Soil carbonate deposition

The equations above describe how solutes in the soil will move in response to concentration or water potential gradients. Such gradients form when the rhizo-sphere is perturbed by the activities of the root including water and MN abstraction and carbon deposition. These activities need to be mathematically described and form one of the two boundary conditions required to solve the initial-value problem. 

Figure 12. Apparent growth temperatures for various Altiplano carbonates based on clumped isotope thermometry, plotted as a function of estimated maximum burial depth. Symbols discriminate among soil carbonates from sections near Callapa, Corque and Salla and lacustrine carbonates from near Tambo Tambillo, as indicated by the legend. The heavy solid line indicates an estimated burial geotherm, assuming a surface temperature of 20 °C and a gradient of 30 °C per km. The dashed lines define a 10° offset from this trend, which we consider a reasonable estimate of its uncertainty. Carbonates deposited within the last 28.5 Ma and buried to 5000 meters or less exhibit no systematic relationship between apparent temperature and burial depth, and show no evidence for pervasive resetting of deeply buried samples. Error bars are la (when not visible, these are approximately the size of the plotted symbol).

Figure 6.5. Changes in soil organic C storage and mineral content along a chronosequence in Hawaii (Torn et al., 1997). The substrate for soil development are basaltic ash deposits of known age. Climate and vegetation are virtually the same across the sites. (A) Soil organic C inventory versus ash substrate age. The solid line is the whole mineral soil to the C horizon, and the dashed line is the top 20 cm. The increase and subsequent decrease in SOM with soil age is mostly due to changes in the subsurface mineral soil. (B) The correlation of soil carbon in mineral horizons with the amount of noncrystalline minerals.

Treseder. K. K. Allen, M. F. (2000). Mycorrhizal fungi have a potential role in soil carbon storage under elevated CO2 and nitrogen deposition. New Phytologist, 147, 189-200. 

One would indeed expect the soil in central Mexico City, which to a great extent is the filled-in bed of Lake Texcoco, to be moist and hence conducive to carbonate deposition and the soil at Teotihuacan, which is... 

Modeling experiments allowed us to control for factors that might cause variation in field-based estimates of woody plant age-SOC relationships. Model estimates of SOC accumulation were comparable to field estimates for upland patch types and substantially lower than field estimates for lowland patch types (Table 4). Model estimates of soil N accumulation were substantially lower than field estimates, especially in lowlands. Given that woody patch age explained only 26-68% of the variance in soil C and N content, our field estimates of accumulation rates cannot be taken as definitive. Model results underestimated field observations, especially for N. Reliability of model estimates of soil carbon could likely be improved with a better understanding of how turnover of the substantial root mass (Table 2) might differ among patch types. Model estimates of soil N are likely constrained by lack of information on inputs associated with N, fixation, atmospheric N deposition, translocation between uplands and lowlands, and root turnover. 

Most of the allochthonous, or foreign, sources represent carbon with lower concentrations ( older radiocarbon ages) than the fraction of TOC originating from phytoplanktonic production. The only exception is the rapid transport and sedimentation of recently synthesized terrestrial plant material, which is in equilibrium with the " C concentration of atmospheric CO2. Other sources of nonmarine carbon typically are of intermediate (lO lO" years) or infinite A C (beyond the detection limit of 50-60 000 years) radiocarbon age, depending on the amount of time spent in other reservoirs such as soils, fluvial deposits, or carbon-rich rocks. 

Fig. 15.8. Simulated change of plant production (a), soil carbon (b), and organic soil phosphorus (c) resulting from altered dust phosphorus deposition rates.

Acrylic acid/sulfonic acid/sodium styrene sulfonate terpolymer sodium salt deposit control agent, soil removal Acrylic acid/suifonic acid/sodium styrene sulfonate terpolymer sodium salt deposit control agent, water treatment Acrylic acid/sulfonic acid/sodium styrene sulfonate terpolymer sodium salt deposit control agent, wet-end paper processes Ammonium zirconium carbonate deposit lime Levulinic acid... 

The harmful effects of air pollutants on human beings have been the major reason for efforts to understand and control their sources. During the past two decades, research on acidic deposition on water-based ecosystems has helped to reemphasize the importance of air pollutants in other receptors, such as soil-based ecosystems (1). When discussing the impact of air pollutants on ecosystems, the matter of scale becomes important. We will discuss three examples of elements which interact with air, water, and soil media on different geographic scales. These are the carbon cycle on a global scale, the sulfur cycle on a regional scale, and the fluoride cycle on a local scale. 

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