By Christian E Junge

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The resulting flux of CO, in the atmosphere from low to high latitudes must be counterbalanced by a corresponding flux in the ocean when arctic waters sink and spread to low latitudes. 3 25 CARBON DIOXIDE Ranwisher (1960) points out that a t least locally, the growth and decay of marine plankton can result in considerable changes of the [CO,] of ocean water with a seasonal trend, but there are too few data to reveal any seasonal effects over sea water and to estimate the biological influence. Naturally, daily variations are small over the oceans.

Paetzold, 1957). In our discussion, emphasis will be placed on the distribution of ozone in the atmosphere, particularly in the troposphere, in the light of the most recent data on vertical profiles and on its budget. Ozone is a comparatively minor constituent of the atmosphere, with an average concentration of about 2 to 3 x ppm if uniformly distributed. The unit ordinarily used to express the total amount of ozone in the atmosphere is the height of an equivalent column of ozone a t standard temperature and pressure.

The CI4 content of various shells shows this value to be about 400 years, but since there may be some local dilution by C12 carbonates from rivers in the coastal waters where these shells grow, 300 years seems to be a reasonable figure (Revelle and Suess, 1957). &/A is equivalent to the average total amount of C14 per em2, and thus the deuominator is the ratio of 8 4 in the sea to that in the atmosphere. 0 X gr/cm2 sec. The greatest uncertainty in tam* is introduced by that of Q, which is about 25%.

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