Interpreting profiles of pore water solutes. First, solute transport (simple) 1.Diffusive Transport: 2. Sediment Burial Generally: Assume a constant mass.

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Presentation transcript:

Interpreting profiles of pore water solutes

First, solute transport (simple) 1.Diffusive Transport: 2. Sediment Burial Generally: Assume a constant mass flux (…not always true) Mass accumulation rate:

Solute burial, cont. Below the “compacting layer” Which must be the same as MAR at shallower depths… That’s for solids…

For solutes… The burial rate for solutes is slightly smaller than for solids… AND

Interpreting pore water profiles… In general: we consider rates of change of concentration over space and time We derive descriptive expressions by considering the mass balance in a layer of sediment x1 x2 R F1F1 F2F2 In the box:

Interpreting, cont. (x2 - x1) --> small… Since…

Interpreting, cont… Then… Simplify: steady state ; constant  ; constant D ; burial << transport:

==> A simple interpretation of pw profiles

Interpretation of profile shapes : quantitative Steady-state mass balance in a sediment layer: Rate of reaction within the layer = net flux out of the layer Diffusive flux : oxic denitrification 1 2 Flux at pt. 1 (x=0) : gives total, net NO3 Production in sediment column Flux at pt. 2 : gives rate of NO3 consump. By denitrification Sum of absolute values of Flux at 1 + Flux at 2: Gives rate of NO3 production by oxic Decomposition of organic matter

But we can get more information… What else do we need to solve this equation?

But we can get more information… Boundary conditions! At sediment-water interface (x=0) At depth in the sediments:

What about R ? Example : organic matter oxidation by O 2 What solutes could you measure to define reaction rate?

For O 2, it has been convenient to use R =  P(x) i.e., with no dependence on [O 2 ], even though it’s a reactant Can that be justified? Devol (1978) DSR 25, Cultured marine bacteria from low-O 2 waters… Found O 2 consumption followed Michaelis-Menten kinetics: And found a “Critical O 2 Concentration” below Which rate depended on [O 2 ] Of ~ 2.4 µmol/l What about R ?

Pore water profiles :O 2 all done by in situ microelectrode profiling Total Corg ox. Rate (µmol/cm2/y)

Continental margin sediments: * large organic matter flux * electron acceptors other than O 2 Let’s consider a sediment dominated by sulfate reduction: Defining P as the production rate of a solute, What would we predict pore water profiles of these 3 solutes to look like? Solution:

Solve the equation for each solute: Assume porosity = 0.8 and D sed = D sw x (porosity) 2 … then D HCO3- = 323 cm 2 /y, D NH4+ = 543 cm 2 /y, D HPO42- = 208 cm 2 /y Assume P 0 = 100, p 1 = 0.2

Plotting the concentration of one solute vs. another… Interpreting the slopes: At any depth, Therefore, the slopes imply

A mineral, undersaturated in seawater apparently simple dissolution kinetics… What do we expect [Si(OH) 4 ] in pore water to look like? C BW C SAT Concentration Diagenesis of a solid, undersaturated in bw Asymptotic approach to Saturation in pore water

Csat = Csat = 600 Csat = Csat = N. Atlantic ( Bermuda) Peru Margin Southern Ocean Observations: Si(OH) 4 In pore waters