28
F. J. Millero
TA(IIM)
NTA(IIM)
2300
2350
2400
2450
2500
2350
2400
2450
2500
0
1000
g
2000
..c::
Co
~ 3000
4000
North
Atlantic
5000
Fig. 1.15. The total alkalinity (TA) and normalized total alkalinity (NTA) as a function of depth in the
Atlantic and Pacific Ocean (Millero 1996)
ters are higher in the Pacific than in the Atlantic. The higher NTA in deep waters is
related to the dissolution of CaC0 3 • The deep Pacific alkalinity values are higher than
those in the Atlantic, because they are older and have accumulated more coj- from
the dissolution of CaC03•
1.4.4
Te02
The total normalized dissolved inorganic carbon dioxide (NTC02 = TC02 x 35 I S) in
the Atlantic and Pacific oceans for surface waters is shown in Fig. 1.16. Unlike the alkalinity, the total CO 2 in the equatorial waters shows a large increase, due to equatorial upwelling. The TC02 shows little latitudinal change. For rapid exchange the PC02
in the water and air are similar, and the TC02 is higher in polar regions. The depth
profiles of NTC0 2 in the Atlantic and Pacific are shown in Fig. 1.17. The values decrease
to a minimum in surface waters due to photosynthesis. In deeper waters the NTC02
increases due to the oxidation of plant material. The values of NTC02 for deep Pacific
waters are higher than those for the Atlantic because the waters are older and have
had more time to accumulate CO 2 due to microbial oxidation. The values of NTC02
and NTA correlate very well with each other, and can be used to characterize various
water masses. The deep waters increase by 20 Ilmol kg- 1 from the North to South Atlantic. A section of TC0 2 in the Atlantic Ocean is shown in Fig. 1.18. The values dearly
show the differences due to the major water masses (North Atlantic Deep Water, Antarctic Intermediate Water and Antarctic Bottom Water).
Due to the buffering effect of sea water, only a small amount of CO2 needs to be
transferred to the oceans to restore the equilibrium between the atmosphere and surface. This buffering is called the Revelle factor (R). It is the ratio of the fractional rise
F. J. Millero
TA(IIM)
NTA(IIM)
2300
2350
2400
2450
2500
2350
2400
2450
2500
0
1000
g
2000
..c::
Co
~ 3000
4000
North
Atlantic
5000
Fig. 1.15. The total alkalinity (TA) and normalized total alkalinity (NTA) as a function of depth in the
Atlantic and Pacific Ocean (Millero 1996)
ters are higher in the Pacific than in the Atlantic. The higher NTA in deep waters is
related to the dissolution of CaC0 3 • The deep Pacific alkalinity values are higher than
those in the Atlantic, because they are older and have accumulated more coj- from
the dissolution of CaC03•
1.4.4
Te02
The total normalized dissolved inorganic carbon dioxide (NTC02 = TC02 x 35 I S) in
the Atlantic and Pacific oceans for surface waters is shown in Fig. 1.16. Unlike the alkalinity, the total CO 2 in the equatorial waters shows a large increase, due to equatorial upwelling. The TC02 shows little latitudinal change. For rapid exchange the PC02
in the water and air are similar, and the TC02 is higher in polar regions. The depth
profiles of NTC0 2 in the Atlantic and Pacific are shown in Fig. 1.17. The values decrease
to a minimum in surface waters due to photosynthesis. In deeper waters the NTC02
increases due to the oxidation of plant material. The values of NTC02 for deep Pacific
waters are higher than those for the Atlantic because the waters are older and have
had more time to accumulate CO 2 due to microbial oxidation. The values of NTC02
and NTA correlate very well with each other, and can be used to characterize various
water masses. The deep waters increase by 20 Ilmol kg- 1 from the North to South Atlantic. A section of TC0 2 in the Atlantic Ocean is shown in Fig. 1.18. The values dearly
show the differences due to the major water masses (North Atlantic Deep Water, Antarctic Intermediate Water and Antarctic Bottom Water).
Due to the buffering effect of sea water, only a small amount of CO2 needs to be
transferred to the oceans to restore the equilibrium between the atmosphere and surface. This buffering is called the Revelle factor (R). It is the ratio of the fractional rise