Stable H-O Isotopic Composition and Water Quality Assessment of Surface Water and Groundwater: A Case Study in the Dabie Mountains, Central China

Abstract

In order to understand the water cycle and assess the water quality for irrigation purposes in the Upper Pi River Basin (UPRB), which is the northern slope of the Dabie Mountains, 68 surface water and groundwater samples were collected and analyzed for H-O isotopes and hydrochemistry during the high-flow season in 2017 and 2018. The results show that ranges of hydrogen and oxygen isotopic composition (δ2H: −68.8‰ to −40.8‰, δ18O: −10.05‰ to −5.05‰) are controlled by the medium latitude and high altitude of the UPRB. Among different types of water, the δ2H and δ18O values can be ordered as follows: reservoir water < spring water ≈ river water < pond water. The water of the upstream medium and small reservoir is enriched with lighter isotopes that is likely related to more exchange with rainwater and less residence time; however, large reservoirs are similar to the upstream river and spring in terms of the H-O isotopic composition. Hydro-chemical facies are dominated by the Ca-HCO3 type in the UPRB, which reflects fresh recharged water from rainfall, and few samples are of the Ca-Cl type that is caused by intensive evaporation. The water quality for irrigation purposes was also evaluated. According to the Wilcox diagram, United States Salinity Laboratory (USSL) diagram, magnesium hazard, and Kelly’s ratio, all water samples have been considered suitable for irrigation water.

Spatial Variation and Controlling Factors of H and O Isotopes in Lancang River Water, Southwest China

“…Hence, Lancang River water did not experience significant evaporation. Scatter plots of δ 18 O and δ 2 H in the wet season in the river water of the Lancang River (this study), the Yellow River [38], the Huai River [30,39], the Yangtze River [40], the Jiulong River [29], the Pearl River [41], and the Mun River [42]. Table 1.…”

“…Locations, water temperature (T), dissolved oxygen (DO), total dissolved solid (TDS), and isotope composition of river water samples. We compared the stable isotopic composition in the wet season of the water of seven rivers in Asia, characterized by different climate types and altitudes, including the Lancang River (this study), the Yellow River, mainly in the temperate zone [38], the Huai River in the temperate-subtropical transition zone [30,39], the Yangtze River, mainly in the subtropical zone [40], the Jiulong River in the subtropical zone [29], the Pearl River in the subtropical zone [41], and the Mun River in the tropical zone [42]. In Figure 2, the mean values of the isotopic composition of different rivers were obviously different, especially when comparing the Lancang River with other rivers.…”

“…Also, the interaction between groundwater and surface water can be traced by H and O isotopes [27,28]. Further, stable H and O isotopes have demonstrated the influence of anthropogenic processes upon the water cycle [29,30]. Cascade dams are massively constructed on the main stream and major tributaries of the Lancang-Mekong River, which may be accelerating and magnifying the long-term effect of climate changes and global warming [31].…”

Active metal deposition in a giant geothermal system

“…Details of water sampling, pre‐treatment, analysis and accuracy have been provided earlier (Dong & Brooks, 2006; Shiller et al, 2006; Zhang et al, 2022). Analyses of major ion (F − , Cl − , NO 3 − , SO 4 2− , HCO 3 − , CO 3 2− , Na + , K + , Mg 2+ and Ca 2+ ), elemental (Li, Be, Sc, Ti, V, Mn, Cr, Co, Ni, Cu, Zn, Ga, Rb, Y, Nb, Mo, Cd, Sb, Cs, Ba, La, Ce, Pr, Nd, Sm, Eu, Gd, Tb, Dy, Ho, Er, Tm, Yb, Lu, W, Tl, Pb, Bi, Th, U, Sr, B) and O–H isotopic compositions (Yang et al, 2019) were undertaken at the Analysis and Testing Center of Beijing Research Institute of Uranium Geology, China.…”

Hydrochemical differences between river water and groundwater in Suzhou, Northern Anhui Province, China

“…Moreover, several studies have found that evaporation and water rock interaction can increase the δ 18 O in the water, then leading to the decrease of d-excess [33,34]. In this study, the d-excess of RW samples ranges from −4.5 to 5.7‰ (mean = −0.2‰), which is lower than the d-excess value of atmospheric precipitation ( Table 1 and Figure 5), and therefore, the river water might have been affected by evaporation.…”