Assignment 6 - Solved Problems - Chemical Ocean | OCEAN 400, Assignments of Geology

Material Type: Assignment; Class: CHEMICAL OCEAN; Subject: Oceanography; University: University of Washington - Seattle; Term: Winter 2009;

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Ocean 400 Name:_________________
Chemical Oceanography 17 February 2009
Winter 2009 (show all your work)
Problem Set #6
1) What controls atmospheric CO2.
As water upwells (Vmix) from the deep ocean to the surface, it equilibrates with the
atmosphere. Biological activity in the surface ocean affects the oceanic carbonate system
and the resulting pCO2 in the atmosphere. For this problem, please calculate atmospheric
pCO2, deep water O2, and AOU for the following four cases:
a.) an abiotic ocean
b.) a productive ocean with preformed phosphate [PO4]º = 0.90 µmol / kg
c.) a productive ocean with no surface PO4
d.) a productive ocean with [PO4]º = 0.90 µmol / kg that is dominated by
siliceous organisms (there are no CaCO3 shells, and hence alkalinity is not
affected by particle flux)
Information you’ll need:
[DICd] = 2250 µmol / kg [Alkd] = 2365 µeq / kg
[PO4 deep] = 2.2 µmol / kg Vmix = 300 cm / yr (note units!)
KH’ (CO2) = 10-1.53 mol / kg atm KH’ (O2) = 10-2.77 mol / kg atm
pO2 = 0.2095 atm K1’ = 10-6 mol / kg
K2’ = 10-9 mol / kg Assume 1 kg = 1 L
Assume the ocean is in steady state. What this implies is that river input is equal
to permanent particle burial, so for this problem do not include rivers or sedimentation
since they will cancel and have a net zero influence on the system. You’ll want to start
by making a PO4 balance for the surface box, and then use Redfield ratios to figure out
surface DIC and alkalinity (see hints below). Assume that the pO2, the partial pressure of
oxygen in the surface ocean, stays constant and in equilibrium with the atmosphere
throughout all four cases.
To calculate DIC from the phosphate balance, use the composite Redfield ratio
determined by Broecker and Peng, which takes into account both “soft” and “hard” parts,
P:N:C:Ca = 1:15:131:26. Assume all the Ca in the B flux is due to CaCO3, so you can use
the ratio of P:Ca:CO3:Alk to find BAlk. In part (d), since no CaCO3 shells are forming,
you should use the Redfield ratio, 1 P:106 C.
We highly recommend that you do your calculations in a spreadsheet after
drawing your box model diagram and writing out your equations. Please e-mail Andrea
your spreadsheet file, named “JaneDoePS4.xls” (obviously, insert your own name), and
hand in a paper copy of the diagrams and equations you used and your answers. You
won’t be graded based on the equations in the spreadsheet.
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Ocean 400 Name:_________________ Chemical Oceanography 17 February 2009 Winter 2009 (show all your work)

Problem Set

  1. What controls atmospheric CO 2.

As water upwells (Vmix ) from the deep ocean to the surface, it equilibrates with the atmosphere. Biological activity in the surface ocean affects the oceanic carbonate system and the resulting pCO 2 in the atmosphere. For this problem, please calculate atmospheric pCO 2 , deep water O 2 , and AOU for the following four cases:

a.) an abiotic ocean b.) a productive ocean with preformed phosphate [PO 4 ]º = 0.90 μmol / kg c.) a productive ocean with no surface PO 4 d.) a productive ocean with [PO 4 ]º = 0.90 μmol / kg that is dominated by siliceous organisms (there are no CaCO 3 shells, and hence alkalinity is not affected by particle flux)

Information you’ll need: [DICd ] = 2250 μmol / kg [Alkd ] = 2365 μeq / kg [PO4 deep ] = 2.2 μmol / kg V (^) mix = 300 cm / yr (note units!) KH’ (CO 2 ) = 10-1.53^ mol / kg atm KH’ (O 2 ) = 10 -2.77^ mol / kg atm pO 2 = 0.2095 atm K 1 ’ = 10-6^ mol / kg K 2 ’ = 10 -9^ mol / kg Assume 1 kg = 1 L

Assume the ocean is in steady state. What this implies is that river input is equal to permanent particle burial, so for this problem do not include rivers or sedimentation since they will cancel and have a net zero influence on the system. You’ll want to start by making a PO 4 balance for the surface box, and then use Redfield ratios to figure out surface DIC and alkalinity (see hints below). Assume that the pO 2 , the partial pressure of oxygen in the surface ocean, stays constant and in equilibrium with the atmosphere throughout all four cases.

To calculate DIC from the phosphate balance, use the composite Redfield ratio determined by Broecker and Peng, which takes into account both “soft” and “hard” parts, P:N:C:Ca = 1:15:131:26. Assume all the Ca in the B flux is due to CaCO 3 , so you can use the ratio of P:Ca:CO 3 :Alk to find BAlk. In part (d), since no CaCO3 shells are forming, you should use the Redfield ratio, 1 P:106 C.

We highly recommend that you do your calculations in a spreadsheet after drawing your box model diagram and writing out your equations. Please e-mail Andrea your spreadsheet file, named “JaneDoePS4.xls” (obviously, insert your own name), and hand in a paper copy of the diagrams and equations you used and your answers. You won’t be graded based on the equations in the spreadsheet.

Here is a basic outline and some hints so that you can stay on track! --Figure out BPO4 first. The concept of “preformed” nutrients, like phosphate, is described in the Power Point, Lecture 16 (it might help to think of it as excess or unutilized nutrient).

--You can use elemental ratios (use the composite Redfield ratio determined by Broecker and Peng, which takes into account both “soft” and “hard” parts, P:N:C:Ca = 1:15:131:26) to then figure out BC and BCa. Since we assume the whole Ca flux is due to CaCO 3 , you can also get BAlk by using the ratio of P:Ca:CO 3 2-:Alk. Hint: each CO 3 2- contributes two units of alkalinity!

--Do a mass balance for the surface box to figure out DICs.

--Do the same to get Alks.

--When you have DIC and Alk, you’ll need to do some algebra (what equations to use?) to get the (surface ocean) pH. Hint: consider using α values.

--When you have pH (and you already know DIC), you can figure out the pCO 2 in the atmosphere. pCO 2 is entirely dependent on the ocean.

--For O 2 : the atmospheric O 2 is fixed, so you can calculate the amount of O 2 in the surface ocean using KH’^ for O 2 (given).

--Calculating O2 deep can be done exactly as we did in a previous problem set using the C:O 2 ratio of 106:154. sources = sinks…(we can assume all of the B flux is consumed in the deep ocean, since we are neglecting burial, and thus all of the particulate carbon flux will contribute oxygen utilization in the deep ocean).

--Once you have that, AOU should be a cinch.

Random items: --Check your units! You will need to do conversions. Assume 1 kg = 1 L. --The quadratic equation. If: ax^2 + bx + c = 0 where a, b, and c are constants, then x = -b ± √(b^2 -4ac) 2a Note that your a, b, and c might not necessarily be easy numbers, so it can help to calculate these first, and then try and solve the part you actually want. If you’re doing a spreadsheet, I recommend having columns or rows for a, b, and c.