14.5     Iodine-129

 

There are over 100 cosmogenic isotopes with masses over 40 and half-lives over one year, which are therefore potentially useful geochemical tracers or dating tools (Henning, 1987). However, most of these elements are metals, and they are not suited to AMS analysis due to the difficulty of forming negative ions. One of the few heavy isotopes to have found significant application is 129I, which is formed in modest abundance in the atmosphere by spallation of Xe, and which, as a non-metal, forms good negative ion beams.

 

            129I analysis by AMS is relatively straightforward, since the only isobaric interference (129Xe) does not form stable negative ions (Elmore et al., 1980). The principal interference is 127I, which at isotope ratios above 1012 forms a peak tail that must be removed by time-of-flight analysis in addition to magnetic and electrostatic analysers. The 129I/127I detection limit under these conditions is about 10!14.

            As in the case of 36Cl, the 129I tracer has been used to study the entry of anthropogenic material into natural systems. In a study of a marine sediment core from the continental slope off Cape Hatteras (North Carolina), Fehn et al. (1986) found 129I/127I levels at the sediment surface that were two orders of magnitude higher than the relatively constant abundances at depth. This has been confirmed by more recent studies. For example, studies of Mississippi delta sediments (Oktay et al., 2000) gave 129I depth profiles very similar to those for 36Cl. In a similar way, anthropogenic 129I signatures in surface ocean waters mimic the radiocarbon signatures of these waters (Fig. 14.46). Maximum 129I signatures are seen at temperate latitudes, where water mixing is lowest, and minimum concentrations at the poles, where upwelling of deep water swamps the anthropogenic signal (Fehn and Snyder, 2000).

Fig. 14.46 Plot of iodine isotope ratio against latitude for surface ocean waters, showing peak signals of anthropogenic iodine at around 40o north and south. After Fehn and Snyder (2000).

 

            129I has a much longer half-life (15.7 Myr) than the other scientifically useful cosmogenic nuclides. It is therefore applicable to much older systems, but its geological applications are complicated by the significant radiogenic iodine production from in situ uranium fission. This was examined in case studies of the Great Artesian Basin of Australia and the Stripa granite of Sweden (Fabryka-Martin et al., 1985; 1989).

 

            Groundwaters in the Great Artesian Basin range up to ca. 1 Myr in age on the basis of hydrological and 36Cl evidence (above), so that negligible decay of 129I is expected. Therefore, in the absence of contamination by radiogenic iodine or extraneous water sources, 129I/127I ratios should be constant across the basin. Analytical data bear out this prediction to a reasonable extent, consistent with the very low uranium content of the aquifer rocks and the hydrostatic overpressure of the artesian basin relative to potential contaminant water bodies. Since the near-surface water is itself old relative to human activity, there is no anthropogenic signature. However, excess 129I/127I ratios (above normal cosmogenic levels) were seen in water of ca. 150 and 500 kyr age. Fabryka-Martin et al. attributed the latter result to contamination by radiogenic 129I from granitic basement, which forms the floor of the aquifer at its distal end. The cause of the other high value is unknown.

 

            Very different conditions were found in studies of the Stripa granite groundwater (Fabryka-Martin et al., 1989). In this case, radiogenic 129I is present at levels two orders of magnitude higher than cosmogenic iodine. The 129I systematics at Stripa can be seen most clearly when plotted against 36Cl/Cl (Fig. 14.47). Except for one shallow water sample with a prominent anthropogenic 36Cl signature, the data form an array trending from estimated meteoric recharge towards a pure radiogenic component. This array could result from mixing between two end-members, but it could also result from variable, but correlated, production of radiogenic 129I and 36Cl in the granite, since both are controlled by the uranium content of the rock. Hence, the main role for 129I is to gauge in situ radiogenic perturbation of 36Cl ages in ground-water systems.

Fig. 14.47. Plot of absolute 129I abundance against the 36Cl/total Cl ratio for groundwaters from the Stripa mine, Sweden. Radiogenic and anthropogenic signatures are shown. After Fabryka-Martin et al. (1989).

 

 

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