Next Article in Journal
The Effect of Irrigation Treatment on the Growth of Lavender Species in an Extensive Green Roof System
Next Article in Special Issue
A Forty-Year Karstic Critical Zone Survey (Baget Catchment, Pyrenees-France): Lithologic and Hydroclimatic Controls on Seasonal and Inter-Annual Variations of Stream Water Chemical Composition, pCO2, and Carbonate Equilibrium
Previous Article in Journal
Classification of Management Alternatives to Combat Reservoir Sedimentation
Previous Article in Special Issue
Ubiquitous Fractal Scaling and Filtering Behavior of Hydrologic Fluxes and Storages from A Mountain Headwater Catchment
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:

Climatic Variabilities Control the Solute Dynamics of Monsoon Karstic River: Approaches from C-Q Relationship, Isotopes, and Model Analysis in the Liujiang River

School of Management Science, Guizhou University of Finance and Economic, Guiyang 550025, China
State key laboratory of Environmental Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences, Guiyang 550081, China
Tianjin Key Laboratory of Water Resources and environment, Tianjin Normal University, Tianjin 300387, China
School of Public Managemerent, Guizhou University of Finance and Economics, Guiyang 550025, China
School of Eco-Environment Engineering, Guizhou Minzu University, Guiyang 550025, China
Authors to whom correspondence should be addressed.
Water 2020, 12(3), 862;
Submission received: 14 February 2020 / Revised: 14 March 2020 / Accepted: 16 March 2020 / Published: 19 March 2020


The dynamics of riverine solutes’ contents and sources reflect geological, ecological, and climatic information of the draining basin. This study investigated the influence of climatic variability on solute dynamics by the high-frequency hydrogeochemical monitory in the Liujiang River draining karst terrain of Guangxi Province, SW (Southwestern) China. In the study river, the content-discharge (C-Q) patterns of riverine solutes indicate that the majority of riverine solutes show similar dilution and near chemostatic behaviors responding to increasing discharge, especially geogenic solutes (such as weathering products from carbonate, silicate, and sulfide oxidation), whereas exogenous solutes (such as atmospheric input to riverine sulfate) and biological solutes (such as soil CO2) show higher contents with increasing discharge. Besides, the biological carbon is the main driver of the chemostatic behaviors of total dissolved inorganic carbon (DIC). The forward model results show that carbonate weathering dominates the water chemistry, and the weathering rates are intensified during high flow period due to additional inputs of weathering agents, i.e., the biologic carbonic acid from dissolution of soil CO2, indicated by δ13CDIC. In addition, there exists the strong capacity of CO2 consumption that is heavily dependent on climatic variables such as precipitation and air temperature in this study river. Our study highlights the impact of climatic variability on solutes dynamics and chemical weathering and thus must be better addressed in C models under future climate change scenarios.

1. Introduction

CO2 consumption during rock chemical weathering by reaction with carbonic and other strong acids (such as sulfuric and nitric acids) are part of the important biogeochemical cycle of carbon and therefore act on regulating the climate on Earth, even on shorter timescales [1,2,3]. Numerous studies have focused on chemical weathering and CO2 consumption in carbonate-dominated catchments to understand local and even global carbon cycles [3,4]. Current estimation of global CO2 consumption by rock weathering varies from 0.1 to 0.44 Gt C a−1 [4,5]. These estimates have some uncertainty, largely due to the spatial variations (such as lithology, soil development, vegetation, precipitation, temperature, anthropogenic activity, etc.), which are inevitable on the continent [6]. Concerning the spatial variations in weathering flux and global CO2 consumption flux, for example, a long-term monitoring system called the Hydrological Benchmark Network (HBN) was established by the United States Geological Survey (USGS) to assess and quantify the human influence on 59 study sites across the U.S. [7]. Subsequently, a temporal rather than a spatial approach may be possible to obtain a stronger correlation between weathering flux and climate.
Solutes’ C-Q relationships in various catchments have been explored in the past decades [2,8,9,10,11,12,13,14,15,16,17] and can represent the integration of hydrological and biogeochemical responses of catchments for understanding riverine solute source, transport, and reaction [17]. The slope (b) of a power-law function [14] and the ratio of the C-Q coefficient of variation (CVC/CVQ) [18] have been proposed to evaluate the C-Q patterns to identify functional linkages between catchment hydrology and biogeochemistry. When b =−1 represents decreasing solute content with increasing discharge [14], this would support dilution behaviors where the solute mass does not increase proportionally to the increasing discharge, whereas positive b indicates increasing solute content with increasing discharge [19] and supports flushing behaviors. A solute is typically characterized as source-limited if it dilutes, whereas it is defined as transport-limited if it shows flushing behavior [20]. Thompson et al. [18] emphasized the importance of CVC/CVQ, which is to facilitate a more nuanced interpretation of C-Q relationships, particularly when b ≈ 0. Because it is related to the “chemostatic” behavior [14] or the “biogeochemical stationarity” [21], this implies that solute content shows a negligible variability. Based on quantitative metrics that were reported by Musolff et al. [19], chemostatic behavior yielded as -0.2 < b < 0.2 and CVC/CVQ < 0.5. In contrast, chemodynamic behavior (b ≈ 0, CVC/CVQ > 1) is a discharge-independent status, indicating dissolved solute content is not controlled by Q.
This study contributes to this line of research to investigate a high-frequency sampling survey in the Liujiang River catchment draining through the carbonate-dominated area, which features a warm subtropical climate. We focused on temporal research to (1) explore the behaviors of riverine solutes in a hydrological year by means of C-Q relations; (2) understand the hydrological and the biogeochemical responses of chemical weathering, CO2 consumption, dissolved carbon, and sulfur dynamics in a typical karst river; (3) trace water, riverine sulfate, and dissolved inorganic carbon (DIC) sources and estimate their contributions constrained by stable isotopic tracers in the study catchment area under various climatic conditions.

2. Materials and Methods

2.1. Study Area

The Liujiang River is a first-order tributary of the Xijiang River consisting of Pearl catchment in southern China (Figure 1). It originates from the village Lang in Guizhou Province and flows through Guizhou, Guangxi and Hunan Provinces, with 72% of its drainage area in the Guangxi Province; the drainage area is 58,270 km2. The main channel length is 1121 km. It is a mountainous watershed with high mountains in the north and a high elevation in the northwest, whereas, in the southern and the southeast areas, the elevations are relatively low. There are six land use types, with average coverage ratios as follows: forestland (64.9%) > cropland (18.7%) > grassland (18.1%) > urban land (14.5%) > water (0.8%) > unused land (0.02%). The Liujiang River catchment is exposed by a subtropical humid under monsoonal climate with a mean annual precipitation of 1800 mm. It is in the center of the storm zone of the Guangxi Province with frequent storms, and 59 disastrous flooding events have been recorded in the past 400 years since 1488 [22]. There are no significant reservoirs to influence flood discharge in the study catchment. Lithologically, the Precambrian metamorphic rocks and the quaternary fluvial sediments are distributed in the whole Xijiang River catchment (Figure 1). Specifically, carbonate rocks (limestone and dolomite) and coal-bearing formations generally enriched in sulfides are widely distributed in the upper-middle reaches. Schist, gneiss and granite are exposed in the middle-lower reaches. Shale and red sandstone are distributed in the source area and are fragmentarily intercalated in the middle catchment area. Minor evaporites are scattered in the Xijiang River catchment, but a salt-bearing stratum has not been found in this area [1,23,24]. Karst topography is well-developed in the study catchment.

2.2. Sampling and Analysis

The sampling site was located at the outlet of the Liujiang River (Figure 1), approximately 29 km away from the mainstream of the Xijiang River. River water samples for chemical and isotopic analyses were collected monthly from October 2013 to September 2014 (Table S1). Additional samples were collected in the high flow season, covering hydrological variations in this period. Water samples were collected from a boat in the middle of the river. Alkalinity was determined using 0.02 M HCl titration within 24 hours. Samples were filtered through 0.45 μM cellulose-acetate membrane paper and then were further separated into two parts; one for anions (Cl, SO42− and NO3) determined by ionic chromatography with a precision of 5% and the other for major cations (K+, Na+, Ca2+ and Mg2+) and Si, which were acidified to pH ≤ 2 with ultra-purified HNO3 and then determined by inductively coupled plasma-optical emission spectrometry (ICP-OES) with precisions better than 3%.
For the δ13CDIC analyses, based on the method of Li et al. [25], 15 ml aliquots of water samples were injected into vacuum glass bottles pre-filled with 2 ml 85% phosphoric acid and a magnetic stirrer bar. The samples were heated at 50 ℃ to extract CO2 in a vacuum line and transferred cryogenically into tubes. The values of δ13CDIC were measured by Finnigan MAT 252 mass spectrometer and were expressed in as permil deviation with reference to a standard (VPDB), with a precision of 0.1‰. The measurement of δ13CDIC was conducted in the State Key Laboratory of Environmental Geochemistry, the Institute of Geochemistry, Chinese Academy of Science. Riverine sulfate was precipitated as BaSO4 through adding excess BaCl2 solution after the water was acidified using HCl for isotopic measurements of sulfate. Then, the precipitate was filtered, washed, and dried. The values of δ34SSO4 and δ18OSO4 were determined using elemental analysis-isotope ratio mass spectrometry (EA-IRMS) and reported using δ notation relative to the Vienna Canyon Diablo Troilite (V-CDT) with precision better than 0.2‰ and the Vienna Standard Mean Ocean Water (V-SMOW) in permil with precision better than 0.5‰, respectively. The measurement of S and O isotopes of riverine sulfate was carried out at the Institute of Geographic Sciences and Natural Resources Research, Chinese Academy of Sciences. Daily water discharge data (m3/s) were obtained online from the Ministry of Water Resources (

3. Results

3.1. Hydrochemistry

Liujiang River water is mildly alkaline, with pH value ranging from 7.5 to 8.1. Electrical conductivity (EC) value varies from 148 to 229 μS/cm, with an average of 191. Total dissolved solid (TDS = Ca2+ + Mg2+ +Na+ + K+ HCO3 + SO42− + Cl + NO3 + SiO2, mg/L) of river varies from 128 mg/L to 224 mg/L, with a mean value of 163 mg/L for the study river, which is higher than the world average value of 97 mg/L [16]. The total cationic charge (TZ+ = K+ + Na+ + Ca2+ + Mg2+) and the total dissolved anionic charge (TZ = HCO3 + Cl + NO3 + SO42−) are well balanced within all NICB (Normalized Ionic Charge Balance) (NICB = (TZ+ − TZ) × 100%/(TZ+ + TZ)) below 5%. Similar to the rivers of Beipan and Nanpan in the upper reaches of the Xijiang River [1], Ca2+ and Mg2+ are dominant cations, while HCO3 and SO42- are the dominant anions, indicating that those waters are of karstic type. The mean contents of major cations are as follows: Ca2+ (806 μmol/L) > Mg2+ (185 μmol/L) > Na+ (111 μmol/L) > K+ (28 μmol/L). The mean contents of major anions are as follows: HCO3 (1612 μmol/L) > SO42− (125 μmol/L) > Cl (110 μmol/L) > NO3 (83 μmol/L). Contents of Cl, NO3, K+, and Na+ are relatively low.

3.2. δ34SSO4, δ18OSO4, and δ13CDIC Values

In the study river, the isotopic compositions of riverine sulfate show a narrow range for δ34SSO4 value from −0.5‰ in the high flow season to −0.1‰ in the low flow season, with a mean value of −0.4‰; for δ18OSO4, the corresponding range is 3.9‰–10.1‰ with a mean value 6.8‰, showing a distinct temporal variation. More depleted δ18OSO4 values are observed in the high flow season relative to those in the low flow season for the study river. The S and O isotopic compositions of sulfate in this study are in agreement with previous studies [26].
In order to calculate the partial pressure of CO2 (pCO2), we used the temperature dependence of thermodynamic constants [27]. The pCO2 ranges from 846 μatm in the high flow season to 3999 μatm in the low flow season with a mean value of 1612 μatm in river water, two to eleven times higher than that of the atmosphere (349 μatm). The δ13CDIC values range from −16.2‰ in the low flow season to −8.0‰ in the high flow season, with an average value of −12.9‰, also showing a clear temporal change.

4. Discussion

4.1. Solute Content-Discharge (C-Q) Relationship

In this study river, the slopes (b) are negative, and CVC/CVQ < 0.5 for weathering products such as Ca2+, Mg2+, HCO3, Na+, K+, SO42−, and Cl signal an inverse relationship between solute content and discharge and indicate dilution, which is common for geogenic solutes, as shown in Figure 2 and Figure 3. Geogenic solutes from carbonate weathering (such as Ca2+, Mg2+, and HCO3) show near chemostatic behavior, which can be attributed to the fast kinetics of carbonate weathering processes [12,28]. Na+ exhibits the strongest dilution pattern among all weathering solutes, with a more negative b and lower CVC/CVQ values. Na+ is mainly sourced from silicate weathering, implying that silicate weathering is more sensitive to various hydrologic conditions relative to carbonate weathering (indicated by Ca2+). Except silicate-sourced weathering, K+ is generally considered to be controlled by soil in water flow with cation exchange [29]. Hence, K+ can be considered a biological solute, especially during most storms with large amounts of soil water inputs [17]. As with K+, SO42− and Cl present similar dilution and chemostatic behaviors, which can be attributed to the geogenic and the exogenous sources. Exogenous sources are closely associated with soil water as well as atmospheric and anthropogenic inputs to these ions. Previous studies in this area demonstrated that sulfuric acid is also an important agent of rock weathering by using 87Sr/86Sr and δ13C [1,24]. The quantitative analysis of the sulfate source of this investigated river is discussed below. NO3 contents are the most variable relative to discharge, implying that exogenous anthropoge nic-printed sources (such as chemical fertilizer, soil organic nitrogen, manure, sewage waste, and atmospheric input) and relevant biogeochemical processes (assimilation, nitrification, denitrification) counteract the dilution effects. However, Si shows strong responses to increasing discharge, which could indicate that, as a result of weathering, Si can accumulate in the weathered zone. Thus, during intensive rainfall, it can be washed out from this zone into surface water [30,31,32]. Moreover, biologically associated solutes such as DOC (dissolved organic carbon), TOC (total organic carbon), NH4+, and PO43− often yield positive slopes and show flushing behaviors [17,33], suggesting that the content variability of these biological solutes is minor relative to discharge. It was reported that contents of biological solutes are often linked to anthropogenic sources, influencing these solute flushing behaviors in forested and agricultural catchments, especially in extreme climate events [17,34]. Our results from plots of b versus CVC/CVQ < 0.5 are consistent with the general interpretation of biogeochemical source presented in the previous study catchment [12,17].

4.2. Response of Sulfur Source to Hydrological Variations

Riverine sulfate is generally derived from atmospheric precipitation, sulfide oxidation, evaporite dissolution, and anthropogenic inputs (such as coal mining and combustion). The chemical composition of river water is insufficient to distinguish dissolved SO42− from geologic and exogenous sources, but the combined values of δ34SSO4 and δ18OSO4 could potentially provide useful constraints to identify the sulfur sources [3,35,36].
Isotopic signatures of sulfur and oxygen are well preserved during the congruent dissolution of evaporites, yielding results of δ34SSO4 varying from 13‰ to 15‰ and δ18OSO4 from 14.5‰ to 32.5‰ [37,38]. The δ34SSO4 values exceed 20‰ along with high contents of Ca2+ and SO42- in the shallow groundwater of the North Chinese Plain, which are associated with the evaporites (such as gypsum) dissolution [39]. The oxidative weathering of sulfide, which provides riverine sulfate, usually produces a more negative δ34SSO4 value; meanwhile, typical δ18OSO4 values of reduced sulfur oxidation vary from −5‰ to 4‰ [40], which is consistent with the values of δ34SSO4 and δ18OSO4 in the studied river water samples. In the Wujiang River, the oxidation of sulfides (averaging 73%) contributes most of the riverine sulfate [3]. Additionally, Turchyn et al. [35] reported that the headwaters of the Marsyandi River exhibit light δ34SSO4 and δ18OSO4, which can be attributed to the anoxic weathering of pyrite via Fe3+. Southern China is also one of the regions that is most affected by acid rain contributed by high sulfur-content coal combustion. Li et al. [41] proved that the source of dissolved riverine SO42− in the Jialing River is likely to be due to high S content coal combustion and oxidation of sulfides during the weathering of coal-containing strata. The δ34SSO4 values of rainwater in Guiyang City are reported to have an average of 4.6 ± 5.0‰ [42]. The δ18OSO4 values of atmospheric precipitation are reported to be from 7‰ to 17‰ [40]. The δ18OSO4 of the Liujiang River averages 6.8‰, which shows the dominant contribution of atmospheric input to sulfate in the river water. As indicated by diagrams of δ34SSO4 versus δ18OSO4 in the Liujiang River (Figure 4), riverine sulfate is mainly sourced from three major sources, including atmospheric precipitation, sulfide oxidation, and evaporites. Although a potential contribution from anthropogenic input can affect the sulfur levels [43], previous related works demonstrated that anthropogenic input only contributes a small fraction in the chemical weathering processes in the study area [23,24,44]; hence, the anthropogenic input to riverine sulfate can be ignored.
According to the discussion above regarding the sulfur sources in the Liujiang River, for the δ34SSO4 of the river water, a balanced equation could be calculated based on the following equation:
δ34S SO4 riv = Fat × δ34S SO4 at + Fsul × δ34S SO4 sul + Fgyp × δ34S SO4 gyp
Fat + Fsul + Fgyp = 1
where Fat, Fsul, and Fgyp are the corresponding relative contributions of SO42- from atmospheric precipitation, oxidation of sulfide, and gypsum input. The end-members can be assigned as follows: δ34SSO4 at = 1.4‰, δ34SSO4 sul = −13‰, and δ34SSO4 gyp = 25.7‰. Specific analysis can be found in related studies [46]. The fractions of SO42- contributed by the three end-members to the Liujiang River were estimated by using the IsoSource (v1.3, program with an increase of 1.0% and a mass balance tolerance of 0.5%. From Figure 5, it can be seen that atmospheric precipitation (averaging 52%) and the oxidation of sulfide (averaging 35%) are the major sources of SO42− in the study river, followed by gypsum (averaging 13%). The values of Fsul and Fgyp contribute to riverine sulfate and show negative relationships with increasing discharge, indicating that these geological sulfate sources exhibit strong dilution behavior with respect to discharge change, while the Fat values show positive relationships with discharge changes. Such variations in hydrological connectivity can be attributed to the geogenic sulfate-rich groundwater predominant in the low flow season and greater contributions from an exogenous source, such as low content of atmospheric precipitation and soil water in the high flow season, which are the main drivers of the chemostatic behavior of total riverine sulfate responding to increasing discharge [17]. Therefore, these results suggest that the specific dual isotopic characteristics of riverine sulfate not only reflect the mixing of compositionally distinct end-members but play an important role in better understanding the hydrological variability of riverine sulfate sources in the studied watershed across multiple events and years.

4.3. Chemical Weathering and CO2 Consumption Are Affected by Climate Variability

Along with the comparison of similar geological backgrounds (predominantly carbonates) from world rivers, good relationships are observed between Ca2+/Na+ vs. HCO3/Na+ (Figure 6a) during a hydrological year in the study river. All river waters fall on a line showing the mixing between carbonate and silicate end-members. River water samples contain more carbonate signature in the high flow conditions than those in the low flow conditions, which can be attributed to, as previously discussed, the stronger chemostatic behavior of carbonates weathering (indicated by Ca2+) than silicates weathering (indicated by Na+). As Figure 6b shows, the water chemistry of the studied river is attributed to carbonate weathering involving not carbonic acid but sulfuric acid, which can be mainly sourced from atmospheric precipitation and sulfide oxidation, as analyzed above (see Section 4.2). For the investigated river, it is worth noting that Ca2+/Na+, HCO3/Na+, and SO42−/Na+ molar ratios of river water samples are also positively correlated with temperature, suggesting that, in addition to discharge, the temperature may be another variable that is usually and highly correlated with chemical weathering, implying that there may be a negative feedback between climate conditions and chemical weathering that could help in regulating atmospheric CO2 [2,28,47].
Based on the mass budget equations, a forward model is employed to quantify the relative contribution of different sources to the dissolved ions in the river [4,24], which were reported in the related studies [45]. In total, the dissolved ions are dominated by carbonate weathering, accounting for a 61% average for the investigated river, which is followed by the average contribution of atmospheric precipitation (17%), anthropogenic input (8%), sulfide oxidation (7%), gypsums (4%), and silicate weathering (2%) in the Liujiang River (Figure 7). For anthropogenic input, the contribution percentage generally varies from 6% to 11%. There is an increasing proportional contribution from atmospheric precipitation responding to increasing discharge, suggesting the dilution effect. The proportion from sulfide oxidation and gypsums responding to discharge changes is constant with the behavior of their sulfate geogenic sources in the study river (see above Section 4.2). The proportion from the contribution of carbonate weathering not only shows a chemostatic behavior in respect of discharge changes but varies with a similar tendency as the water temperature change. These can be attributed to, under high temperature and discharge conditions, hydrological flushing of subsurface materials that could further induce the water–rock interaction [28], thus leading to the high intensity of carbonate weathering by reacting with soil CO2 and plant biological processes in the warm-wet environment [25]. Hence, relative to silicate weathering, carbonate weathering shows a stronger chemostatic behavior to respond with increasing discharge, while silicate weathering has more sensitivity to respond with increasing discharge, which is in agreement with the observations reported in climatic-impacted world rivers [9,12,28,48].
The CO2 consumption fluxes of silicate weathering (FCO2sil) and carbonate weathering (FCO2carb) are deducted from the sulfuric acid consumed by silicate and carbonate weathering, respectively. The total CO2 consumption flux (FCO2 = FCO2sil + FCO2carb) in the Liujiang River ranges from 7.7 kg/day/km2 to 237.8 kg/day/km2, averaging 95.4 kg/day/km2, which is slightly higher than the values from Xu and Liu [24]. Meanwhile, both discharge and temperature are positively correlated with chemical weathering, as indicated in Figure 8. In the low flow season, when discharge is < 2000 m3/s while temperature covers a wide range of change (8.5–29.5 ℃), FCO2 is more sensitive to variations in temperature than discharge; on the other hand, in the high flow season with high temperature, the discharge is likely to be a dominant driver in transporting the chemical weathering materials and stimulating the chemical weathering intensity by enhancing the available water–rock reaction surface area [2]. The observed positive relation between CO2 consumption and climatic conditions in the study river is consistent with the Loch Vale River [2], the Xijiang River [12], and other relative studies that used a spatial approach to investigate impacts on CO2 consumption flux by chemical weathering [4,5]. The results from this study have important implications in light of regulations for CO2 in the air; if discharge and temperature increase in response to climate change, CO2 consumption flux by chemical weathering may respond similarly, providing a negative feedback on greenhouse CO2 content.

4.4. Riverine Carbon Dynamic in Hydrological Variation

Dissolved inorganic carbon represents the largest fraction of the annual fluvial carbon flux to ocean, more than 80% in the Xijiang River [12]. Riverine DIC is mainly sourced from soil CO2, carbonate dissolution, and atmospheric CO2. Due to the high pCO2 in the study river, the contribution of atmospheric CO2 is not considered. Soil CO2, in situ biodegradation, and photosynthesis are the primary drivers of the pCO2 in river water [25,49,50]. Due to the relatively low DOC content and the few aquatic plants in the study catchment, the contributions of biodegradation and photosynthesis to pCO2 could be ignored. Thus, soil CO2 should be a dominant control on pCO2 content. As shown in Figure 9a, the pCO2 contents yield a power-law dilution effect and chemostatic behavior in responding to discharge variation. The dilution signals for pCO2 contents could result from contributions of high-content soil CO2 in the low flow conditions that become increasingly exhausted in the high flow conditions, while the chemostatic behavior for pCO2 contents with respect to increasing discharge should be attributed to exogenous soil CO2 discharged into river water, especially in extreme climatic events such as storms, when the exogenous soil CO2 counteracts the dilution effects [12,25].
The soil CO2 decreases δ13CDIC values in the study river, as indicated in Figure 9b, with δ13CDIC values showing a similar behavior to pCO2 contents responding to hydrological variations. Therefore, δ13CDIC can be used to constrain the riverine DIC sources. The major vegetation in the study catchment is C3 plants with a mean δ13CDIC value of −27‰ [1]. After considering isotopic fractionation 4.4‰ [51], the δ13CDIC of soil water should be −22.6‰. Carbonate carbon has a mean value of 0‰. Therefore, the proportions of two DIC sources are calculated as follows:
δ13CDIC riv = FCO2× δ13CCO2 + (1-FCO2) × δ13CCarb
where FCO2 is the proportion of soil CO2, and δ13CDIC riv, δ13CCO2, and δ13CCarb are δ13C values of river, soil CO2, and carbonate dissolution, respectively. Based on the mixing model, 29%–65% (averaging 43%) of the DIC is sourced from carbonate dissolution, while 35%-71% (averaging 57%) of the DIC is from soil CO2. As presented in Figure 9c,d, the contributions of carbonate dissolution to riverine DIC show chemostatic behavior responding to increasing discharge, while the contribution of soil CO2 presents a linear relationship with increasing discharge, implying that soil CO2 is a dominant driver of the chemostatic behavior of total riverine DIC with increasing discharge, which is in agreement with previous studies [25]. Therefore, under high temperature and discharge conditions, rainwater infiltrates into the soil and flushes excessive biological solutes, including soil CO2 into the river, leading to increasing the amounts of soil CO2 to total DIC in the high flow season compared to those in the low flow season.
Our calculation indicates that fluvial DIC content and its carbon isotope primarily reflect the mixing of compositionally distinct riverine DIC sources and biogeochemical processes in response to hydrological changes. These results are important, as they clearly show that physical and biological processes affect the DIC pool with respect to hydrological variations, and the δ13CDIC can be used to constrain carbon evolution. The riverine dissolved carbon dynamic in response to hydrological variations can be considered a positive feedback in the geological and the biological carbon cycle and a negative feedback in the acidification of ocean by the absorption of atmospheric CO2. Therefore, investigations of long-term carbon dynamics within a single catchment and across multiple catchments incorporating data from multiple storm events over many years should be campaigned.

5. Conclusions

According to a high-frequency variation in riverine solutes contents and multiple sable isotopic tracers (carbon and sulfur isotopes), this study investigated chemical weathering, CO2 consumption, and riverine solute sources and their contributions impacted by climatic variabilities in the typical monsoonal river. The variability of solute content is generally much smaller than that of climatic variability, which would support a similar chemostatic behavior. The main reason can be attributed to carbonates dissolution and biological processes. In this study catchment, carbonate weathering controls the major solute source and shows strong chemostatic behavior owing to the rapid dissolution characteristics. On the other hand, along with high temperature, primary production is increased in the high flow season, leading to the influx of δ13C-depleted soil CO2 being the main driver controlling the riverine DIC dynamics. Moreover, the positive correlations between CO2 consumption fluxes and discharge and temperature provide a negative feedback on the greenhouse CO2 in the atmosphere. Quantifying the strength of the feedback between CO2 consumption fluxes and climate change in a range of catchments needs to be addressed in future studies.

Supplementary Materials

The following are available online at, Table S1: The hydrochemistry and stable isotopes for the Liujiang River.

Author Contributions

Conceptualization, J.L., H.D. and M.X.; Formal analysis, H.D. and M.X.; Funding acquisition, J.L.; Investigation, M.X., Z.-Y.X., Y.W., J.-T.P., H.W. and X.-D.W.; Methodology, L.Z.; Software, Z.-H.S.; Writing—original draft, J.L. All authors have read and agreed to the published version of the manuscript.


This work was supported financially by National Natural Science Foundation of China (Grant Nos. 41803022, 41964005), the Guizhou Science and Technology Department Fund (Grant Nos. [2013]3118, [2019]1043), Guizhou Education Department Fund (Grant Nos. [2018]139, [2018]161) and scientific platform talent project of Guizhou University of Finance and Economics (Grant No. [2018]5774-029).

Conflicts of Interest

The authors declare no conflict of interest.


  1. Li, S.L.; Calmels, D.; Han, G.L.; Gaillardet, J.; Liu, C.Q. Sulfuric acid as an agent of carbonate weathering constrained by δ13CDIC: Examples from Southwest China. Earth Planet. Sci. Lett. 2008, 270, 189–199. [Google Scholar] [CrossRef]
  2. Clow, D.W.; Mast, M.A. Mechanisms for chemostatic behavior in catchments: Implications for CO2 consumption by mineral weathering. Chem. Geol. 2010, 269, 40–51. [Google Scholar] [CrossRef]
  3. Li, C.; Ji, H. Chemical weathering and the role of sulfuric and nitric acids in carbonate weathering: Isotopes (13C,15N,34S, and 18O) and chemical constraints. J. Geophy. Res. Biogeosci. 2016, 121, 1288–1305. [Google Scholar] [CrossRef] [Green Version]
  4. Gaillardet, J.; Dupré, B.; Louvat, P.; Allègre, C.J. Global silicate weathering and CO2 consumption rates deduced from the chemistry of large rivers. Chem. Geol. 1999, 159, 3–30. [Google Scholar] [CrossRef]
  5. Amiotte Suchet, P.; Probst, J.L.; Ludwig, W. Worldwide distribution of continental rock lithology: Implications for the atmospheric/soil CO2 uptake by continental weathering and alkalinity river transport to the oceans. Global Biogeochem. Cycl. 2003, 17, 1038. [Google Scholar] [CrossRef] [Green Version]
  6. Kump, L.R.; Brantley, S.L.; Arthur, M.A. Chemical weathering, atmospheric CO2, and climate. Annu. Rev. Earth Planet. Sci. 2000, 28, 611–667. [Google Scholar] [CrossRef] [Green Version]
  7. Leopold, L.B. A National Network of Hydrologic Bench Marks, Geological Survey Circular 460-B; United States Department of the Interior, Geological Survey: Washington, DC, USA, 1962.
  8. Zhong, J.; Li, S.L.; Cai, H.M.; Yue, F.J.; Tao, F.X. The Response of Carbon Geochemistry to Hydrological Events within an Urban River, Southwestern China. Geochem. Int. 2018, 56, 462–473. [Google Scholar] [CrossRef]
  9. Zhong, J.; Li, S.L.; Tao, F.X.; Yue, F.J.; Liu, C.Q. Sensitivity of chemical weathering and dissolved carbon dynamics to hydrological conditions in a typical karst river. Sci. Rep. 2017, 7, 42944. [Google Scholar] [CrossRef] [Green Version]
  10. Zhong, J.; Li, S.L.; Ding, H.; Lang, Y.; Maberly, S.C.; Xu, S. Mechanisms controlling dissolved CO2 over-saturation in the Three Gorges Reservoir area. Inland Waters 2018, 8, 148–156. [Google Scholar] [CrossRef] [Green Version]
  11. Zhong, J.; Li, S.L.; Tao, F.X.; Ding, H.; Liu, J. Impacts of hydrologic variations on chemical weathering and solute sources in the Min River basin, Himalayan-Tibetan region. Environ. Sci. Pollut. Res. 2017, 24, 19126–19137. [Google Scholar] [CrossRef] [PubMed]
  12. Zhong, J.; Li, S.L.; Liu, J.; Ding, H.; Sun, X.L.; Xu, S.; Wang, T.J.; Ellam, R.M.; Liu, C.Q. Climate variability controls on CO2 consumption fluxes and carbon dynamics for monsoonal rivers: Evidence from Xijiang River, Southwest China. J. Geophys. Res. Biogeosci. 2018, 123, 2553–2567. [Google Scholar] [CrossRef] [Green Version]
  13. Calmels, D.; Galy, A.; Hovius, N.; Bickle, M.; West, A.J.; Chen, M.C.; Chapman, H. Contribution of deep groundwater to the weathering budget in a rapidly eroding mountain belt, Taiwan. Earth Planet. Sci. Lett. 2011, 303, 48–58. [Google Scholar] [CrossRef]
  14. Godsey, S.E.; Kirchner, J.W.; Clow, D.W. Concentration-discharge relationships reflect chemostatic characteristics of US catchments. Hydrol. Process. 2009, 23, 1844–1864. [Google Scholar] [CrossRef]
  15. Kim, H.; Dietrich, W.E.; Thurnhoffer, B.M.; Bishop, J.K.B.; Fung, I.Y. Controls on solute concentration-discharge relationships revealed by simultaneous hydrochemistry observations of hillslope runoff and stream flow: The importance of critical zone structure. Water Resour. Res. 2017, 53, 1424–1443. [Google Scholar] [CrossRef] [Green Version]
  16. Li, S.Y.; Bush, R.T. Changing fluxes of carbon and other solutes from the Mekong River. Sci. Rep. 2015, 5, 16005. [Google Scholar] [CrossRef] [Green Version]
  17. Rose, L.A.; Karwan, D.L.; Godsey, S.E. Concentration-discharge relationships describe solute and sediment mobilization, reaction, and transport at event and longer timescales. Hydrol. Process. 2018, 32, 2829–2844. [Google Scholar] [CrossRef]
  18. Thompson, S.E.; Basu, N.B.; Lascurain, J.; Aubeneau, A.; Rao, P.S.C. Relative dominance of hydrologic versus biogeochemical factors on solute export across impact gradients. Water Resour. Res. 2011, 47, 10. [Google Scholar] [CrossRef]
  19. Musolff, A.; Schmidt, C.; Selle, B.; Fleckenstein, J.H. Catchment controls on solute export. Adv. Water Resour. 2015, 86, 133–146. [Google Scholar] [CrossRef]
  20. Duncan, J.M.; Band, L.E.; Groffman, P.M. Variable nitrate concentration-discharge relationships in a forested watershed. Hydrol. Process. 2017, 31, 1817–1824. [Google Scholar] [CrossRef]
  21. Basu, N.B.; Destouni, G.; Jawitz, J.W.; Thompson, S.E.; Loukinova, N.V.; Darracq, A.; Zanardo, S.; Yaeger, M.; Sivapalan, M.; Rinaldo, A.; et al. Nutrient loads exported from managed catchments reveal emergent biogeochemical stationarity. Geophys. Res. Lett. 2010, 37, 23. [Google Scholar] [CrossRef]
  22. Chen, Y.; Li, J.; Wang, H.; Qin, J.; Dong, L. Large-watershed flood forecasting with high-resolution distributed hydrological model. Hydrol. Earth Syst. Sci. 2017, 21, 735–749. [Google Scholar] [CrossRef] [Green Version]
  23. Gao, Q.Z.; Tao, Z.; Huang, X.K.; Nan, L.; Yu, K.F.; Wang, Z.G. Chemical weathering and CO2 consumption in the Xijiang River basin, South China. Geomorphology 2009, 106, 324–332. [Google Scholar] [CrossRef]
  24. Xu, Z.F.; Liu, C.Q. Water geochemistry of the Xijiang basin rivers, South China: Chemical weathering and CO2 consumption. Appl. Geochem. 2010, 25, 1603–1614. [Google Scholar] [CrossRef]
  25. Li, S.L.; Liu, C.Q.; Li, J.; Lang, Y.C.; Ding, H.; Li, L. Geochemistry of dissolved inorganic carbon and carbonate weathering in a small typical karstic catchment of Southwest China: Isotopic and chemical constraints. Chem. Geol. 2010, 277, 301–309. [Google Scholar] [CrossRef]
  26. Han, G.L.; Tang, Y.; Wu, Q.X.; Liu, M.; Wang, Z.R. Assessing Contamination Sources by Using Sulfur and Oxygen Isotopes of Sulfate Ions in Xijiang River Basin, Southwest China. J. Environ. Qual. 2019, 48, 1507–1516. [Google Scholar] [CrossRef] [PubMed]
  27. Plummer, L.N.; Busenberg, E. The solubilities of calcite, aragonite and vaterite in CO2–H2O solutions between 0 and 90 °C, and an evaluation of the aqueous model for the system CaCO3–CO2–H2O. Geochim. Cosmochim. Acta 1982, 46, 1011–1040. [Google Scholar] [CrossRef]
  28. Tipper, E.T.; Bickle, M.J.; Galy, A.; West, A.J.; Pomiès, C.; Chapman, H.J. The short term climatic sensitivity of carbonate and silicate weathering fluxes: Insight from seasonal variations in river chemistry. Geochim. Cosmochim. Acta 2006, 70, 2737–2754. [Google Scholar] [CrossRef]
  29. Boy, J.; Valarezo, C.; Wilcke, W. Water flow paths in soil control element exports in an Andean tropical montane forest. Eur. J. Soil Sci. 2008, 59, 1209–1227. [Google Scholar] [CrossRef]
  30. Asano, Y.; Uchida, T.; Ohte, N. Hydrologic and geochemical influences on the dissolved silica concentration in natural water in a steep headwater catchment. Geochim. Cosmochim. Acta 2003, 67, 1973–1989. [Google Scholar] [CrossRef]
  31. Dobrzyński, D. Silica origin and solubility in groundwater from the weathered zone of sedimentary rocks of the Intra-Sudetic Basin, SW Poland. Acta Geol. Pol. 2005, 55, 445–462. [Google Scholar]
  32. Wels, C.; Cornett, R.J.; Lazerte, B.D. Hydrograph separation: A comparison of geochemical and isotopic tracers. J. Hydrol. 1991, 122, 253–274. [Google Scholar] [CrossRef]
  33. Diamond, J.S.; Cohen, M.J. Complex patterns of catchment solute-discharge relationships for coastal plain rivers. Hydrol. Process. 2018, 32, 388–401. [Google Scholar] [CrossRef]
  34. Siwek, J.; Siwek, J.P.; Żelazny, M. Environmental and land use factors affecting phosphate hysteresis patterns of stream water during flood events (Carpathian Foothills, Poland). Hydrol. Process. 2013, 27, 3674–3684. [Google Scholar] [CrossRef]
  35. Turchyn, A.V.; Tipper, E.T.; Galy, A.; Lo, J.K.; Bickle, M.J. Isotope evidence for secondary sulfide precipitation along the Marsyandi River, Nepal, Himalayas. Earth Planet. Sci. Lett. 2013, 374, 36–46. [Google Scholar] [CrossRef]
  36. Li, S.L.; Chetelat, B.; Yue, F.J.; Zhao, Z.Q.; Liu, C.Q. Chemical weathering processes in the Yalong River draining the eastern Tibetan Plateau, China. J. Asian Earth Sci. 2014, 88, 74–84. [Google Scholar] [CrossRef]
  37. Goldberg, T.; Poulton, S.W.; Strauss, H. Sulphur and oxygen isotope signatures of late Neoproterozoic to early Cambrian sulphate, Yangtze Platform, China: Diagenetic constraints and seawater evolution. Precambrain Res. 2005, 137, 223–241. [Google Scholar] [CrossRef]
  38. Strauss, H. The isotopic composition of sedimentary sulfur through time. Palaeogeogr. Palaeoclimatol. Palaeoacol. 1997, 132, 97–118. [Google Scholar] [CrossRef]
  39. Li, X.; Zhou, A.; Gan, Y.; Yu, T.; Wang, D.; Liu, Y. Controls on the δ34S and δ18O of dissolved sulfate in the Quaternary aquifers of the North China Plain. J. Hydrol. 2011, 400, 312–322. [Google Scholar] [CrossRef]
  40. Krouse, H.R.; Mayer, B. Sulphur and oxygen isotopes in sulphate. In Environmental Tracers in Subsurface Hydrology; Cook, P.G., Herczeg, A.L., Eds.; Kluwer Academic: Boston, MA, USA, 2000. [Google Scholar]
  41. Li, X.-D.; Liu, C.-Q.; Liu, X.-L.; Bao, L.-R. Identification of dissolved sulfate sources and the role of sulfuric acid in carbonate weathering using dual-isotopic data from the Jialing River. Southwest China. J. Asian Earth Sci. 2011, 42, 370–380. [Google Scholar] [CrossRef]
  42. Xiao, H.Y.; Liu, C.Q. Sources of nitrogen and sulfur in wet deposition at Guiyang, southwest China. Atmos. Environ. 2002, 36, 5121–5130. [Google Scholar] [CrossRef]
  43. Raymond, P.A.; Oh, N.H. Long term changes of chemical weathering products in rivers heavily impacted from acid mine drainage: Insights on the impact of coal mining on regional and global carbon and sulfur budgets. Earth Planet. Sci. Lett. 2009, 284, 50–56. [Google Scholar] [CrossRef]
  44. Li, C.; Li, S.L.; Yue, F.J.; Liu, J.; Zhong, J.; Yan, Z.F.; Zhang, R.C.; Wang, Z.J.; Xu, S. Identification of sources and transformations of nitrate in the Xijiang River using nitrate isotopes and Bayesian model. Sci. Total Environ. 2019, 646, 801–810. [Google Scholar] [CrossRef] [PubMed]
  45. Liu, J.; Li, S.L.; Chen, J.B.; Zhong, J.; Yue, F.J.; Lang, Y.C.; Ding, H. Temporal transport of major and trace elements in the upper reaches of the Xijiang River, SW China. Environ. Earth Sci. 2017, 76, 299. [Google Scholar] [CrossRef]
  46. Liu, J.; Li, S.L.; Zhong, J.; Zhu, X.T.; Guo, Q.J.; Lang, Y.C.; Han, X.K. Sulfate sources constrained by sulfur and oxygen isotopic compositions in the upper reaches of the Xijiang River, China. Acta Geochim. 2017, 36, 611–618. [Google Scholar] [CrossRef] [Green Version]
  47. Moon, S.; Chamberlain, C.P.; Hilley, G.E. New estimates of silicate weathering rates and their uncertainties in global rivers. Geochim. Cosmochim. Acta 2014, 134, 257–274. [Google Scholar] [CrossRef]
  48. Ollivier, P.; Hamelin, B.; Radakovitch, O. Seasonal variations of physical and chemical erosion: A three-year survey of the Rhone River (France). Geochim. Cosmochim. Acta 2010, 74, 907–927. [Google Scholar] [CrossRef]
  49. Barth, J.A.C.; Cronin, A.A.; Dunlop, J.; Kalin, R.M. Influence of carbonates on the riverine carbon cycle in an anthropogenically dominated catchment basin: Evidence from major elements and stable carbon isotopes in the Lagan River (N. Ireland). Chem. Geol. 2003, 200, 203–216. [Google Scholar] [CrossRef]
  50. Zou, J. Sources and Dynamics of Inorganic Carbon within the Upper Reaches of the Xi River Basin, Southwest China. PLoS ONE 2016, 11, e0160964. [Google Scholar]
  51. Cerling, T.E.; Solomon, D.K.; Quade, J.; Bowman, J.R. On the isotopic composition of carbon in soil carbon dioxide. Geochim. Cosmochim. Acta 1991, 55, 3403–3405. [Google Scholar] [CrossRef]
Figure 1. Map showing sampling location, geological background, digital elevation model (DEM), and land use types of the Liujiang River catchment.
Figure 1. Map showing sampling location, geological background, digital elevation model (DEM), and land use types of the Liujiang River catchment.
Water 12 00862 g001
Figure 2. Riverine dissolved solutes content–discharge relationships in the Liujiang River.
Figure 2. Riverine dissolved solutes content–discharge relationships in the Liujiang River.
Water 12 00862 g002
Figure 3. Plot of slope (b) versus CVC/CVQ for riverine dissolved solutes in the Liujiang River.
Figure 3. Plot of slope (b) versus CVC/CVQ for riverine dissolved solutes in the Liujiang River.
Water 12 00862 g003
Figure 4. A diagram of δ34SSO4 versus δ18OSO4 showing the riverine sulfate sources produce isotopically distinct sulfate in the Liujiang River [3,35,39,41,45].
Figure 4. A diagram of δ34SSO4 versus δ18OSO4 showing the riverine sulfate sources produce isotopically distinct sulfate in the Liujiang River [3,35,39,41,45].
Water 12 00862 g004
Figure 5. The fractions of riverine sulfate contributed by different three end-members (Fat, Fsul, and Fgyp) to the Liujiang River.
Figure 5. The fractions of riverine sulfate contributed by different three end-members (Fat, Fsul, and Fgyp) to the Liujiang River.
Water 12 00862 g005
Figure 6. Plots of (a) Ca2+/Na+ versus HCO3/Na+ and (b) Ca2+/Na+ versus SO42-/Na+ for the Liujiang River waters in a hydrological year [1,4,9,11,23].
Figure 6. Plots of (a) Ca2+/Na+ versus HCO3/Na+ and (b) Ca2+/Na+ versus SO42-/Na+ for the Liujiang River waters in a hydrological year [1,4,9,11,23].
Water 12 00862 g006
Figure 7. The contribution percentage of different end-members under various temperature and discharge conditions for the Liujiang River in a hydrological year.
Figure 7. The contribution percentage of different end-members under various temperature and discharge conditions for the Liujiang River in a hydrological year.
Water 12 00862 g007
Figure 8. Three-dimensional representation of FCO2, discharge, and temperature for the Liujiang River in a hydrological year.
Figure 8. Three-dimensional representation of FCO2, discharge, and temperature for the Liujiang River in a hydrological year.
Water 12 00862 g008
Figure 9. The power–law relationship between pCO2 and discharge (a). δ13CDIC values responding with discharge variations (b). The power–law relationship between DICcarb and discharge (c). The power–law relationship between DICCO2 and discharge (d).
Figure 9. The power–law relationship between pCO2 and discharge (a). δ13CDIC values responding with discharge variations (b). The power–law relationship between DICcarb and discharge (c). The power–law relationship between DICCO2 and discharge (d).
Water 12 00862 g009

Share and Cite

MDPI and ACS Style

Liu, J.; Ding, H.; Xiao, M.; Xu, Z.-Y.; Wei, Y.; Su, Z.-H.; Zhao, L.; Peng, J.-T.; Wang, H.; Wang, X.-D. Climatic Variabilities Control the Solute Dynamics of Monsoon Karstic River: Approaches from C-Q Relationship, Isotopes, and Model Analysis in the Liujiang River. Water 2020, 12, 862.

AMA Style

Liu J, Ding H, Xiao M, Xu Z-Y, Wei Y, Su Z-H, Zhao L, Peng J-T, Wang H, Wang X-D. Climatic Variabilities Control the Solute Dynamics of Monsoon Karstic River: Approaches from C-Q Relationship, Isotopes, and Model Analysis in the Liujiang River. Water. 2020; 12(3):862.

Chicago/Turabian Style

Liu, Jing, Hu Ding, Min Xiao, Zhu-Yan Xu, Yuan Wei, Zhi-Hua Su, Lei Zhao, Jiao-Ting Peng, Heng Wang, and Xiao-Dan Wang. 2020. "Climatic Variabilities Control the Solute Dynamics of Monsoon Karstic River: Approaches from C-Q Relationship, Isotopes, and Model Analysis in the Liujiang River" Water 12, no. 3: 862.

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop