Hydrogeochemistry and Acidic Property of Submarine Groundwater Discharge Around Two Coral Islands in the Northern South China Sea

Introduction

River inputs play an essential role in global water cycles and biogeochemical cycles. They transport water and large amounts of nutrients, such as nitrate, phosphate, and silicate, to support the estuaries’ high productivity and biodiversity. In addition to the river waters, there is also fresh groundwater discharging into the ocean through the seabed directly. This phenomenon is called submarine groundwater discharge (SGD) (Burnett et al., 2003; Bishop et al., 2017; Taniguchi et al., 2019). Taniguchi et al. (2019) defined SGD as “the flow of water through continental and insular margins from the seabed to the coastal ocean, regardless of fluid composition or driving force”, stating that islands typically have higher SGD, in terms of fluxes per unit area of landmass, than continents. According to this definition, the SGD includes both the freshwater and recirculated (or recharged) seawater.

Primarily due to difficulties in observations and measurements, there are not as many studies on SGD as there are on riverine systems. The amount of water fluxes of SGD is considerably high, accounting for 1–10% of the total riverine discharge (Burnett et al., 2001; Santos et al., 2021). However, the proportion of the nutrient flux of the SGD could be higher. This is because SGD water generally has a longer residual time than that of river water before entering the oceans, accumulating a more significant effect of organic matter decomposition; chemical weathering; and human activities, such as sewage inputs and fertilizer leakage. (Wang et al., 2018; Chen et al., 2019; Santos et al., 2021). Consequently, SGD water is usually high in nutrients but low in dissolved oxygen (DO) and pH (Wang et al., 2018). Coupling with the dissolution of minerals, such as CaCO₃, SGD water could also be high in dissolved inorganic carbon (DIC) and total alkalinity (TA) (Wang et al., 2018). Since the pre-industrial period, the oceans have been absorbing an increasing amount of human-released CO₂ from the atmosphere. Consequently, the pH, saturation state of calcite (Ω_Cal), and aragonite (Ω_Ara) are gradually decreasing with time. Such a process is called ocean acidification. Generally speaking, the pH of the surface ocean is around 8.25 on the NBS scale (or about 8.1 on the total scale), and the value is expected to have a 0.3 pH unit drop at the end of this century due to the increasing atmospheric CO₂ (Orr et al., 2005; Hoegh-Guldberg et al., 2007; Dore et al., 2009; Bates et al., 2014). It is well known that ocean acidification reduces the calcification rates of many marine organisms that use CaCO₃ as their skeleton. Indeed, SGD could be an acidity source for coastal oceans.

Previous studies have shown that the SGD is a vital source of nutrients in many coastal regions, but little information is available on its carbonate chemistry and the controlling factors. Using Taiwan as an example, a previous study showed that in the coastal region, there is a larger amount of inorganic carbon (such as carbon dioxide) brought in by the SGD than organic carbon produced by phytoplankton from the nutrients brought in by the SGD (Wang et al., 2018). The extra-inorganic carbon may eventually move to the atmosphere in the form of CO₂. That is, SGD is a source of CO₂ that ends up in the atmosphere. Studies have pointed out that the lower the Ω_Cal or Ω_Ara values, the lower the calcification rate of some marine organisms with calcium carbonate shells (Hoegh-Guldberg et al., 2007). Of note is that the Ω_Cal and Ω_Ara of SGD water could be lower than one (undersaturation) (Wang et al., 2018). In that case, CaCO₃ starts to dissolve. The Ω_ara value of the discharged submarine groundwater is anticipated to decrease from oversaturation to undersaturation with the increasing atmospheric CO₂ in Sanya Bay in the northern South China Sea (Wang et al., 2014). Understanding the hydrogeochemistry and carbonate chemistry of the SGD water is critical for examining and predicting the impact of human activities on the chemistry of SGD and on the coastal ecosystem, especially on coral reefs where the highest marine biodiversity exists.

This study aims to investigate the processes and factors controlling the hydrogeochemistry and the acidic property of the SGD water and groundwater of two isolated coral islands, Liuqiu Island (13 km off southwestern Taiwan) and Dongsha Island (located in the northern South China Sea, 420 km away from Liuqiu Island) (Figure 1). Liuqiu Island is a 4 km long and 2 km wide NW–SE elongated coral-reef island with an area of 6.8 km². The island has been raised at a rate of about 2 mm/year, mainly due to mud diapirism (Shih et al., 1991; Chen et al., 2014). Dongsha Island is a 2.8 km long and 0.9 km wide E–W coral reef island with an area of 1.8 km². It is the only reef island among a circular coral reef with a diameter of about 25 km, namely, the Dongsha Atoll. We collected water samples around Liuqiu Island and Dongsha Island. The carbonate chemistry and major ions of rainwaters, spring waters, and SGD waters were analyzed. Factors controlling the chemical weathering and the carbonate chemistry are discussed. This study is likely the first to examine the effect of the acidic property of SGD water on the biogenic carbonate spine of a sea urchin and a pteropod shell.

FIGURE 1

FIGURE 1. (A) Study areas and sampling locations of (B,C) Liuqiu Island and (D) Dongsha Island. The satellite image of Dongsha Atoll was taken from the National Geospatial-Intelligence Agency of the U.S. The maps were generated using Ocean Data View 5.0.0. Schlitzer, R., Ocean Data View, https://odv.awi.de, 2018.

Methods and Materials

Eight expeditions took place on 1987/9/26, 2017/7/13, 2017/9/25, 2019/12/11-13, 2020/6/15-19, 2020/9/17, 2020/12/3, and 2021/1/25 in Liuqiu Island. Four spring waters (S1-S4, Figure 1B) were sampled on 1987/9/26, and only the major ions were used in this study. For the remaining seven expeditions between 2017 and 2021, we regularly sampled the spring water (S5, Figures 1B,C) as well as the SGD waters and seawaters at the southern tip of Liuqiu Island (station A1, Figure 1B). Three expeditions took place on 2020/9/2, 2021/1/5, and 2021/1/11 in Dongsha Island (Figure 1D). Two groundwater samples were taken from two wells on 2020/9/2. Groundwater, SGD, and seawater samples were sampled around Dongsha Island on 2021/1/5. A groundwater sample was taken from a well, and two seawater samples were taken from the inner lagoon on 2021/1/11. Fifteen rainwater samples were sampled from two stations (R1 and R2) located in southwestern Taiwan (32 km away from Liuqiu Island) in 2020 on 4/6, 5/19, 5/20, 5/21 (two samples), 5/22 (three samples), 5/27 (two samples), 6/7, 7/15, 8/3, 8/4, and 8/26 (Figure 1A).

A hollow stainless steel needle with a total length of 0.5 m was inserted from the water into the seabed 0.2–1 m below the sea surface around the coasts of Liuqiu Island and Dongsha Island. The SGD waters were drawn using the needle and stored immediately in a plastic-made sampling bag to minimize the gases exchange between the water samples and air. Field water temperature, salinity (or conductivity), and DO were measured using a Hach HQ40 portable multimeter. DO was calibrated using H₂O-saturated air, and salinity was calibrated with the OSIL-produced International Association for the Physical Sciences of the Oceans (IAPSO) salinity standard seawater. Water samples were collected and poisoned with 0.05% saturated HgCl₂. Waters for pH, TA, DIC, and CH₄ measurements were stored in borosilicate glass bottles. Waters for nutrient measurements were filtered with a 0.45 μm Millex-HA syringe filter (MF-Millipore mixed cellulose ester membrane) and stored in PP bottles. TA was measured by Gran titration with an open-cell system using the Apollo-manufactured total alkalinity titrator (model: AS-ALK2). DIC was measured with an infrared detector using an Apollo-manufactured DIC analyzer (model AS-C6L). Both TA and DIC were calibrated against certified reference material for ocean CO₂ measurements provided by Dr. A.G. Dickson at the Scripps Institution of Oceanography Marine Physical Laboratory, University of California, San Diego. For the brackish water and seawater samples, pH on the total scale was measured using a spectrophotometer with meta-cresol purple at 25°C. For the freshwater samples, the pH on the NBS scale was measured with a glass electrode pH meter at 25°C. To compare the pH data on the same scale, we converted the pH on the total scale to the NBS scale. The differences in pH values of our samples between two scales (pH on the NBS minus pH on the total scale), determined using the CO₂ System Calculations Program version 2.3 (Pierrot et al., 2006), is as high as 0.16 at a salinity of 1.4 and as low as 0.14 at a salinity of 36.4. pH values reported in this study are on the NBS scale at 25°C.

Two SGD samples collected from Dongsha Island formed black precipitation when HgCl₂ was added for preservation. This could be due to the formation of HgS when HgCl₂ reacted with the H₂S, which is one of the gases that commonly exist in groundwater. The chemical reaction is as follows:

$H_2{S}_{\left(aq\right)}+HgC{l}_{2 \left(aq\right)}\to {\text{HgS}}_{\left(s\right)}+{2\text{HCl}}_{\left(aq\right)}$

Of note is that this reaction generates hydrochloric acid, further reducing the pH and TA of the water samples. Assuming all the black precipitation was HgS, using its weight, we corrected the changes in TA and pH due to the formation of HCl.

Nitrate plus nitrite, phosphate, and silicate were calibrated with the OSIL nutrient standards, and detailed information was given by Chen and Wang (2006). CH₄ was measured with the head-space equilibration technique (Weiss, 1981) using a gas chromatograph (Agilent 7,890) fitted with a flame ionization detector (FID). The primary standard was 1.16 ppmV CH₄ (MESA Specialty Gas, United States). The precision of repeated analysis of water samples was about ±3% in routine sample analysis. The CO₃²⁻, HCO₃⁻, and partial pressure of CO₂ (pCO₂) were calculated using the CO₂ System Calculations Program version 2.3 (Pierrot et al., 2006). The dissociation constants for the carbonate chemistry were taken from Millero (2010). Ω_Cal and Ω_Ara were calculated using the following equation:

$\frac{\left[C{a}^{2+}\right]\left[C{O}_3^{2-}\right]}{K_{sp}}$

where K_sp, the stoichiometric solubility product, was taken from Mucci (1983).

Major ions were analyzed for the spring waters collected at stations S1–S4 on 1987/9/26, the spring water collected at station S5 on 2020/12/3, and the rainwater collected at R1 on 2020/8/26. Cations of samples collected in 1987 were measured using the Dionex ion chromatography system (model: 2000i). Cl⁻ was determined using the mercury thiocyanate method (Florence and Farrar, 1971), SO₄²⁻ was determined using turbidimetric method (American Public Health Association, 1981), and HCO₃⁻ was calculated using the measured TA and pH. Major ions of water samples collected in 2020 were analyzed using ion chromatography at the Ultra Trace Industrial Safety Hygiene Laboratory of the SGS Taiwan Ltd. The results are shown in Table 1. For the remaining water samples, the Ca²⁺ used to calculated the Ω_Cal and Ω_Ara values was estimated using the linear correlation with the spring water at S5 (Ca²⁺ = 1931 μmol/kg at a salinity of 0.42; see Table 1) mixed with the standard seawater (Ca²⁺ = 10,282 μmol/kg at a salinity of 35 (Millero et al., 2008)) as endmembers.

TABLE 1

TABLE 1. Conductivity, salinity, and the major ions of the spring waters at stations S1–S5 and the rainwater at station R1.

A sea urchin, Hemicentrotus pulcherrimus, was collected from Liuqiu Island. A 10% KOH solution was used for tissue digestion. The shell of a pteropod, Creseis virgula, was collected around the coast of southwestern Taiwan. Spring water collected at station S5 on 2021/12/3, and surface seawater collected at the coast of southwest Taiwan on 2021/1/12 were poisoned with 0.05% saturated HgCl₂ and sealed for the incubation experiments. The spine and shell were incubated in a 250 ml borosilicate glass bottle filled with the spring water for 60 days at 25°C. The seawater incubated with the spine was used as the control. On the 30th day, we refreshed the spring water and seawater, as well as taking images under a microscope (model: MSHOT MZ88) using a Canon EOS 600D digital camera on the 1st, 30th and 60th days.

Results and Discussion

Major Ions and Their Implied Material Source From Chemical Weathering

Table 1 shows the conductivity, salinity, and the major ions of the spring waters at stations S1–S5 and the rainwater at station R1. Generally speaking, atmospheric depositions and the chemical weathering of rocks are two significant sources of ions for natural waters. Human activities, such as sewage input, could also contribute major ions. Of note is that the low CH₄ concentrations of the spring water (Table 2) suggested that the influence of human activities on the major ions of the spring water was minimal, as local sewage discharge usually has several orders of magnitude higher in CH₄ concentration (Borges et al., 2018). Major ions in the spring waters of Liuqiu Island are contributed mainly from the chemical weathering of rocks, as the major cations (Na⁺, K⁺, Ca²⁺, Mg²⁺) and anions (Cl⁻, SO₄²⁻, HCO₃⁻) in rainwater collected on 2020/8/26 were negligibly small when compared with the spring water in Liuqiu Island collected on 2020/12/3 (Table 1). Taking Na⁺, K⁺, Ca²⁺, Mg²⁺ as examples, the rainwater was able to contribute only 0.2, 1.1, 0.1, and 0.2%, respectively, to that of the spring water. Such a result implies that various chemical weathering processes contribute the most to the spring water’s major ions. The positive correlations between the major ions and salinity of the spring waters of Liuqiu Island and the rainwater provided further evidence for this suggestion (Figure 2). Several chemical weathering reactions are listed as follows:

TABLE 2

TABLE 2. Flow rate, temperature, salinity, DO, pH on the NBS scale, DIC, TA, CO₃^2-, pCO₂, NO₃⁻ + NO₂⁻, PO₄^3-, SiO₂, CH₄, Ca²⁺, Ω_Ara, and the Ω_Cal of the spring water at S5 on Liuqiu Island between 2017 and 2021.

FIGURE 2

FIGURE 2. Major ions vs. salinity of the rainwater at R1 and the spring waters at S1–S5 on Liuqiu Island. The solid lines show the linear regression lines passing the origins.

The dissolution of halite:

$\text{NaCl}\to {\text{Na}}^{+}+{\text{Cl}}^{-}(1)$

The dissolution of a silicate mineral (using sodium feldspar as an example):

$2{\text{NaAlSi}}_3{O}_8+2{\text{H}}_2{\text{CO}}_3+9{\text{H}}_2\text{O}\to 2{\text{Na}}^{2+}+2{\text{HCO}}_3^{-}+4{\text{H}}_4{\text{SiO}}_4+{\text{Al}}_2{\text{Si}}_2{\text{O}}_5{\left(\text{OH}\right)}_4(2)$

The dissolution of CaCO₃ or MgCO₃ (using CaCO₃ as an example):

${\text{CaCO}}_3+{\text{H}}_2{\text{CO}}_3\to {\text{Ca}}^{2+}+2{\text{HCO}}_3^{-}(3)$

The dissolution of dolomite:

${\text{Mg}}_{\left(1-x\right)}{\text{Ca}}_x{\text{CO}}_3+{\text{CO}}_2+{\text{H}}_2\text{O}\to \left(1-x\right)\text{Mg}+x{\text{Ca}}^{2+}+2{\text{HCO}}_3^{-}\text{and}\left(\text{0}\le \text{x}\le \text{<}1\right)(4)$

The oxidation of pyrite:

$4{\text{FeS}}_2+15{\text{O}}_2+8{\text{H}}_2\text{O}\to 2{\text{Fe}}_2{\text{O}}_3+8{\text{H}}_2{\text{SO}}_4(5)$

Na⁺ was the most or second most abundant among the cations, followed by Ca²⁺ in the rainwater and spring waters, whereas HCO₃⁻ was the most abundant anion followed by Cl⁻ (Table 1). Generally, Cl⁻ ion mainly came from halite dissolution or marine spacy. Seawater has a Na⁺: Cl⁻ ratio of approximately 0.86 (Millero et al., 2008). In contrast, the freshwater samples shown in Table 1 had excess Na⁺ rather than Cl⁻ with ratios between 1.03 and 1.63. The almost 1:1 correlation between the Na and Cl ions (Figure 3) suggested that the Cl⁻ and the equivalent of Na⁺ came from the halite dissolution or marine spacy. The remaining Na⁺ (Na⁺ minus Cl⁻, corrected for halite dissolution contribution) and K⁺ were from Na- or K-feldspar weathering, which was expected to contribute the same amount of TA in the form of bicarbonate ion as shown in Eq. 2. Such a result is in accordance with previous study that in Liuqiu Island siliceous soils cover carbonate rocks (Holocene coral reef or Pleistocene limestone) (Cheng et al., 2011). The carbonate rocks’ dissolution mainly contributes to the Ca²⁺ and Mg²⁺ ions (see Eqs 3, 4. The [Ca²⁺]/[Mg²⁺] ratio of 3.8 of the spring water is in accordance with that of the soil pedons in Liuqiu Island, ranging between 1.4 and 7.1 (average 3.7 ± 1.9, n = 21) (Cheng et al., 2011). The SO₄^2- could be contributed by the CaCO₃ or MgCO₃ dissolution with the participation of H₂SO₄ instead of H₂CO₃. But this is unlikely to explain the amount of SO₄ found in the spring waters of Liuqiu Island, as the rainwater contained a negligibly small amount of SO₄. Pyrite oxidation (see Eq. 5) might contribute the SO₄ to the spring water and the surface freshwaters in Liuqiu Island. Under pyrite oxidation, 1 mol of SO₄ formation would lead to 2 mol of TA deduction due to sulfuric acid formation.

FIGURE 3

FIGURE 3. Na⁻ vs. Cl⁻ of the rainwater and spring waters on Liuqiu Island. Table 1 shows the information in detail. The solid line shows the 1:1 ratio.

Carbonate Chemistry and the Acidic Property of Spring Water

Rainwaters sampled contained only a small amount of TA (-19–94 μmol/kg, n = 9) and DIC 38–89 μmol/kg, n = 9), whereas our time-series data at station S5 showed that the spring water at S5 had significantly higher TA (6,624–6,704 μmol/kg) and DIC (7,309–7,931 μmol/kg) values (Table 2). As mentioned above, the dissolution of feldspar or carbonate rocks contributed TA and DIC. Based on Eqs 1–3, regarding the spring water sampled on 2020/12/3, we estimated (Na⁺ − Cl⁻ ) + K⁺ + 2 (Ca²⁺ + Mg²⁺) = 5787 μmol/kg for TA and (Ca²⁺ + Mg²⁺) = 2439 for DIC. Note that CaCO₃ or MgCO₃ weathering consumed CO₂. The organic matter decomposition could contribute to this CO₂ in the groundwater. Soil air has a significantly higher CO₂ concentration than that of the atmosphere and could also contribute to the CO₂ in the groundwater. Using the TA value, we calculated that the DIC value to be 6,252 μmol/kg when the pCO₂ was the same as that in the atmosphere (about 400 μatm; 100% humidity). That is, we estimated that there was (7,848–6,252) = 1,596 μmol/kg of excess DIC or CO₂ in the spring water with respect to the atmospheric CO₂ level. Figure 4 shows the estimations. Again, this amount of CO₂ could be contributed by the organic matter decomposition or by soil air. Organic matter decomposition increased the DIC value but slightly decreased the TA value. In comparison, the CO₂ gas exchange between soil air and groundwater would not change TA. However, we could not quantify the amount of TA change with this 1,596 μmol/kg excess CO₂, as we could not quantify the amount of CO₂ in the soil air–groundwater CO₂ exchange or in the groundwater’s organic matter decomposition. Based on Eqs 1–3, we estimated the TA value of the spring water to be 5,787 μmol/kg, explaining 86% of the measured value of 6,701 μmol/kg. The excess CO₂ of 1,596 μmol/kg accounted for 20% of the measured DIC of 7,848 μmol/kg (Figure 4). Such results suggest that the chemical weathering mainly contributed to the TA and DIC values, and part of the DIC was contributed by the increase in CO₂ through organic matter decomposition or soil air–groundwater CO₂ exchange.

FIGURE 4

FIGURE 4. Estimated TA and DIC of the spring water at station S5 using major ion concentrations and the excess CO₂ calculated with measured TA and pCO₂ = 400 μatm, assuming the air–water CO₂ equilibrium.

Surface seawaters around southwest Taiwan and in the northern South China Sea generally had pH values of about 8.20 (about 8.05 on the total scale) or higher (Chen et al., 2010; Lui and Chen, 2015; 2017). In contrast, the spring waters collected between 2017 and 2021 had a relatively low pH value, ranging 7.02–7.25 and averaging 7.15 ± 0.09 (n = 5). The dissolution of carbonate rock consumes dissolved CO₂ and generates TA and DIC in a ratio of 2:1. Feldspar dissolution consumes CO₂ and generates TA as well. That is, increasing TA and DIC in a ratio equal to or higher than 2:1 increases the pH, Ω_Ara, and Ω_Cal values but decreases the pCO₂ value. Such a change also increases the carbonate buffering capacity of a water body by reducing the extent by which the pH, Ω_Ara, and Ω_Cal values are reduced under additional CO₂ dissolution (Chou et al., 2013). Indeed, these water bodies’ relatively low pH values were mainly due to the dissolution of CO₂ through the soil air–groundwater CO₂ exchange and organic matter decomposition. Although the dissolution of carbonate rocks generated a considerable amount of CO₃²⁻ and Ca²⁺, the addition of a high amount of excess CO₂ reduced the CO₃²⁻ concentrations of the spring waters to just 6.3–9.4 μmol/kg due to thermodynamics. Consequently, the Ω_Ara and Ω_Cal were 0.92–1.40 and 1.50–2.28, respectively. With a considerable amount of excess CO₂, the pCO₂ of the spring waters could be as high as 37,316 μatm (Table 2).

Physical Mixing Behaviors in the Subterranean Estuaries

In Liuqiu Island, the values of temperature, DO, pH, TA, DIC, Ω_Ara, and SiO₂ in the spring water did not considerably change across seasons (Figure 5). The temperatures of the SGD samples and seawaters showed strong seasonal variations. The strong negative linearities between TA, DIC, NO₃⁻ + NO₂⁻, SiO₂, and the salinity of the SGD samples suggested that the carbonate chemistry and nutrients of the SGD samples were controlled mainly by physical mixing between the groundwater and ambient seawater within the seabed, the so-called subterranean estuary. The freshwater endmembers of the TA, DIC, and SiO₂, determined using the SGD data and linear regressions methods, were similar to those of the spring water, suggesting that the carbonate chemistry of the discharged submarine groundwater at station A1 had similar carbonate chemistry to that of the spring water at station S5, which had no observable changes across seasons. The differences in TA and DIC between the linear-regression determined freshwater endmembers of the SGD samples and the spring waters were (7,917–6,640) = 1,277 μmol/kg and (8,330–7,649) = 681 μmol/kg, respectively (Figure 5; Table 2). The differences in TA and DIC had a ratio of 1.88. Such a result reflects that the higher TA and DIC of the SGD freshwater endmembers were mainly due to the further dissolution of carbonate rocks, which has changes of TA and DIC in a ratio of two. Generally, water with a lower pH or Ω_Ara value is more corrosive to CaCO₃. Although the spring water contained a very low CO₃²⁻ concentration, it had a Ω_Ara value that was sometimes slightly below one. This is because the spring water contained a high concentration of Ca²⁺ that came from the weathering of the CaCO₃ rock, increasing the Ω_ara value. That is, the dissolution of CaCO₃ minerals around the coral islands effectively reduced the corrosiveness of the groundwater and hence the SGD water, reducing the environmental stress that was due to the discharge of the acidic SGD. Meanwhile, the linearities of TA and DIC vs. salinity of the SGD samples in Liuqiu Island suggested that the residual time of the groundwater in the freshwater–seawater mixing zones, the so-called subterranean estuaries, was short. The increase in buffering effect of the SGD water due to an additional dissolution of carbonate rock in the subterranean estuary was insignificant, making SGD is an additional acidic source with similar carbonate chemistry of the groundwater for the coastal areas.

FIGURE 5

FIGURE 5. Temperature, DO, pH, TA, DIC, Ω_Ara, NO₃⁻ + NO₂⁻, PO₄³⁻, SiO₂, and CH₄ vs. salinity of rainwater, spring water, SGD water, and seawater in Liuqiu Island. The rainwater, spring water, SGD water, and seawater are in light blue, black, red, and blue, respectively. The red lines extended to the axes and equations show the linear regressions for the conservative parameters of the SGD data.

The SGD waters likely had a freshwater endmember with a lower NO₃⁻ concentration than that of the spring water. The PO₄³⁻ was scattered across the salinity gradient largely because the groundwater and the ambient seawater contained similar but low concentrations of PO₄³⁻. The use of chemical fertilizer could be an important source of nutrients for groundwater. According to the Liuqiu Township Office, only 0.01 km² (0.15% of the total area) is farmland in Liuqiu Island. Most important is that nearly all of the farmland is dryland. Without sufficient freshwater (such as river water) to support a considerable scale of agriculture, the influence of the use of fertilizer on the chemistry of the groundwater in Liuqiu Island or Dongsha Island is expected to be insignificant. Sewage input could be another critical factor influencing the chemistry of groundwater in Liuqiu Island or Dongsha Island. In Liuqiu Island, the CH₄ concentrations were low for both the spring water and SGD samples, showing no observable influence of anthropogenic activities in our sampling sites, such as local sewage discharge, which is usually several orders of magnitude higher in CH₄ concentration (Borges et al., 2018). Noting, fresh SGD can be observed in Liuqiu Island in both the wet and dry seasons, showing that it has a continual effect on the coast of Liuqiu Island all year round. In contrast, the surface seawaters had high DO, pH, and Ω_ara values but low nutrient concentrations. Such a result was likely due to the enhanced productivity achieved via the support of nutrients from the SGD or from the Gaoping River, which is about 13 km from Liuqiu Island. Local discharges may also affect this and warrant further investigation.

In Dongsha Island, which is about 420 km from Liuqiu Island, the DO and pH of the groundwater, SGD waters, and seawaters had positive correlations with salinity, whereas the TA, DIC NO₃⁻ + NO₂⁻, PO₄³⁻, SiO₂ and CH₄ showed negative correlations with salinity (Figure 6). Such results suggest that the carbonate chemistry and nutrients of the SGD waters were controlled mainly by physical mixing between the groundwater and seawaters. Furthermore, the carbonate chemistry and nutrients of water samples collected over the wet and dry seasons in Dongsha Island were consistent with each other, showing stable chemical properties of the groundwater endmember for the SGD waters. Interestingly, the trends of the pH, TA and DIC vs. salinity plots suggested that the freshwater endmembers of the SGD waters in Dongsha Island were similar to those in Liuqiu Island. Such a result suggests that the factors controlling the carbonate chemistry of the groundwaters and SGD waters in Dongsha Island might be similar to those in Liuqiu Island. In the seagrass meadows in the inner lagoon, the TA and DIC released from the sediment, as well as the high productivity increased the TA:DIC ratio, making the seawater around the seagrass meadows high in DO, TA, pH and Ω_Ara but low in DIC and pCO₂ values (Chou et al., 2018). Our water samples were likely not affected by the seawater with relatively high TA but low DIC from the seagrass meadows, maintaining values similar to that of the offshore surface waters. Notably, in Dongsha Island, the high CH₄ and PO₄^3- concentrations of the groundwaters, SGD waters, and seawaters suggest that sewage discharges might have affected these waters. Similar to the case in Liuqiu Island, fresh SGD waters could be found around Dongsha Island in the dry season when the rainfall was low, suggesting that the SGD in Dongsha Island maintains a continual effect around the coast all year round and not to mention in the wet season when the rainfall is high.

FIGURE 6

FIGURE 6. Temperature, DO, pH, TA, DIC, Ω_Ara, NO₃⁻ + NO₂⁻, PO₄³⁻, SiO₂, and CH₄ vs. salinity of groundwater, SGD water, and seawater in Dongsha Island. The groundwater, SGD, and seawater are in green, red, and blue, respectively. The red lines extended to the axes and equations show the linear regressions for the conservative parameters of the SGD data.

Effect of Acidic Property and Corrosiveness of SGD on CaCO₃ Skeleton and Shells

Notably, the pH could be as low as 7.02 for the spring water in Liuqiu Island and 7.07 for the groundwater in Dongsha Island (Figures 5, 6). Most pH values of the SGD samples in Liuqiu Island and Dongsha Island, however, were far below 7.95, reaching as low as 7.30 for Liuqiu Island and 7.34 for Dongsha Island. Such results reflect the acidic properties of the groundwaters and SGD waters in these two coral reef Islands. As mentioned above, the spring water at station S5 in Liuqiu Island had similar carbonate chemistry to that of the fresh SGD endmembers in Liuqiu and Dongsha Islands. Although the spring water and biogenic carbonate minerals are spatially separated, interactions between the spring water and biogenic carbonate minerals could provide insights into the acidic effects of the SGD on carbonate skeletons and shells. On this basis, the spring water of Liuqiu Island collected on 2020/12/3 with a Ω_Ara of 0.96 and preserved with saturated HgCl₂ was used to conduct an incubation experiment. A surface seawater sample collected at the coast of southwestern Taiwan on 2021/1/12 with a Ω_Ara value of 2.73 was used for comparison. The spines of sea urchins (H. pulcherrimus) were incubated in the water samples and observed after 30 and 60 days. The shell of a pteropod (C. virgula) was also incubated in the spring water for observation.

The incubation results showed that the spine of H. pulcherrimus had no observable difference after incubation in seawater for 60 days (Figure 7). In contrast, the spine showed significant dissolution after 30 days and 60 days incubations in the spring water of Liuqiu Island. The base of the spine showed a reduction in size, and the shaft of the spine was etched, becoming rough (Figure 7). The shell of C. virgula also showed an indication of dissolution, turning from transparent to milky white. Since HgCl₂ was added to inhibit microbial activity, we expected that the dissolution of the spine or shell caused by microbial activities to be insignificant. Our observation showed that the spine of the sea urchin dissolved more readily than the shell of the pteropod. This was because the spine of the sea urchin is composed of high-magnesium calcite, which has higher solubility than that of aragonite (Grossmann and Nebelsick, 2013; Haese et al., 2014). Furthermore, even though the shells of pteropods are composed of aragonite, the shapes, microstructures, and MgCO₃:CaCO₃ ratio of the shells are different, causing the shells to have different solubility and dissolution rates.

FIGURE 7

FIGURE 7. Images of (bottom left) the spine of H. pulcherrimus and (right) shell of C. virgula before (0 days) and after incubation in the spring water at station S5 with Ω_Ara = 0.96 for 30 and 60 days. Seawater with Ω_Ara = 2.73 incubated with (top left) the spine of H. pulcherrimus was used as the control.

It is worth mentioning that our incubation experiments indicated the acidic property of SGD on biogenic carbonate minerals. However, the effects of acidic SGD on live marine organisms are expected to be more complicated. This is because Ω_Ara and other factors, such as pH, temperature, pCO₂ and dissolved oxygen, also influence the physiology of marine organisms (Glover and Kidwell, 1993; Shirayama and Thornton, 2005; Kroeker et al., 2013; Van de Waal et al., 2013; Peck et al., 2016; Mekkes et al., 2021). Moreover, the outermost organic layer, periostracum, or other organic matters of many calcifying organisms can effectively counter the CaCO₃ dissolution under an acidic environment (Glover and Kidwell, 1993; Peck et al., 2016). Of note is that both incubation experiments and field samples showed that acidified conditions enhanced carbonate shell dissolution and reduced calcification rates of many live calcifying organisms (Glover and Kidwell, 1993; Orr et al., 2005; Shirayama and Thornton, 2005; Hall-Spencer et al., 2008; Talmage and Gobler, 2010; Lischka et al., 2011; Moya et al., 2016; Peck et al., 2016; Zhai, 2018; Li and Zhai, 2019; Zhai et al., 2019; Mekkes et al., 2021). Indeed, the reported acidified conditions mostly had higher pH and Ω_ara values but lower pCO₂ values than that of the SGD samples in Liuqiu Island or Dongsha Island. For instance, the shell of Limacina helicina significantly degraded after 29 days of incubation when pH on the total scale and pCO₂ were 7.66 and 1,150 μatm, respectively (Lischka et al., 2011). In the North Yellow Sea, the community net calcification rate was nearly zero when the Ω_ara value reached 1.5–1.6 (Zhai, 2018; Li and Zhai, 2019; Zhai et al., 2019). Additionally, the CaCO₃ sediments would be dissolved when the Ω_ara value of the seawater reached 2.92 ± 0.16 or lower (Eyre et al., 2018). This is largely due to the additional acidic effect as a result of the CO₂ produced by the decomposition of organic matter in sediment. The Liuqiu Island and Dongsha Island examples reveal that SGD could be an important acidic input to coastal oceans.

Conclusion

The hydrogeochemistry and carbonate chemistry of the groundwaters, SGD waters, and the seawaters in two coral islands were examined in this study. Our results show that although the dissolution of carbonate rocks increased pH, Ω_Ara, Ω_Cal and the buffering capacity of the groundwater, the CO₂ from the organic matter decomposition or soil CO₂ enhanced the corrosiveness of the groundwater, shifting Ω_Ara from oversaturation to undersaturation. The acidic property of the SGD waters was verified using biogenic carbonate minerals. Although SGD amounts to only several percent of the riverine discharge, it is a common natural phenomenon that could affect the coast all year round, especially in winter when there is minimal rainfall. We suggest that the impacts of SGD on coastal biogeochemical cycles and ecosystems due to its acidic property and continual effect on the coast all year round deserve consideration in further investigations.

Data Availability Statement

The raw data supporting the conclusion of this article will be made available by the authors.

Author Contributions

H-KL designed and led the writing of the manuscript. C-TAC was responsible for the overall structure of the manuscript. H-KL, M-YL, F-YW, and RC participated in the sampling. H-KL, RC, H-CT, and W-PH participated in the measurements. H-CL provided the pteropod samples and assisted in taking images. H-CL and L-LL provided advice for the incubation experiment. All authors read and commented on the final version of the manuscript.

Funding

This research was funded by the Ministry of Science and Technology of Taiwan (MOST 107-2611-M-110-026-, MOST 108-2611-M-110-025, MOST 109-2611-M-110-010, MOST 109-2611-M-110-016, MOST 110-2611-M-110-024).

Conflict of Interest

The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Publisher’s Note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Acknowledgments

Chih-Chieh Su, Feng-Sin Hsu, Pei-Fen Chen, Ting-Hsuan Huang, Sheng-Xiang Xu, and research assistants from Dongsha Atoll Research Station are acknowledged for their assistance during sampling in Dongsha Island. Three reviewers provided detailed and constructive comments, which helped strengthen the manuscript.

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