ATMOSPHERIC CARBON DIOXIDE AND RADIOCARBON: II 131 



2622 38 



-log (K ) = — - — + 15.5873 - 0.0178471T 



+ 0.0117950 CI - (2.77676 X 10" 5 ) Cl T (D.6) 



-log (Ki) = — 15.6500 + 0.034153T 



-0.074709 (Cl) 1/2 - 0.0023483 Cl (D.7) 



2902 39 

 -log (K 2 ) = 6.4980 + 0.023790T 



0.45322 (Cl) % + 0.035226 Cl (D.8) 



2291 90 

 log (K B ) = — 3.3850 + 0.01756T 0.32051 (CD* (D.9) 



K w was interpolated from a table of Harvey. 45 By a widely accepted convention 

 [H + ] was replaced in the defining Eqs. D.2 to D.5 by a thermodynamic activity 

 whose negative logarithm is denoted by the symbol pH. This replacement has a 

 negligible effect on the calculations discussed in this paper, and we have assumed 

 pH = -log [H + ]. 



The values of the equilibrium quotients for average ocean surface water are 

 K = 0.03347, K t = 9.747 X 10" 7 , K 2 = 8.501 X 10" 10 , K B = 1.881 X 10~ 9 , and 

 Kw = 6.463 X 10 . Other properties of average ocean surface water are: 

 alkalinity (A) = 2.435 meq/liter, initial pH = 8.271, total boron concentration 

 (SB) = 0.409 millimole/liter, and initial total inorganic-carbon concentr- 

 ation = 2.057 millimole/liter. The chemical properties of average ocean water are 

 as derived by Keeling. 5 



The equation for total inorganic carbon concentration is 



2C= [C0 2 ] + [HCOi] + [COl - ] = ?£ (D.10) 







where 



r K °( 1 + [Fi + Ti^) «>"> 



0o in Appendix C is evaluated at the initial hydrogen-ion concentration. The 

 variation of with isotopic mass (which enters the perturbation equations only 

 as the ratio of *00 O /*0 O where *0 and *0 O denote the radioisotope equivalents 

 of and O ) is too small to justify distinguishing between inactive and 

 radiocarbon. 5 



