown by silicate weathering have been the major long-term fluxes over this period, and that drawdown has only slightly outstripped... [Pg.261]

Crust-mantle chemical mass-balance models offer important constraints on compositional variations in the mantle, but their constraints on the size of the various reservoirs involved depend critically on uncertainties in the estimates of the bulk composition of the continental crust, the degree of depletion of the complementary depleted mantle, and the existence of enriched reservoirs in Earth s interior, for example, possibly significant volumes of subducted oceanic crust. This last item was left out of the mass-balance models that suggested that the upper and lower mantle are chemically distinct. Chapter 2.03 makes it clear that much of the chemical and isotopic heterogeneity observed in oceanic volcanic rocks reflects various mixtures of depleted mantle with different types of recycled subducted crust. With this realization, and excepting the noble gas evidence for undegassed mantle, some of the characteristics of what was once labeled... [Pg.604]

The data presented above can be used to set some limits on C02 levels over geological time. The 2.75 Ga paleosol evidence sets an upper limit of 0.04 bars on COa levels whereas the weathering rind study of Hassler et al. (2004) may set a lower limit of 0.0025 bars for 3.2 Ga. Calculations by Mel nik (1982) show that C02 levels were not greater than 0.1-0.15 bars, for otherwise BIFs would be present as iron carbonates rather than oxides. The nahco-lite study of Lowe and Tice (2004) lies within this range, although this result must be regarded as a maximum, as does the estimate of Zahnle and Sleep (2002) based purely on a mass balance between volcanic COa and subducted, carbonated ocean crust (Fig. 5.15). [Pg.205]

Similarly, the amount of volcanically emitted C02 needed to account for the isotopic excursion, which can be estimated by mass balance, is without precedence. For a transient input of carbon (x) we can write (Dickens et al. 1995) ... [Pg.283]

Hydrodynamic dispersion may however be significant in small, local hydrogeological problems, such as a point source contamination (Plummer et al., 1992). Another instance where diffusion may play an important role in water chemistry is the diffusion from permeable to less permeable parts of the aquifer, or matrix diffusion. This process appears to be important in fractured aquifers (Maloszewski and Zuber, 1991 Neretnieks, 1981), volcanic rock aquifers, aquifers adjacent to confining units (Sudicky and Frind, 1981), and sand layers inter-stratified with confining clay layers (Sanford, 1997). In systems in which a chemical steady state (see below) has not been reached, matrix diffusion effects may severely limit the applicability of inverse mass balance modeling to those systems. [Pg.181]

Volatile flux estimates derived in the previous section, both for arcs individually as well as arc-related volcanism globally, make no distinction as to the source or provenance of the volatiles. However, in order to assess the chemical mass balance between output at arcs and input associated with the subducting slab, the total arc output flux must be resolved into its component structures. In this way, the fraction of the total output that is derived from the subducted slab can be quantified and compared with estimates of the input parameter. As we show in this section, helium has proven remarkably sensitive in discerning volatile provenance. We use CO2 and N2 to illustrate the case. [Pg.349]

In addition to supplying volatiles that are lost via arc-related volcanism, the subducting slab may also contribute volatiles to both the back-arc and fore-arc regions. To complete a realistic mass balance for subduction zones, therefore, it is essential to quantify volatile fluxes at the back-arc and fore-arc. As we discuss below, both fluxes are severely underconstrained at present. [Pg.352]

The input fluxes of various volatile species (Table 10) can now be compared to various output fluxes through arc volcanism (Table 9) to assess the extent of volatile mass balance. At this stage, we ignore possible volatile losses at the back-arc given the large uncertainty in actual values. Also, we note that in the case of subducted carbon, it is important to distinguish between reduced sedimentary carbon, sedimentary carbonate and carbonate of the altered oceanic crust. [Pg.354]


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See also in sourсe #XX -- [ Pg.298 ]




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