22
400
380
Air
360
E
cp
....
~
III
3- 340
8
N
V
Q.
320
300
280
-40
-20
o
20
40
Lattitude
F. J. Millero
Air
1
b 1 1
10
~~I
CO 9
1
60
Fig. 1.S. The partial pressure of carbon dioxide in the atmosphere and surface waters of the Atlantic
Ocean (2S0W) (Millero 1996)
ing the spring bloom. As discussed earlier, for this biological pump to take CO2 permanently from the atmosphere, the organic carbon must sink below the thermocline
and be oxidized back to CO2 where it can be stored for hundreds of years in deep waters.
The depth profiles of Pe0 2 for the Atlantic and Pacific oceans are shown in Fig. 1.11.
These values were calculated from TA and Te02, so they are not as accurate as direct
measurements. The general trends, however, are real and as expected. The surface values are similar to atmospheric values. The values increase to a maximum (500 Jlatm
in the North Atlantic Ocean and 1200 Jlatm in the Pacific Ocean) at 1 km due to the
oxidation of plant material. The higher values at 1 km in the Pacific Ocean are due to
the higher productivity of the surface waters resulting in the production of more organic carbon. The deep water values in the Pacific Ocean are higher than in the Atlantic Ocean due to the fact that the waters are older and have accumulated more CO2
from the oxidation of organic carbon as the waters make the trip from the N. Atlantic
to the N. Pacific (600 years). The deep waters originally formed at the surface have
lower Peo 2 than the values at the oxygen minimum.
1.4.2
pH
The pH of most surface waters in equilibrium with the atmosphere is 8.2 ±O.1. Recent
measurements of pH in the surface waters of the Atlantic and Pacific Ocean are shown
400
380
Air
360
E
cp
....
~
III
3- 340
8
N
V
Q.
320
300
280
-40
-20
o
20
40
Lattitude
F. J. Millero
Air
1
b 1 1
10
~~I
CO 9
1
60
Fig. 1.S. The partial pressure of carbon dioxide in the atmosphere and surface waters of the Atlantic
Ocean (2S0W) (Millero 1996)
ing the spring bloom. As discussed earlier, for this biological pump to take CO2 permanently from the atmosphere, the organic carbon must sink below the thermocline
and be oxidized back to CO2 where it can be stored for hundreds of years in deep waters.
The depth profiles of Pe0 2 for the Atlantic and Pacific oceans are shown in Fig. 1.11.
These values were calculated from TA and Te02, so they are not as accurate as direct
measurements. The general trends, however, are real and as expected. The surface values are similar to atmospheric values. The values increase to a maximum (500 Jlatm
in the North Atlantic Ocean and 1200 Jlatm in the Pacific Ocean) at 1 km due to the
oxidation of plant material. The higher values at 1 km in the Pacific Ocean are due to
the higher productivity of the surface waters resulting in the production of more organic carbon. The deep water values in the Pacific Ocean are higher than in the Atlantic Ocean due to the fact that the waters are older and have accumulated more CO2
from the oxidation of organic carbon as the waters make the trip from the N. Atlantic
to the N. Pacific (600 years). The deep waters originally formed at the surface have
lower Peo 2 than the values at the oxygen minimum.
1.4.2
pH
The pH of most surface waters in equilibrium with the atmosphere is 8.2 ±O.1. Recent
measurements of pH in the surface waters of the Atlantic and Pacific Ocean are shown