pore water fluxes and mass balance solute transport: fickâ€™s first law of...
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DESCRIPTIONPore water fluxes and mass balance Solute transport: Fick’s first law of diffusion: Einstein equation (diffusive depth/time scale) x 2 = 2Dt Pore water profiles: Reaction Advection Changing porosity, diffusivity. Diffusion only case diffusive flux ( = J ) = - D dC/dz - PowerPoint PPT Presentation
Pore water fluxes and mass balanceSolute transport:Ficks first law of diffusion:
Einstein equation (diffusive depth/time scale)x2 = 2Dt
Pore water profiles:ReactionAdvectionChanging porosity, diffusivity
Diffusion only case diffusive flux ( = J ) = - D dC/dz "Fick's first law of diffusion"Solutes diffuse from high concentration to low concentration (high and low activity), and the flux is proportional to the concentration gradient.
Diffusion only case For diffusion in a porous medium (i.e., in pore water) the area occupied by sediment grains must be taken into account by factoring in the sediment porosity (), and by using a "bulk" diffusivity rather than the molecular diffusivity. SoJ = - D(bulk) dC/dzIn pure water D (molecular) varies with solute chemistry, and with temperature.
For pore water, D (bulk) also takes into account the effects of electrical effects (electroneutrality), and sediment tortuosity ().
Porosity = total connected water volume (as fraction of bulk sediment volume)
Tortuosity a measure of diffusive path length relative to bulk length.The tortuosity effect is given by:D(bulk) = D(molec) / 2
Tortuosity can be detemirned empirically, by measuring the electrical resistivity of bulk sediment and sea water:
2 = * F
where F is the "formation factor", the ratio of bulk sediment resistivity to pore water resistivity.Often, tortuosity is estimated using only porosity data, with an empirical relationship of the form:
2 = ()(-n)
where n is typically 1.5 or 2.