Articles | Volume 25, issue 10
Hydrol. Earth Syst. Sci., 25, 5399–5413, 2021
Hydrol. Earth Syst. Sci., 25, 5399–5413, 2021
Technical note
07 Oct 2021
Technical note | 07 Oct 2021

Technical note: Evaporating water is different from bulk soil water in δ2H and δ18O and has implications for evaporation calculation

Hongxiu Wang et al.

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Cited articles

Allison, G. B. and Barnes, C. J.: Estimation of evaporation from non-vegetated surfaces using natural deuterium, Nature, 301, 143–145,, 1983. 
Aminzadeh, M. and Or, D.: Energy partitioning dynamics of drying terrestrial surfaces, J. Hydrol., 519, 1257–1270,, 2014. 
Beven, K. and Germann, P.: Macropores and water flow in soils, Water Resour. Res., 18, 1311–1325,, 1982. 
Booltink, H. W. G. and Bouma, J.: Physical and morphological characterization of bypass flow in a well-structured clay soil, Soil Sci. Soc. Am. J., 55, 1249–1254,, 1991. 
Brooks, J. R., Barnard, H. R., Coulombe, R., and McDonnell, J. J.: Ecohydrologic separation of water between trees and streams in a Mediterranean climate, Nat. Geosci., 3, 100–104,, 2010. 
Short summary
Evaporation led to progressively more heavy-isotope-enriched bulk soil water (BW) following the precipitation/irrigation of heavy-isotope-depleted new water but causes progressively more heavy-isotope-depleted BW following irrigation of heavy-isotope-enriched new water. The results indicated that δ2H and δ18O in evaporating water (EW) were similar to new water and differed from BW. However, the evaporative water loss calculated from BW did not differ significantly from that of EW.