Dissolved inorganic source

Table II summarizes analytical data for dissolved inorganic matter in a number of natural water sources (J3, 9, J 9, 20, 21). Because of the interaction of rainwater with soil and surface minerals, waters in lakes, rivers and shallow wells (<50m) are quite different and vary considerably from one location to another. Nevertheless, the table gives a useful picture of how the composition of natural water changes in the sequence rain ->- surface water deep bedrock water in a granitic environment. Changes with depth may be considerable as illustrated by the Stripa mine studies (22) and other recent surveys (23). Typical changes are an increase in pH and decrease in total carbonate (coupled), a decrease in 02 and Eh (coupled), and an increase in dissolved inorganic constituents. The total salt concentration can vary by a factor of 10-100 with depth in the same borehole as a consequence of the presence of strata with relict sea water. Pockets with such water seem to be common in Scandinavian granite at >100 m depth.

Soil solution is the aqueous phase of soil. It is in the pore space of soils and includes soil water and soluble constituents, such as dissolved inorganic ions and dissolved organic solutes. Soil solution accommodates and nourishes many surface and solution reactions and soil processes, such as soil formation and decomposition of organic matter. Soil solution provides the source and a channel for movement and transport of nutrients and trace elements and regulates their bioavailability in soils to plants. Trace element uptake by organisms and transport in natural systems typically occurs through the solution phase (Traina and Laperche, 1999). 

Effect of temperature, pressure, and salinity on speciation of the dissolved inorganic carbon for 2co2 = 2mmol/kg. Source After Zeebe, R.E. and D. Wolf-Gladrow (2001) Elsevier Oceanography... 

Station ALOHA (see Figure 23.4 for location information). Three-point running mean observations of N/P molar ratios in (a) total dissolved inorganic plus organic pool, (b) total suspended particulate matter in the upper 0-100 m, (c) in exported particulate matter at 150 m depth, and (d) cycling in nutrient limitation (described in text). Source From Karl, D. M. (2002). Trends in Microbiology 10(9), 410-418. 

Surface water concentrations of (a) total alkalinity ( ji,mol/kg) and (b) dissolved inorganic carbon (ljumol/kg). Source After Key, R. M., et al. (2004). Global Blogeochemical Cycles 18, GB3011. (See companion website for color version.)... 

Figure 9.1 Freshwater-marine mixing ratios of dissolved inorganic carbon (DIC) and isotopic composition (DI13C) across three different salinity gradients. Bottom isotopic change between — 10%e at the freshwater end-member, and +2%c at the marine end-member, both end-member values are based on concentration-weighted averages (data sources Spiker and Schemel, 1979 Spiker, 1980). (Modified from Fry, 2002.)...

Isotopic mixing models models used to evaluate sources of dissolved inorganic nutrients (C, N, S) and organic matter (POM and DOM). 

Cai, W.J., Wiebe, W.J., Wang, Y., and Sheldon, J.E. (2000) Intertidal marsh as a source of dissolved inorganic carbon and a sink of nitrate in the Satilla River estuarine complex in the southeastern U.S. Lirnnol. Oceanogr. 45, 1743-1752. 

Haertel-Borer, S. S., AUen, D. M., and Dame, R. F. (2004). Fishes and shrimps are significant sources of dissolved inorganic nutrients in the intertidal salt marsh creeks. J Exp. Mar. Biol. Ecol. 311, 79—99. 

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