Zhanjiang Bay is surrounded by Zhanjiang City ( Figure 1 ). There is a Suixi River at the top of the upper bay. The annual runoff of the river is 10.4 × 10 ⁸ m³, and it directly flows into the upper bay. The depth in the bay ranges from 2 to 23 m, with the lower bay being deeper. Only a narrow outlet (width of ~2 km) connects Zhanjiang Bay with the SCS water outside the bay ( Figure 1 ). In the outer bay, a West-Guangdong Coastal Current (WGCC) affects Zhanjiang Bay year-round. During the summer, stronger coastal current can intrude the high-salinity seawater outside the bay into Zhanjiang Bay (Lao et al., 2022b). Affected by the East Asian monsoon, rainfall in the rainy seasons (April-October) (>85% of the annual rainfall) is much higher than in other seasons (Chen et al., 2019, 2021). Moreover, due to frequent typhoon events, the amount of rainfall brought by typhoons can reach over 50% of the annual rainfall in this region (Chen et al., 2021).

Typhoon Talim (2023) generated near the Luzon Island in July 14. It migrated northwest at an average speed of 4.3 m s^-1 (a range of 1.7-6.1 m s^-1, from https://typhoon.slt.zj.gov.cn/###), passing through the SCS and increasing its intensity in the northwestern SCS (with maximum wind speed reaching 40 m s^-1) before making landfall in Zhanjiang Bay in July 17 ( Figure 1A ). Affected by Typhoon Talim, heavy rainfall occurred in Zhanjiang Bay during the typhoon period (with a rainfall of over 300 mm), with the highest rainfall (over 100 mm on July 18) occurring after the typhoon made landfall.

Two cruises were conducted in Zhanjiang Bay before (July 05) and two days after the Typhoon Talim landfall (July 19). Seven stations, including four in the upper bay and three in the lower bay, were established in each cruise ( Figure 1B ). In addition, during the typhoon period, five rainwater samples were collected on the roof of Guangdong Ocean University, located about 3 km from Zhanjiang Bay. Among them are two rainwater samples before the typhoon, and three rainwater samples during the typhoon period. Rainfall is recorded simultaneously during the collection of rainwater samples. Surface and bottom seawater samples were collected using Niskin bottles (10 L) in each station before and after the typhoon cruises.

Seawater temperature, salinity and depth were determined on-site using an RBR Maestro multiparameter water quality monitor (RBRmaestro3, RBR, Canada). After sampling, about 1000 mL seawater was filtered by glass fiber filters (GF/F, 0.7 μm aperture and 47 mm diameter, Whatman) for the dual water isotope (δD and δ¹⁸O) and nutrient samples, and the filtrate was transferred into the pre-cleaned acid-washed polyethylene bottles. The pre-treatment process of dual water isotope in seawater samples followed the study of Lao et al. (2022a, 2022b, 2023b), and the rainfall samples followed the study of Chen et al. (2021).

Nutrient samples (NO₂ ^-, NO₃ ^-, PO₄ ^3-, and SiO₃ ^2-) were measured by a San++ continuous flow analyzer (Skalar, Netherlands), and the samples for NH₄ ⁺ were measured using spectrophotometry. The measurements of δD and δ¹⁸O followed the procedures prescribed by Lao et al. (2022a, 2023b) using an isotope ratio mass spectrometer (Gasbench II-IRMS) (Gasbench II interfaced with a 253 plus mass spectrometer). H₂ and CO₂ were used to equilibrate δD and δ¹⁸O, and these equilibrated gases were measured using the Gasbench II-IRMS. For the measurement of δD, Pt catalyst was added into the 200 μL seawater sample, and a small amount of H₂ (2% H₂/He) was injected to make D/H in water and D/H in H₂, to be in isotopic equilibrium at 28.00 °C for 40 min. For the measurement of δ¹⁸O, a small amount of CO₂ (1% CO₂/He) was injected into a 500 μL seawater sample to make ¹⁸O/¹⁶O in isotopic equilibrium at 24.00 °C for at least 24 hours. The international standard reference materials for water (VSMOW2, GISP, and SALP2) were used to calibrate the samples, and the precision for δD and δ¹⁸O was ±0.5‰ and ±0.1‰, respectively. The detection limits for NO₂ ^-, NO₃ ^-, NH₄ ⁺, PO₄ ^3-, and SiO₃ ^2- were 0.1 μmol L^-1, 0.1 μmol L^-1, 0.1 μmol L^-1, 0.02 μmol L^-1 and 0.45 μmol L^-1, respectively.

As the water isotopes are conserved and less affected by the water environment, the proportion of mixing between different water masses can be quantified using the Bayesian model (Wu et al., 2021; Lao et al., 2022a, 2022b, 2023b, 2023c). The Bayesian model was constructed using the Stable Isotope Analysis software package in R (SIAR). The framework and detailed information on the Bayesian model were described by Lao et al. (2022a) and Moore and Semmens (2008). In this study, we first excluded the influence of water isotope fractionation after water mass mixing through the relationship between δ¹⁸O and deuterium excess (d-excess, defined as δD – 8 × δ¹⁸O, can be used as an indicator for kinetic fractionation, which exhibits an inverse relationship with δ¹⁸O during evaporation) (Dansgaard, 1964). In this study, four end-members, including the fresh diluted water from the top of the upper bay, rainwater, groundwater around the Zhanjiang Bay and the seawater from the outer bay, were used to quantify the contribution of different water sources to the bay before and after the typhoon. The data on groundwater around Zhanjiang Bay was obtained from our previous study (Lao et al., 2022b). Due to the minor seasonal variation of δD and δ¹⁸O in groundwater around the Zhanjiang Bay, the groundwater water end-member for the pre- and post-typhoon periods were all obtained from the study of Lao et al. (2022b). The rainwater end-member was obtained from the average values of δD and δ¹⁸O in rainwater during the pre- and post-typhoon periods, respectively. The fresh diluted water end-member was obtained from the δD and δ¹⁸O values in the Suixi River during summer (Chen et al., 2024), which is similar to the sampling period of this study. The seawater end-member was obtained from the station ZJ10. These end-member values are presented in Table 1 .

The mixing of water masses can alter the distribution of nutrients in the local marine environment (Lao et al., 2022a, 2023a; Chen et al., 2024). According to the proportional contribution of each water source and their nutrient concentrations, the contribution of the different water sources to the nutrient load in Zhanjiang Bay can be calculated by the follows:

where Q is the contribution of water masses to the nutrient load in Zhanjiang Bay (f: freshwater; o: outer bay; g: groundwater; r: rainwater), P is the contribution from each water source to the seawater of Zhanjiang Bay, and C is the nutrient concentrations of each water end-member ( Table 2 ).

The Pearson’s correlation analysis and Student’s t-test analysis were conducted using SPSS Statistics 19.0. Before conducting the Pearson’s correlation analysis and Student’s t-test analysis, all variables were tested for normality using Kolmogorov-Smirnov test.

Before the typhoon, a high temperature (30.07-32.15°C) was observed in Zhanjiang Bay, especially in the surface water, and the temperature gradually decreased from the upper bay to the lower bay ( Figure 2A ). The salinity ranged from 16.4 to 30.7, and the lowest salinity was observed at the top of the upper bay, with a decreased trend toward the lower bay ( Figure 2C ). Higher temperature (an average of 31.35°C) but lower salinity (an average of 25.2) in the surface water than those in the bottom water (an average of 30.76°C for temperature and of 26.8 for salinity), suggesting that moderate stratification occurred in the water column of Zhanjiang Bay during the pre-typhoon period. However, the water temperature (28.03-30.03°C) and salinity (4.8-29.8) dropped remarkably after Typhoon Talim ( Figure 2 ). Particularly in the upper bay, the surface water temperature dropped by 2.07°C during the post-typhoon period, indicating that strong external force of the typhoon has destroyed the stratification structure in the water column of the bay. In addition, the salinity in the upper bay has also decreased from an average of 22.6 during the pre-typhoon period to an average of 16.9 during the post-typhoon period. This indicated that the heavy rainfall during the typhoon period increased runoff input into the bay. However, the salinity in the lower bay exhibited less variation after the typhoon, with an average of 29.2 during both periods. Moreover, after the typhoon, the salinity in the surface water was almost consistent with the bottom water in the lower bay ( Figure 2D ), which was different from the distribution before the typhoon (average of 28.8 on the surface, an average of 29.6 on the bottom water). This indicated that in addition to the freshwater input and the stratification destroyed by the typhoon, the typhoon might cause intrusion of high-salinity water from the outer bay during the typhoon period. Remarkably, the surface salinity gradient increased substantially in the upper bay (from ZJ3 to ZJ7, with ~22.0 km) after the typhoon (with a salinity gradient of 1.04 psu km^-1 during the post-typhoon) ( Figures 2C, D ), which further indicates the intrusion of high-salinity seawater and the formation of a strong salinity front by mixing a large amount of freshwater input into the bay.

Before the typhoon, δD and δ¹⁸O values ranged from -21.4‰ to 0.8‰ and from -2.7‰ to -0.6‰ in the Zhanjiang Bay, with an average of -8.4‰ and -1.3‰, respectively. Both δD and δ¹⁸O values in the surface water was similar to the bottom water, and the values increased gradually from the upper bay to the lower bay ( Figures 2E, G ). However, similar to the salinity, the δD and δ¹⁸O values decreased remarkably and formed a large isotopic value gradient in the upper bay during the post-typhoon period ( Figures 2F, H ). δD and δ¹⁸O values ranged from -54.4‰ to -7.0‰ and from -8.3‰ to -0.8‰ in the Zhanjiang Bay during the post-typhoon period, with an average of -19.7‰ and -2.6‰, respectively. In the upper bay, δD and δ¹⁸O values dropped substantially from the pre-typhoon period (an average of -13.2‰ for δD and -1.8‰ for δ¹⁸O) to the post-typhoon period (an average of -28.9‰ for δD and -4.4‰ for δ¹⁸O). However, a minor decrease in δD and δ¹⁸O values was observed in the lower bay (an average of -3.5‰ for δD and -0.8‰ for δ¹⁸O during the pre-typhoon, and an average of -9.6‰ for δD and -0.9‰ for δ¹⁸O). In the rainwater, the δD and δ¹⁸O values ranged from -30.4‰ to -22.9‰ and from -4.2‰ to -3.4‰ during the pre-typhoon period. However, the values decreased substantially during the post-typhoon periods (from -96.9‰ to -50.0‰ for δD and from -13.2‰ to -7.4‰ for δ¹⁸O).

Before the typhoon, the concentrations of NO₂ ^-, NO₃ ^-, NH₄ ⁺, PO₄ ^3-, and SiO₃ ^2- ranged from 0.6 to 5.2 μmol L^-1, 1.6 to 46.6 μmol L^-1, 3.9 to 21.0 μmol L^-1, 0.3 to 4.1 μmol L^-1 and 10.0 to 61.8 μmol L^-1, respectively. They all exhibited higher concentrations at the top of the upper bay (station ZJ3), gradually decreasing toward the lower bay with increasing salinity. This indicated the influence of terrestrial nutrient input in the bay. In addition, there is no significant difference in nutrient concentration between the surface and bottom layers during the pre-typhoon period (t-test, p>0.05). However, except for the NO₂ ^-, the nutrient concentrations increased remarkably in the bay during the post-typhoon period, particularly in the upper bay ( Figure 3 ). After the typhoon, the concentrations of NO₂ ^-, NO₃ ^-, NH₄ ⁺, PO₄ ^3-, and SiO₃ ^2- ranged from 0.4 to 4.5 μmol L^-1, 1.8 to 70.5 μmol L^-1, 3.4 to 42.2 μmol L^-1, 0.6 to 5.1 μmol L^-1 and 11.5 to 61.3 μmol L^-1, respectively. In the upper bay, the concentrations of NO₃ ^-, NH₄ ⁺, PO₄ ^3-, and SiO₃ ^2- during the post-typhoon period were 1.7 times, 1.9 times, 1.5 times, 1.3 times, respectively, higher than the pre-typhoon period ( Table 3 ). However, in the lower bay, the nutrient concentrations were decreased during the post-typhoon period compared to the pre-typhoon period (except for PO₄ ^3-) ( Table 3 ). This further indicated that the intrusion of high-salinity seawater from the outer bay has diluted the nutrients in the lower bay, while the formation of a salinity front in the upper bay caused by the typhoon has retained nutrients in the upper bay (the barrier effect of the front). In addition, the nutrient concentrations in the rainwater during the typhoon period were lower than those in the pre-typhoon period ( Table 3 ), which could be related to the nutrients in the rainwater being diluted by the heavy rainfall during the typhoon period.

The correlation between isotopic values and other physiochemical parameters is presented in Table 4 . There was a significantly positive relationship between δD and δ¹⁸O values with salinity in Zhanjiang Bay during both pre- and post-typhoon periods, indicating that the seawater mixed well in the bay during these two periods. In addition, significantly negative relationships were found between the nutrient concentrations with salinity and dual water isotopic values during pre- and post-typhoon periods. This indicated that nutrient distribution was greatly influenced by water mixing in the bay.

Correlations of δD-δ¹⁸O and δD/δ¹⁸O-salinity are commonly used to indicate the mixing processes of water masses, as their relationship changes after mixing with other water sources, such as precipitation, runoff, and large-scale ocean mixing (Kumar et al., 2018; Reyes-Macaya et al., 2022; Lao et al., 2023b, 2023c; Craig and Gordon, 1965; Lian et al., 2016; Chen et al., 2020). In nature, the change in D value (over 250‰) is larger than that of ¹⁸O because the variability in the abundance of δD is much higher than δ¹⁸O (Dawson and Siegwolf, 2007). Therefore, after mixing with other water sources, the change in δD will be greater than in δ¹⁸O, resulting in changing their relationship (slope) (Lao et al., 2023c). For example, when seawater mixes with water that is characterized by lower isotopic values, such as runoff and precipitation, the slope of δD-δ¹⁸O will increase; when the seawater mixes with water that is characterized by higher isotopic values such as high-salinity seawater and evaporation, the slope will decrease (Craig and Gordon, 1965; Lao et al., 2022a, 2022b; Deshpande et al., 2013; Kumar et al., 2018). Moreover, dual water isotopes and salinity have an empirical relationship, greatly affected by marine hydrology and dynamics (Lao et al., 2023b). Their linear relationships are expected to be modified after mixing with other water masses (Deshpande et al., 2013; Kumar et al., 2018).

In this study, the slope of δD-δ¹⁸O (8.65) during the pre-typhoon period ( Figure 4 ) was higher than the global meteoric water line (GMWL, 8.0) (Craig, 1961) and the global ocean water line (GOWL, 7.37) (Rohling, 2007), and it was close to the precipitation line (8.96) in the Zhanjiang Bay (Chen et al., 2021) and the seawater of northwestern SCS (outer Zhanjiang Bay, 8.64) during summer (Lao et al., 2023b). This suggested that the seawater in the bay during the pre-typhoon period could be influenced by the input of precipitation, which is related to the frequent heavy rainfall during that period (Lao et al., 2022b, 2023c). In addition, the slope of δ¹⁸O-salinity (0.16) was lower than that in the Beibu Gulf (adjacent to Zhanjiang Bay, 0.25) during summer (Lao et al., 2022a), the SCS (0.27) during summer. This indicated that the seawater may also be influenced by the mixing with high-salinity water or evaporation, or both (Craig and Gordon, 1965; Rohling, 2007; Sengupta et al., 2013). The evaporation process can be excluded because of the decoupling relationship between d-excess and δ¹⁸O before the typhoon ( Figure 4B ). Therefore, the intrusion of high-salinity could be responsible for the lower slope of δ¹⁸O-salinity in the bay. Although the higher rainfall occurred in the summer, the salinity in the lower bay during this period (29.2) was still consistent with the winter (29.2) (Lao et al., 2022b). This indicated the possibility of high-salinity seawater intrusion from the outer bay. In the outer bay, the WGCC affects the Zhanjiang Bay year-round, and the intensity of the coastal current increases in summer (Yang et al., 2003; Xie et al., 2012; Lao et al., 2023d). The WGCC is affected by the subsurface water of the SCS, and its salinity is substantially higher than that of Zhanjiang Bay. This observation is consistent with previous studies (Lao et al., 2022b, 2023c).

During the post-typhoon period, the heavy rainfall and the increase in runoff input could be responsible for the decrease of δD and δ¹⁸O during the post-typhoon period ( Figure 2 ), which is supported by the increase in the slopes of δD-salinity and δ¹⁸O-salinity ( Figures 4C, D ). Unlike the δD/δ¹⁸O-salinity, a decreased slope of δD-δ¹⁸O indicated evaporation or increased intrusion of high-salinity seawater during the typhoon. δ¹⁸O was negatively correlated with d-excess during the post-typhoon period ( Figure 4B ). However, if evaporation were the primary process for the decreased slope of δD-δ¹⁸O, kinetic fractionation caused by evaporation would decrease the d-excess value to<0‰ in the seawater (Lao et al., 2023c). The positive d-excess value (an average of 0.8‰) during the post-typhoon period suggested less influence of evaporation during that period. In addition, the d-excess values from the runoff and oceanic seawater are ~10‰ and ~0‰, respectively (Kumar et al., 2018; Zhou et al., 2022). A d-excess value of 0.5‰ can be a critical point for indicating water processes, and a value between 0 and this threshold can be considered affected by the mixing with high-salinity seawater, and exceeding this threshold indicates the runoff input (Deshpande et al., 2013). The d-excess value (0.8‰) after the typhoon approaches this threshold, further indicating the impact of high-salinity seawater intrusion. The strong onshore winds caused by typhoons result in residual currents in Zhanjiang Bay flowing from the outer bay to the inner bay (Lao et al., 2023c). This was also supported by decreased nutrient concentrations in the lower bay during the post-typhoon period ( Table 2 ).

The increase in runoff input during typhoons and the mixing of intruding high-salinity seawater in the bay form a high salinity gradient (strong ocean front). There are two reasons for the relatively small changes in salinity in the lower bay. One is the barrier effect of the front, and the other is the intrusion of high-salinity seawater from the outer bay. Due to the barrier effect of the front, a large amount of fresh water is blocked in the upper bay, resulting in less freshwater flowing into the lower bay. In addition, seawater intrusion into the bay can “buffer” some freshwater input.

Compared to the Typhoon Barijat in 2018 (with a salinity gradient of 0.47 psu km^-1) (Lao et al., 2023c), Typhoon Talim formed a much higher salinity gradient in Zhanjiang Bay (1.04 psu km^-1), suggesting that a stronger ocean front formed after the Typhoon Talim. The migration trajectory of Typhoon Barijat closely resembles that of Typhoon Talim, with both making direct landfall in Zhanjiang Bay. Furthermore, the precipitation associated with Typhoon Barijat exhibits a similar pattern to that of Typhoon Talim, both yielding approximately 300 mm (Lao et al., 2023c). This suggests a comparable influx of freshwater into Zhanjiang Bay during these two typhoons. However, the intensity of Typhoon Talim (typhoon level) is stronger than that of Typhoon Barijat (a strong tropical storm), with wind speeds reaching reach 40 m s^-1 upon landfall, surpassing the maximum speed observed during Typhoon Barijat (28 m s^-1). These two typhoons confirmed that that typhoons directly landing in the bay can intrude high-salinity seawater into the bay. However, the stronger Typhoon Talim caused more seawater intrusion and formed a stronger ocean front. This indicates that under the similar typhoon conditions, the strength of the ocean front formation in the bay caused by typhoons depends on the typhoon intensity.

Owing to the lesser influence of kinetic fractionation before and after Typhoon Talim, dual water isotopes can be used to quantify water mixing in Zhanjiang Bay using the Bayesian model. Results were presented in Figure 5 . Before the typhoon, the high-salinity water dominated the contribution to the seawater in both the upper and lower bay, and the contribution in the lower bay (95%) was higher than that in the upper bay (72%). The contribution of freshwater in the upper bay (8%) was higher than that in the lower bay (only 2%). This is similar to the results of a previous study in Zhanjiang Bay (Lao et al., 2022b, 2023c). After the typhoon, the contribution of freshwater to the seawater in the upper bay increased remarkably (increased by 18%), while the contribution of high-salinity seawater decreased (decreased by 35%) ( Figure 5 ). In addition, the contribution of groundwater increased to 23% in the upper bay during the post-typhoon period, reflecting massive freshwater input into the upper bay during the typhoon period. During the typhoon period, a significant intrusion of high-salinity seawater into the lower bay was observed, with nearly 97% contribution to the seawater from the outer bay. Moreover, the formation of the ocean front prevented freshwater transport to the lower bay, resulting in a decrease in the contribution of freshwater to the seawater of the lower bay after the typhoon despite heavy rainfall during that period.

Changes in water mixing in Zhanjiang Bay could alter the distribution of nutrients after the typhoon because freshwater can erode substantial terrestrial nutrients into Zhanjiang Bay, while seawater intrusion dilutes the nutrients in the bay. According to the equations (1)-(4), the contribution of each water source to the nutrient loads was quantified, and the results were presented in Figure 6 . Before the typhoon, except for NH₄ ⁺, nutrients in the upper bay mainly originated from the freshwater input (54-65%). The higher contribution to the NH₄ ⁺ loads in the upper bay was observed from the precipitation input, which was similar to a previous study in the northwestern SCS, mainly due to the high NH₄ ⁺ concentration in the atmosphere affected by the industrial activities (Lao et al., 2023b). In the lower bay, the freshwater remained the main contributor to the NO₃ ^- (50%) during the pre-typhoon period. However, the sources of other nutrients have shifted towards input from the outer bay (69-79%) due to their significant contribution to seawater. Minor nutrient contribution from the groundwater in both upper and lower bay (0-5%). After the typhoon, the contribution of nutrients has undergone significant changes in Zhanjiang Bay. In the upper bay, the freshwater dominated the contribution of nutrients during the pre-typhoon period (53-95%). The contribution of seawater from the outer bay to the nutrients in this region sharply declined (from 9-41% before the typhoon decreased to 4-15%). The outer bay’s seawater dominated the lower bay’s nutrient load (54-92%). The contribution of groundwater to the nutrients in Zhanjiang Bay was still minor after the typhoon ( Figure 6 ). Although the typhoon brought heavy rainfall, it also diluted nutrient concentration in the rainwater, resulting in a small contribution of precipitation to the nutrients in Zhanjiang Bay (0-28%). Overall, the formation of the ocean front caused by the typhoon greatly limited nutrient transport between the upper and lower bay. This resulted in nutrient accumulation in the upper bay, while the intrusion of high-salinity seawater diluted the nutrients in the lower bay. Compared to the Typhoon Barijat period (an average of 45.2 μmol L^-1 for DIN) (Lao et al., 2023c), the stronger ocean front induced by the Typhoon Talim resulted in a significant increase in DIN concentration in the upper bay (increased by nearly 50%). This is mainly because runoff is the main DIN source in the bay, and the DIN input exhibited an increasing trend in the recent five years (2017-2021) (He et al., 2023). On the contrary, the input of PO₄ ^3- decreased during this period (He et al., 2023), and thus less change of PO₄ ^3- contribution was observed after the Typhoon Talim compared to the Typhoon Barijat (an average of 3.5 μmol L^-1 in the upper bay). However, in the lower bay, the DIN concentration during the post-typhoon Talim decreased compared to the Typhon Barijat (an average of 11.8 μmol L^-1) (Lao et al., 2023c), mainly influenced by more seawater intrusion after stronger typhoon Talim.

Zhanjiang Bay is a region frequently affected by typhoons. Typhoon has caused an increase in the contaminant loads in Zhanjiang Bay, seriously threatening local eco-environment and aquaculture activities and greatly affecting the development of local marine economy and human society (Zhou et al., 2021; Lao et al., 2023c). In addition, due to intense human activities such as dredging and basin dam construction, the intrusion of seawater from the outer bay has increased significantly over the past two decades, which could increase the salinity gradient (frontal enhancement) in the upper bay, thereby retaining more pollutants in the bay (Lao et al., 2022b). Typhoon activities can amplify such ecological risk, especially stronger typhoons ( Figure 7 ). Previous studies have found that after a super typhoon, a large number of land-based pollutants accumulate in Zhanjiang Bay, and the strong degradation of organic matter caused by the typhoon consumes a large amount of oxygen in the water (Zhou et al., 2021). This has caused devastating damage to local aquaculture activities (Zhou et al., 2021). The rainy season is the most frequent period of typhoon activity in Zhanjiang Bay, which is likely an important factor in aggravating eutrophication (Zhang et al., 2021; Zhang et al., 2022; He et al., 2023). According to historical data, eutrophication in Zhanjiang Bay has shown a significantly increasing trend over three decades, especially during the rainy seasons (He et al., 2023). This has led to an increase in the frequency of harmful algal blooms in Zhanjiang Bay (Zhang et al., 2022), posing a huge threat to the local eco-environment and aquaculture activities. Under global changes, although the number of typhoons may decrease, the intensity of typhoons become stronger (Elsner et al., 2008; Balaguru et al., 2016; Zhou et al., 2019), which may exacerbate the deterioration of water quality in the region. Therefore, the implementation of control measures to control the emission of nutrients into Zhanjiang Bay is urgent.