High Chlorophyll-a Areas along the Western Coast of South Sulawesi-Indonesia during the Rainy Season Revealed by Satellite Data

: The southern coast of South Sulawesi-Indonesia is known as an upwelling area occurring during dry season, which peaks in August. This upwelling area is indicated by high chlorophyll-a (Chl-a) concentrations due to a strong easterly wind-induced upwelling. However, the investigation of Chl-a variability is less studied along the western coast of South Sulawesi. By taking advantages of remote sensing data of Chl-a, sea surface temperature, surface wind, and precipitation, the present study firstly shows that along the western coast of South Sulawesi, there are two areas, which have high primary productivity occurring during the rainy season. The first area is at 119.0° E– 119.5° E; 3.5° S–4.0° S, while the second area is at 119.0° E–119.5° E; 3.5° S–4.0° S. The maximum primary productivity in the first (second) area occurs in April (January). The generating mechanism of the high primary productivity along the western coast of South Sulawesi is different from its southern coast. The presence of river runoff in these two areas may bring anthropogenic organic compounds during the peak of rainy season, resulting in increased Chl-a concentration.


Introduction
Chlorophyll-a (Chl-a) is an indicator for phytoplankton biomass, which becomes the most important driver of ocean ecosystem health and productivity. As the first trophic level, phytoplankton biomass transfers both material and energy to higher-trophic-level organisms. Thus, as a connection of food chain sequence, Chl-a concentration determines the biomass of fish and therefore, regulates the fish catch production in an area. The higher Chl-a concentration corresponds to the higher catch of fishes. Welliken et al. [1] reported a strong positive correlation between the catch of mackerel fish and Chl-a concentration in the Arafura Sea. Furthermore, Welliken et al. [2] also reported that the variation of skipjack tuna catches is influenced by Chl-a concentration in the Savu Sea. During August and September, the peak of Chl-a concentration becomes the potential fishing season for skipjack tuna in the Savu Sea. For the southern coast of Java, Lahlali et al. [3] found that the catch per unit effort of tuna fish increases along with the increase of Chl-a concentration and the decrease of sea surface temperature (SST). Thus, understanding the characteristics of Chl-a variability in an area is a key success for fishery management.
To date, the big picture of the variability of Chl-a in the Indonesian Maritime Continent (IMC) has been investigated by Siswanto et al. [4]. Using more than two decades of data of the satellite-based Chl-a, they managed to reveal the distinct spatio-temporal distribution of Chl-a associated with different climate events. In the coastal area of IMC, Chla mostly varies by the fluctuation of rainfall/river discharge. Meanwhile, in the open ocean, the mechanisms of the wind generated upwelling and downwelling dominantly controls the variability of Chl-a in the IMC.
As part of the IMC, the sea of South Sulawesi was less emphasized in the study of Siswanto et al. [4]. The sea off the southern coast of South Sulawesi is a well-known high Chl-a area during the peak of the boreal summer (gray box in Figure 1) [5,6]. By analyzing satellite data, Setiawan and Kawamura [5] found that the strong easterly wind blowing during the boreal summer monsoon corresponds to the events of Chl-a blooming and SST cooling at the southern coast of South Sulawesi. Furthermore, the evidence of the upwelling event was found by Utama et al. [6] by using a combination of Conductivity Temperature Depth (CTD) observation and reanalysis data. As indicated by their CTD data, the elevated cooler water mass proves the upwelling occurrence near the southern coast of South Sulawesi. They suggested that the offshore Ekman transport of around 8.5 m 2 /s causes this upwelling.
The topography of South Sulawesi is complex, as seen in Figure 1. The southern (red box) and northern (blue box) parts of the south of Sulawesi are separated by two mountain ranges. The bathymetry of the sea off the western coast of South Sulawesi is deeper in the north than in the south. Nurdin et al. [7] investigated the variability of Chl-a along the western coast of South Sulawesi. However, their research was limited to the Spermonde Islands (black box at Figure 1). They discovered that the Chl-a at the Spermonde Islands during the summer season is higher than during the rainy season. Furthermore, the Chla variation at the Spermonde Islands corresponds to the fishing ground of Rastrelliger kanagurta [8]. Therefore, the whole area along the western coast of the South Sulawesi has never before been explored.
In the present study, we investigate the variability of Chl-a for the whole area along the western coast of South Sulawesi. In Section 2 we explain the merging product of satellite-based Chl-a data as a proxy of primary productivity to reach the maximum coverage of the Chl-a, an observation that was used in this study. In addition, SST, surface wind, and rainfall data were also used for investigating its underlying mechanisms. The results and discussion are presented in Section 3, which emphasizes the spatial and temporal variation of Chl-a, surface wind, and precipitation in the study area. Finally, the conclusion is presented in Section 4. The gray box represents the well-known upwelling area that occurs during boreal summer, as reported by Setiawan and Kawamura [5]. The black box denotes the location of the Spermonde Islands. The blue and red dots denote the meteorological stations at Majene Regency and Makassar City, respectively. The yellow dot denotes the location of Barrang Caddi Island where in situ data collection was conducted on 8 September 2020. The blue (c) and red (d) boxes denote the area with mountainous ranges at the northern and southern part of the South Sulawesi, respectively. The land cover of (c,d) are obtained from Landsat 8 images on 15 March 2020 and 3 June 2020, respectively.

Data
We used blended multi satellites Chl-a products from the Ocean Color-Climate Change Initiative version 4.2 (OC-CCI 4.2) to investigate the primary productivity along the western coast of the South Sulawesi [9]. These data have daily and 4 km temporal and spatial resolutions, respectively. The Chl-a measurements from the Medium Resolution Imaging Spectrometer (MERIS), Aqua-Moderate Resolution Imaging Spectroradiometer (MODIS), Sea-Viewing Wide Field-of-View Sensor (SeaWiFS), and the Visible Infrared Imaging Radiometer Suite (VIIRS) were used for OC-CCI data production. Remote sensing reflectant (Rrs) 443, Rrs 555, phytoplankton absorption coefficient at 443 nm (aph 443), and particulate backscattering coefficient for dissolved and detrital material at 555 nm (bbp 555) of OC-CCI 4.2 were also used for examining the suspended sediment contamination in the observed Chl-a concentration. Rrs 443 (Rrs 555) estimates the existence of phytoplankton (suspended sediment) due to the strong absorption (reflectant) of Rrs 443 by phytoplankton (Rrs 555 by suspended sediment) [10,11]. Thus, the higher aph 443 and bbp 555 denote the more phytoplankton biomass and higher suspended sediment concentration.
SST data was from the daily group for the High-Resolution Sea Surface Temperature (GHRSST) Level 4 Multiscale Ultrahigh Resolution (MUR) analysis with the spatial resolution of 0.01° [12,13]. This dataset is based upon nighttime GHRSST L2P skin and subskin SST observations from several instruments, including the NASA Advanced Microwave Scanning Radiometer-EOS (AMSR-E), the JAXA Advanced Microwave Scanning Radiometer 2 on GCOM-W1, the Moderate Resolution Imaging Spectroradiometers (MODIS) on the NASA Aqua and Terra platforms, the US Navy microwave WindSat radiometer, the Advanced Very High Resolution Radiometer (AVHRR) on several NOAA satellites, and in situ SST observations from the NOAA iQuam project. This SST product has been evaluated against the in situ observations [14].
A semi-daily Advanced Scatterometer (ASCAT) with a spatial resolution of 0.125° × 0.125° was used for investigating the surface wind variation [15]. Furthermore, we used an hourly precipitation product from Global Satellite Mapping for Precipitation (GSMaP) with a spatial resolution of 0.1° × 0.1° [16]. GSMaP product was constructed from the Dualfrequency Precipitation Radar (DPR) onboard GPM core satellites, other GPM constellation satellites, and Geostationary satellites. In the present study, our analysis was based on the original spatial resolution of each dataset without any interpolation. In addition, we also analyzed the precipitation data obtained from meteorological stations at Makassar City and Majene Regency, as shown in Figure 1b.
On 8 September 2020, we conducted field observation in the sea around Barrang Caddi Island, which is part of the Spermonde Islands ( Figure 1). We took water samples from 26 stations and analyzed the Chl-a concentration and total suspended sediment (TSS). The detail methods of the field sampling and analysis can be found in Maslukah et al. [17].

Method
The method of this study was based on the climatological analysis from 13 years of data (2007-2019) of each variable. Firstly, hourly and semi-daily data were composited into daily data. Then, all daily data were composited into monthly and monthly climatology following Wirasatriya et al. [18], where ̅ ( , ) is the monthly mean value or monthly climatology value at position (x,y), xi (x,y,t) is i-th value of the data at (x,y) position and time t. Next, n is the number of days in a one month period and the number of months in one period of climatology for the monthly calculation and monthly climatology calculation, respectively. Furthermore, xi is excluded in the calculation if that pixel is hollow.

Spatial Distribution of Chl-a, SST, and Surface Wind
First, we present the spatial distribution of Chl-a, SST, and surface wind along the western coast of South Sulawesi in August ( Figure 2). The high Chl-a concentration appears in two areas. The first area is at 119.0° E-119.5° E; 3.5° S-4.0° S. In this area the high Chl-a concentration corresponds to the low SST and strong easterly wind. This strong easterly wind comes from the gap between the mountain ranges known as the expansion fan. The mechanisms of the strong wind off the wind gap are possibly due to the drop of the marine atmospheric boundary layer height after passing the gap, which accelerates the wind speed (e.g., [19,20]). The expansion fan phenomenon is also detected at the gap between the Gorontalo Mountain and the Sulawesi Mountain, described by Wirasatriya et al. [21]. Since the first area is located in the southern hemisphere, the strong easterly wind may generate southward offshore Ekman transport that causes coastal upwelling, reducing SST and enhancing Chl-a concentration. This offshore Ekman transport mechanism is also found in the coastal upwelling event along the southern coast of Java during the summer monsoon [22]. However, the magnitudes of enhancing Chl-a and reducing SST are less than those at the southern coast of the South Sulawesi, as described by Setiawan and Kawamura [5] and Utama et al. [6]. The second area is the Spermonde Islands, which are located at 119.0° E-119.5° E; 4.6° S-5.1° S. Unlike the first area, the enhancing Chl-a concentration at the second area in January does not relate to SST and surface wind speed ( Figure 3). The high Chl-a in the second area occurs under the weak wind and warm SST conditions. This may indicate that other factors, rather than wind speed, are influencing the high Chl-a concentration in the Spermonde Islands.

Temporal Analysis of Chl-a, SST, Surface Wind, and Precipitation
Temporal variability of SST, Chl-a, and wind speed are shown in Figure 4a. It is clearly shown that the variabilities of SSTs in both areas follow the variabilities of wind speed. The higher the wind speed, the lower SST will be, and vice versa. In contrast, the variabilities of Chl-a in both areas are almost independent of the variabilities of wind speed. There are two Chl-a peaks in the first area (thin box), which occur in August and April. Chl-a concentrations reach 0.41 mg/m 3 in August. This is related to the high wind speed of roughly 6.5 m/s that promotes coastal upwelling, as discussed in the previous section. In April, the concentration of Chl-a reaches its maximum (i.e., 0.55 mg/m 3 ), but this occurs under the condition of minimum wind speed (i.e., 1 m/s). Chl-a concentrations in the second area (thick line) are generally higher than those in the first area throughout the whole year, except for April, the first area's peak. The whole monthly climatology of Chl-a is higher than 0.39 mg/m 3 . An outstanding maximum Chla concentration occurs in January when Chl-a concentration reaches 0.6 mg/m 3 . However, the variability of Chl-a concentration in the second area is not consistent with the variability of wind speed. Although intense wind speed in January may contribute to the increase of Chl-a concentration, August's most vigorous wind speed does not result in the highest Chl-a. Therefore, another factor controls the occurrence of the highest Chl-a concentration in the first (second) area in April (January).
To address the incongruity of the relationship between wind speed and Chl-a, we plot the temporal variability of precipitation and Chl-a in both areas in Figure 4b. We extend the average precipitation area to the upland area to account for the potential impact of the river runoff during the rainy season. We also plot the precipitation observed from meteorological stations at Majene Regency and Makassar City, which represent the first and second areas, respectively. The variability of precipitation derived from satellites have similar pattern with the observed precipitations. The amplitude difference during the peak of precipitation may be due to the areal representative differences of both data. The peak of Chl-a concentration in January at the second area and in April at the first area corresponds to precipitation. Thus, the variability of the Chl-a concentration in both areas is more strongly influenced by precipitation. This finding is supported by the correlation analysis presented in Table 1. SST versus wind speed has strong negative correlations in both areas, indicating that SST is highly dependent on wind speed. The correlation coefficient between Chl-a and wind speed, on the other hand, is minimal, which is ≤0.4. The higher correlations are shown by Chl-a versus precipitation i.e., 0.43 and 0.51 for the first and second areas, respectively. This means that the precipitation has a greater impact on Chl-a variation than wind speed. The terrestrial nutrient input brought by river runoff during the rainy season may be the mechanism by which precipitation influences Chl-a variation. As shown by Maslukah et al. [23], the phosphate influx in the northern shore of Java is driven by river runoffs that transport organic materials. However, combining the independent variables of wind speed and precipitation may have a greater impact on Chla variability than each variable alone. The correlation coefficients for the first and second areas increased to 0.46 and 0.58, respectively. This finding could explain how wind speed affects Chl-a regulation during the boreal summer monsoon.

Possibility of Suspended Sediment That Bias the Observed Chl-a Concentration
The nutrient influx from river runoff may come along with the organic sediment particles, increasing the turbidity in the coastal seas, then possibly turning the study area into case-2 waters. The NASA OC4v4 standard algorithm, on the other hand, was used to extract the standard Chl-a product, which is only suited for case-1 waters and may fail to recover Chl-a consistently in case-2 waters [24]. This section examined the presence of suspended sediment that could influence the Chl-a value in the western coast of South Sulawesi by using Rrs 443 and 555 ( Figure 5). This method has also been used by Wirasatriya et al. [25] for examining the potential contamination of satellite Chl-a measurements by suspended sediment within the Indonesian sea. Low Rrs 443 appears in the first and second areas, corresponding to phytoplankton biomass's existence in both areas. However, low Rrs 555 is only detected in the first area. This means that the observed Chl-a concentration in the first area is not contaminated by suspended sediment. In contrast, high Chl-a concentration in the second area is co-located with the high Rrs 555. Furthermore, the area with low Rrs 443 (high Rrs 555) corresponds to the area with high aph 443 (high bbp 555), which denotes the high phytoplankton absorption coefficient at 443 nm, and the high particulate backscattering coefficient, at 555 nm. Thus, the observed Chl-a in the second area may be biased by the condition of turbid water. A further explanation is depicted in the scatter plots shown in Figure 6. For the relation between Rrs 443 and Chla, both areas show the same tendency i.e., the lower Rrs 443, the higher Chl-a (Figure 6a,c). However, this relation is more scattered in the second area, indicating the stronger bias in the second area than the first area. In the first area, the Rrs 555 is low, distributed from 1.2 × 10 −3 sr −1 -3.2 × 10 −3 sr −1 . This explains the low suspended sediment in the first area. In contrast, the high Rrs 555 in the second area, distributed from 2 × 10 −3 sr −1 -4.5 × 10 −3 sr −1 (Figure 6b,d) indicates the existence of high suspended sediments, which may bias the Chl-a measurement. This result is supported with an in situ observation, as shown in Figure 7. Although the correlation is weak and the coefficient of determination is low, we still can see the linear trend, which shows the higher the Chl-a, the higher the TSS concentration. The weak correlation between in situ Chl-a and in situ TSS is common in the coastal waters, as also shown by Maslukah et al. [26], probably due to the limitation of the data population. We also cannot obtain the correlation between the Chl-a satellite and in situ Chl-a, due to the cloudy condition during field observation. Thus, the high Chl-a observed in the second area is contaminated by the high-suspended sediment. Further investigation is needed to obtain the typical algorithm for estimating Chl-a in the second area, which is classified as case-2 water. This task is left for future study. As shown earlier, the suspended sediment in the first area is lower than that in the second area. This could be because the first area receives less precipitation than the second. Furthermore, as shown in Figure 1, the difference in land cover between areas may contribute to the varying sediment influx between the two areas. The upland side of the second area has more rivers than the first, which pass through the agricultural and urban areas. The sediment influx from the upland area brought by the river runoff during the rainy season that passes through the agriculture and urban areas is responsible for the high-suspended sediment at the high Chl-a areas. Therefore, it may suggest that the anthropogenic activities in the upland area determine the organic sediment matter that influences Chl-a concentration in both areas.

Discussion
The previous study has shown that the southern coast of South Sulawesi is known as the high Chl-a area occurring during the boreal summer monsoon, which peaks in August [5,6]. In terms of magnitude, the highest Chl-a concentration at the second area on South Sulawesi's western coast, which reaches 0.65 mg/m 3 , is lower than the southern coast, which reaches 1.4 mg/m 3 [5]. This may be related to the different generating mechanisms at the western and southern coasts of South Sulawesi. The strong upwelling at the southern coast of South Sulawesi may bring more nutrient-rich water than the river runoff due to the heavy rain. Nevertheless, the Chl-a concentration at the second area is higher than the other upwelling areas, such as in the Maluku Sea (e.g., [18,21,27]). This may correspond to the speed of wind-generated offshore; Ekman transport at the Maluku Sea is less than that at the southern coast of South Sulawesi. As a major path for monsoon wind, the wind speed along the southern coast of South Sulawesi is stronger than that at the Maluku Sea [28]. By conducting the climatological analysis, the present study enhances the seasonal variation of Chl-a along the western coast of South Sulawesi. Further, it is also important to investigate its inter-annual variation. As summarized by Wirasatriya et al. [25], the effect of El Niño Southern Oscillation on the magnitude of upwelling within the Indonesian Seas depends on the season. During summer or southeast monsoon season, El Niño (La Niña) tends to increase (decrease) upwelling intensity. Conversely, the intensity of northwest monsoon upwelling reduces (increases) during El Niño (La Niña). Furthermore, for the Chl-a variation in the coastal area, Siswanto et al. [4] showed that Chl-a concentration declines (increases) most notably during the concurrent positive Indian Ocean Dipole (IOD) and El Niño (negative IOD and La Niña) events. Since the area along the western coast of the South Sulawesi was not discussed in both previous studies, understanding the impact of the inter-annual climate variability to the Chl-a along the western coast of South Sulawesi will be beneficial for fisheries management in this area. This task is left for future study.
It is worth noting that the number of high Chl-a zones identified in Indonesian waters influenced by river runoff is still smaller than the upwelling areas. Wirasatriya et al. [25] have collected and identified upwelling locations in the Indonesian seas during the summer and rainy seasons. On the other hand, Siswanto et al. [4] found that, except for the coastal area of the northern Malacca Strait, the Chl-a variations at the coastal areas within the Indonesian seas are primarily influenced by the riverine nutrient fluxes and vary with the climatic events. As presented in the present study, the detailed feature of Chl-a blooms along the western coast of South Sulawesi during the rainy season is one example of how rainfall may influence Chl-a variation through the river runoff. This may trigger more investigation of other high Chl-a areas during the rainy season within the Indonesian Seas. However, careful interpretation of satellite-based Chl-a data should apply, as riverine organic/inorganic matter may bias the satellite Chl-a reading. Thus, collecting in situ data of Chl-a and suspended matter along the western coast of South Sulawesi and other coastal areas becomes the most valuable task to guarantee the accuracy of the satellite Chl-a reading. Further, it can be used to reproduce the new algorithm for the satellite-based Chl-a in those specified areas. This work is left for future study.

Conclusions
By taking advantage of blended products of satellite-based Chl-a data, we revealed the spatial and temporal variation of the Chl-a along the western coast of South Sulawesi. Two areas have been identified as high primary productivity areas occurring during the rainy season. The first and second areas are located at 119.0° E-119.5° E; 3.5° S-4.0° S and 119.0° E-119.5° E; 4.6° S-5.1° S, respectively. The monthly Chl-a variation in the first and second areas range from 0.35 mg/m 3 to 0.55 mg/m 3 and from 0.39 mg/m 3 to 0.6 mg/m 3 , respectively. The highest Chl-a concentration is observed in April and January for the first and second areas, respectively. The generating mechanism of the high Chl-a along the western coast of South Sulawesi is different from its southern coast, which is known as the coastal upwelling area. The existence of river runoff in these two areas may bring anthropogenic organic compounds during the peak of the rainy season, which increases the Chl-a concentration at the western coast of South Sulawesi.