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Geological Society, London, Special Publications; 2001; v. 189; p. 193-212;
DOI: 10.1144/GSL.SP.2001.189.01.12
© 2001 Geological Society of London

Isotopic methods and their hydrogeochemical context in the investigation of palaeowaters

H. H. Loosli1, W. Aeschbach-Hertig2, F. Barbecot4, P. Blaser1, W. G. Darling3, L. Dever4, W. M. Edmunds3, R. Kipfer2, R. Purtschert1 & K. Walraevens5

1 University of Bern, Climate and Environmental Physics, Sidlerstrasse 5, CH-3012, Bern, Switzerland
2 EAWAG, Ueberlandstrasse 133, CH 8600 Dübendorf, Switzerland
3 Hydrogeology Group, British Geological Survey, Maclean Building, Wallingford, Oxon, OX10 8BB UK
4 Université Paris-Sud, Lab. d’Hydrologie et de Géochimie Isotopique, Bat. 504, F-91405 Orsay Cedex, France
5 Ghent University, Lab. Applied Geology and Hydrogeology, Krijgslaan 281, B-9000, Gent, Belgium

Isotope and geochemical techniques are the primary way in which the residence time, recharge conditions and subsequent evolution of palaeowaters can be determined. Isotopic species and noble gas concentrations are used as residence time and palaeoclimate indicators. Among the former, 14C is pre-eminent in late Quaternary studies because of an age range which covers the Pleistocene-Holocene transition. However, its use is constrained by frequent difficulties in determining the dilution of dissolved 14C due to water-rock interaction. A combination of 14C data with 226Ra and 4He results may be useful for Holocene waters but they can also be used to validate the carbon systematics assumed for 14C dating. For waters beyond the range of 14C dating, 81Kr, 36Cl, 4He and chemical tracers can be applied.

Stable isotope ratios and noble gas concentrations primarily reflect climatic conditions at the time of recharge. While the noble gases provide absolute values for recharge temperatures, stable isotopes are only relative indicators that vary regionally. The PALAEAUX programme has examined these aspects in some detail by looking at the {delta}18O shift between Pleistocene and Holocene waters on the European scale, and by calculating {delta}18O/{Delta}T ratios from {delta}18O v. recharge temperature plots for aquifers at different distances from the Atlantic Ocean. Indications are that the more positive {delta}18O value of ocean water during the Pleistocene dominates in the more westerly European countries over the negative {delta}18O shift during cooler conditions. There are also indications that air-mass circulation during the Pleistocene was similar to the present day.

The evolution of a palaeowater can best be studied by measuring chemical tracers; this is possible in freshwater aquifers, where a clear trend of geochemical reactions is observed, and in freshening marine aquifers. Chemical and isotopic tracers can also be used to study the movement of the front between palaeowater and younger components that must be identified in coastal aquifers to guarantee a sustainable water use.





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