Technical note: Evaporating water is different from bulk soil water in <i>δ</i>²H and <i>δ</i>¹⁸O and has implications for evaporation calculation

• Main Authors: H. Wang, J. Jin, B. Cui, B. Si, X. Ma, M. Wen
• Format: Article
• Language: English
• Published: Copernicus Publications 2021-10-01
• Series: Hydrology and Earth System Sciences
• Online Access: https://hess.copernicus.org/articles/25/5399/2021/hess-25-5399-2021.pdf
• ISSN: 1027-5606; 1607-7938

<p>Soil evaporation is a key process in the water cycle and can be conveniently quantified using <span class="inline-formula"><i>δ</i>²H</span> and <span class="inline-formula"><i>δ</i>¹⁸O</span> in bulk surface soil water (BW). However, recent research shows that soil water in larger pores evaporates first and differs from water in smaller pores in <span class="inline-formula"><i>δ</i>²H</span> and <span class="inline-formula"><i>δ</i>¹⁸O</span>, which disqualifies the quantification of evaporation from BW <span class="inline-formula"><i>δ</i>²H</span> and <span class="inline-formula"><i>δ</i>¹⁸O</span>. We hypothesized that BW had different isotopic compositions from evaporating water (EW). Therefore, our objectives were to test this hypothesis first and then evaluate whether the isotopic difference alters the calculated evaporative water loss. We measured the isotopic composition of soil water during two continuous evaporation periods in a summer maize field. Period I had a duration of 32 d, following a natural precipitation event, and period II lasted 24 d, following an irrigation event with a <span class="inline-formula">²H</span>-enriched water. BW was obtained by cryogenically extracting water from samples of 0–5 cm soil taken every 3 d; EW was derived from condensation water collected every 2 d on a plastic film placed on the soil surface. The results showed that when event water was heavier than pre-event BW, <span class="inline-formula"><i>δ</i>²H</span> of BW in period II decreased, with an increase in evaporation time, indicating heavy water evaporation. When event water was lighter than the pre-event BW, <span class="inline-formula"><i>δ</i>²H</span> and <span class="inline-formula"><i>δ</i>¹⁸O</span> of BW in period I and <span class="inline-formula"><i>δ</i>¹⁸O</span> of BW in period II increased with increasing evaporation time, suggesting light water evaporation. Moreover, relative to BW, EW had significantly smaller <span class="inline-formula"><i>δ</i>²H</span> and <span class="inline-formula"><i>δ</i>¹⁸O</span> in period I and significantly smaller <span class="inline-formula"><i>δ</i>¹⁸O</span> in period II (<span class="inline-formula"><i>p</i>&lt;0.05</span>). These observations suggest that the evaporating water was close to the event water, both of which differed from the bulk soil water. Furthermore, the event water might be in larger pores from which evaporation takes precedence. The soil evaporative water losses derived from EW isotopes were compared with those from BW. With a small isotopic difference between EW and BW, the evaporative water losses in the soil did not differ significantly (<span class="inline-formula"><i>p</i>&gt;0.05</span>). Our results have important implications for quantifying evaporation processes using water stable isotopes. Future studies are needed to investigate how soil water isotopes partition differently between pores in soils with different pore size distributions and how this might affect soil evaporation estimation.</p>