120 BACASTOW AND KEELING 



Deep sea 



Water conservation 



^j- = k md N m + F g - k dm N d (A.7) 



= k md W m -k dm W d (A.8) 



where k u j = upper-atmosphere to lower-atmosphere transfer coefficient 



ki u = lower-atmosphere to upper-atmosphere transfer coefficient [the 

 preindustrial equation leads to k) u = k u j (N u0 /N] )] 

 k am = air to sea transfer coefficient [defined in terms of the carbon mass 

 of the total atmosphere; e.g., the preindustrial (steady-state) flux is 



kamNaol 

 km a = sea to a i f transfer coefficient (the preindustrial flux k ma P m0 is 



numerically equal to k am N a0 ) 

 k md , k dm = surface-layer to deep-ocean and deep-ocean to surface-layer transfer 



coefficients, respectively 

 (All transfer coefficients, k;; are assumed to be time invariant.) 



N u ,N b , N e , 



N\, N m , N d = masses of inactive carbon in designated reservoirs 



N a = N u + N| = mass of inactive carbon in the atmosphere as a 

 whole 



Nuo> N b0 , N e0 , 

 Nio. N m0, N d0 , 



N a0 = masses of inactive carbon in the designated reservoir before 

 the industrial era 



Fib = FboU + ln (Ni/Nio)] (N b /N b0 ) = flux from lower atmo- 

 sphere to long-lived land biota 



F b0 = flux from lower atmosphere to long-lived land biota before 

 industrial era and vice versa 



(5 = land-biota growth factor (assumed to be time invariant) 



F b i = F b0 (N b /N b0 ) = flux from long-lived land biota to lower 

 atmosphere 



Fie = F e0 [l + /3 In (N e /N e0 )] (N b /N b0 ) = flux from lower atmo- 

 sphere to short-lived land biota (taken as proportional to 

 N b /N b0 rather than N e /N e0 ) 



F e0 = flux from lower atmosphere to short-lived land biota before 

 the industrial era and vice versa 



F e l = F e0 (N e /N e0 ) = flux from short-lived land biota to lower 

 atmosphere 



