From 2010 to 2014, eight anchored diel studies were conducted at the SEATS station (18°N, 116°E; Figure 1) in the northern SCS. Eight diel studies were categorized as representatives of the four seasons (Table 1). Seawater was collected from 4 to 8 depths within the upper 100 m every 3–6 h (see Supplementary Figures for detailed sampling information) for at least 24 h using a rosette sampler with 20-L Teflon-coated X-Niskin bottles (General Oceanics, Miami, FL, USA) and a mounted CTD (Seabird, Bellevue, WA, USA). In addition to temperature and salinity, depth profiles of underwater PAR (Chelsea Technologies, UK), fluorescence, and transmission were also recorded. The mixed layer depth (MLD) was defined at which a density (sigma-t) change of 0.125 kg m⁻³ from the surface occurred (Vaulot and Marie, 1999).

Nutrient (nitrate, nitrite, phosphate, and silicate) samples were collected in acid-washed polypropylene bottles, immediately frozen in liquid nitrogen on board, transferred, and kept at −20°C in the laboratory until analysis. Nitrate was reduced to nitrite using cadmium-copper filings, and concentrations were determined by the diazo-pink method (Parsons et al., 1984). Nitrite concentrations were determined the same way as nitrate concentration but excluding the reduction process. Phosphate concentrations were determined by the molybdenum-blue method (Parsons et al., 1984), and silicate concentrations were determined by the molybdate-blue method (Parsons et al., 1984). The dissolved organic carbon (DOC) concentrations were determined by the high-temperature catalytic oxidation (HTCO) method on a Shimadzu TOC-V (Japan) analyzer (Wurl, 2009). Samples (2 L) for chlorophyll-a (Chl-a) were collected on GF/F filters (Whatman, Marlborough, MA, USA) and kept at −20°C until analysis. Chl-a was extracted with 90% acetone, and concentrations were determined using a fluorometer (Turner Designs, San Jose, CA, USA) (Parsons et al., 1984).

Picoplankton abundance was determined by flow cytometric counting. Subsamples of 2 ml for flow cytometry were preserved with paraformaldehyde (0.2%, final concentration), placed in liquid nitrogen, and stored at −80°C until analysis (Campbell et al., 1997). A flow cytometer (PARTEC, Germany) equipped with a 488-nm laser was used to count picoplankton (Marie et al., 1999). Forward and side light scatters and green, red, and orange fluorescence were collected and analyzed using FlowMax software to identify three major groups of picophytoplankton (Prochlorococcus, Synechococcus, and picoeukaryotes) and heterotrophic bacteria. Fluoresbrite yellow-green beads (1 μm; Polysciences, Warrington, PA, USA) were used as internal standards. Heterotrophic bacteria were counted in separate subsamples stained with SYBR Green I (Molecular Probes, Eugene, OR, USA) (Marie et al., 1999). Carbon conversion factors were adopted from previous studies. The carbon conversion factors for Prochlorococcus, Synechococcus, and picoeukaryotes were 32, 100, and 1,500 fg C cell⁻¹ (Zubkov et al., 1998), respectively, while a cellular carbon content of 20 fg C cell⁻¹ was used for heterotrophic bacteria (Lee and Fuhrman, 1987).

JMP software (SAS Institute, USA) was used for statistical analysis. Unless otherwise indicated, variation around each mean is presented as +/– one standard deviation. All depth averages were calculated as the integrations down to 100 m divided by 100.

The sea surface temperature (SST) and the mixed layer depth (MLD) are presented in Table 1. The SST showed obvious seasonal differences with small diel changes (Table 1; Supplementary Figure 1). The SSTs of 24.78 ± 0.16 and 25.71 ± 0.08°C in the winter (December 2011 and 2013, respectively) were significantly lower than those in the other seasons (mean SST ranged from 26.99 to 29.26°C) with very small diel variations (coefficient of variance, CV%, ranging from 0.2 to 0.7%). On the other hand, the seawater temperature at a depth of 100 m had a relatively narrow range (see Supplementary Figure 1; mean temperature ranged from 18.34 to 21.62°C) with a diel CV% of 1.2 to 4.4%. The MLD displayed a similar pattern to that of SST but with larger diel variations (Table 1; Supplementary Figure 1). The MLD values of 55.6 ± 5.6 and 45.6 ± 28.5 m in the winter (December 2011 and 2013, respectively) were deeper than those in the other seasons (mean MLD ranged from 21.7 to 37.8 m) with relatively large diel variations (CV% ranged from 8.2 to 62.4% and a maximum/minimum factor of 1.29 to 12.7). The large diel variability in the MLD indicated a dynamic physical environment in the interior of the water column during a 24-h period. Nitrate concentrations were homogeneous under the detection limit in the upper ocean (see Supplementary Figure 2) and were high at depths of 100 m (>5 μm). Nitracline depth (defined as the depth where nitrate concentration equals 1 μm) was fairly consistent at depths of ~60 m (see Supplementary Figure 2). Phosphate and silicate concentrations exhibited vertical and temporal distributions similar to those of nitrate, showing depleted or low concentrations at the surface (Supplementary Figures 3, 4). Dissolved organic carbon (DOC) concentrations exhibited typical vertical distributions in the open ocean, ranging from 70 to 100 μm at the surface and decreased to 50–60 μm at a depth of 100 m (Supplementary Figure 5).

The Chl-a concentration generally displayed a subsurface chlorophyll maximum (SCM) except in the winter of 2011 (see Supplementary Figure 6). The SCM was consistently located at a depth of ~50 m except in the spring of 2013 (~80 m). In the winter of 2011, Chl-a appeared high at the surface and decreased with depth. Generally, Chl-a concentration was <0.7 mg m⁻³. For seasonal variation, the depth-averaged Chl-a concentration showed high values of 0.32 ± 0.09 mg m⁻³ in the winter and a range of 0.18 to 0.21 mg m⁻³ in the other seasons (Table 1). The CV% of Chl-a diel variability ranged from 9.7 to 32.1% with an average of 22 ± 9%, while the maximum/minimum factor ranged from 1.3 to 2.6 with an average of 2 ± 0.5.

Prochlorococcus abundance was generally low at the surface and displayed a subsurface maximum in warm seasons (spring, summer, and fall; see Supplementary Figure 7), ranging from 3.1 to 9.9 × 10⁴ cells ml⁻¹ at the surface and reaching up to 13.9 × 10⁴ cells ml⁻¹ in the mid-layer except in the fall of 2010. Prochlorococcus was the most abundant in the fall of 2010, with 24.1 × 10⁴ cells ml⁻¹ as the subsurface maximum. The subsurface maximum of Prochlorococcus disappeared in the winter with decreasing depth-averaged cell numbers (1.8 ± 0.6 and 4.6 ± 1.1 × 10⁴ cells ml⁻¹ in the winter of 2011 and 2013, respectively). Synechococcus abundance was generally high at the surface and decreased with depth (see Supplementary Figure 8). The depth-averaged abundance of Synechococcus in the upper 50 m ranging from 4.2 to 8.4 × 10³ cells ml⁻¹ was higher than those of 1.8 to 3.6 × 10³ cells ml⁻¹ in the depth between 50 and 100 m except in the winter of 2013. Synechococcus abundance in the winter of 2013 was 10 times more abundant than that of other investigated seasons, at 90.9 ± 17.3 × 10³ cells ml⁻¹ in the upper 50 m of the ocean. The vertical distribution of picoeukaryotes was similar to that of Prochlorococcus, which displayed a subsurface maximum in the warm seasons and was relatively homogeneous in the winter (see Supplementary Figure 9). Generally, the subsurface maximum of picoeukaryotes ranged between 4 and 8 × 10³ cells ml⁻¹, located mostly at depths of 40 to 60 m. In the winter of 2011, picoeukaryotes abundance was approximately double that of the other seasons and reached 13.9 × 10³ cells ml⁻¹.

Heterotrophic bacteria accounted for the major component of the picoplankton community. Heterotrophic bacteria were ubiquitous in the water column and slightly more abundant at the surface (see Supplementary Figure 10). The heterotrophic bacterial abundance ranged from 1.2 to 11 × 10⁵ cells ml⁻¹ at the surface and from 0.7 to 3.9 × 10⁵ cells ml⁻¹ at a depth of 100 m.

Despite the existence of the vertical variability in picoplankton, depth-averaged abundance better described the seasonal variability. Prochlorococcus occurred at high-abundance levels in the warm seasons (i.e., spring, summer, and fall; ranging from 5.88 to 9.43 × 10⁴ cells ml⁻¹) and at low-abundance levels of 1.85 ± 0.56 and 4.61 ± 1.12 × 10⁴ cells ml⁻¹ in the winter of 2011 and 2013, respectively (Table 1). Synechococcus, by contrast, occurred at low-abundance levels in the warm seasons (ranging from 3.14 to 4.86 × 10³ cells ml⁻¹) and at high-abundance levels of 6.01 ± 1.71 × 10³ cells ml⁻¹ and an extremely high abundance of 57.13 ± 11.25 × 10³ cells ml⁻¹ in the winter of 2011 and 2013, respectively (Table 1), at approximately an orderly less abundant than that of Prochlorococcus in terms of cell numbers. Similar to Synechococcus, the seasonal pattern of picoeukaryotes showed low values of 1.08 to 2.53 × 10³ cells ml⁻¹ in the warm seasons and high values of 6.18 ± 1.75 and 2.41 ± 0.36 × 10³ cells ml⁻¹ in the winters of 2011 and 2013, respectively (Table 1). Prochlorococcus was the most abundant autotrophic picoplankton in the warm seasons, accounting for 92.1 ± 1.8% of the total picophytoplankton cell numbers. The picophytoplankton community structure substantially changed in the winters. In the winter of 2011, Prochlorococcus was still the most abundant with a smaller fraction of 59.8 ± 6.3%, followed by picoeukaryotes (20.2 ± 2.1%) and Synechococcus (20 ± 5.1%). In the winter of 2013, Synechococcus became the most abundant picophytoplankton (54.1 ± 9.8%), followed by Prochlorococcus (43.6 ± 9.8%) and picoeukaryotes (2.3 ± 0.3%).

Integrated autotrophic picoplankton carbon biomass in the upper 100 m showed high values in the winter (1.046 ± 0.289 and 1.080 ± 0.114 g m⁻² for 2011 and 2013, respectively) and ranged from 0.414 to 0.628 gm⁻² in the warm seasons (Figure 2). Picoeukaryotes and Prochlorococcus were the major components of autotrophic picoplankton biomass in the warm seasons, accounting for 48.7 ± 8.6 and 43.3 ± 7.7% of the biomass, respectively. However, contributions to picophytoplankton carbon biomass were variable in the winter. In the winter of 2011, picoeukaryotes dominated the autotrophic picoplankton biomass (accounting for 88.5 ± 1.2%), followed by Synechococcus (5.8 ± 1.3%) and Prochlorococcus (5.7 ± 1.3%). In the winter of 2013, Synechococcus became the dominant group of picophytoplankton (contributing 52.6 ± 6.7%), followed by picoeukaryotes (33.5 ± 3.9%) and Prochlorococcus (13.9 ± 4.2%).

Heterotrophic bacteria were the major component of the picoplankton community in terms of both abundance and biomass. Heterotrophic bacterial abundance ranged from 1.77 to 6.37 × 10⁵ cells ml⁻¹, showing an insignificant seasonality (Table 1). Heterotrophic bacterial biomass generally exceeded or equaled the total picophytoplankton biomass, ranging from 0.353 to 1.300 gm⁻² in warm seasons and 1.274 ± 0.113 and 1.003 ± 0.106 gm⁻² in the winters of 2011 and 2013, respectively (Figure 2).

Picoplankton abundance in some investigations showed clear diel cycles (Figure 3; see more detail in Section 4.3). Synechococcus abundance (data from OR1_1103, OR1_944, and OR1_1053) peaked at 1 a.m. (Figure 3B), followed by Prochlorococcus (peaking at 2 a.m.) based on data from OR1_944, OR1_1053, and OR1_1060 (Figure 3A). Picoeukaryotes peaked at ~7 to 8 p.m. based on data from OR1_1034, OR1_1010, OR1_944, and OR1_988 (Figure 3C). Diel variation occurred in two types for heterotrophic bacteria: the night-peak group, including OR1_944 and OR1_1053, which peaked at 7 p.m. (Figure 3D), and the day-peak group, including OR1_1034, OR1_1010, OR1_1084, and OR1_1060, which peaked at noon (Figure 3E). In addition to diel patterns, the results also showed large variations among frequent samplings (Table 1). The CV% of depth-averaged Prochlorococcus abundance ranged from 9 to 30.3% with an average of 22 ± 6.2%, while the maximum/minimum factor ranged from 1.3 to 2.3 with an average of 1.9 ± 0.3. Diel variation in Synechococcus abundance was larger than that in Prochlorococcus abundance. The CV% of Synechococcus ranged from 14.9 to 37.6% with an average of 26.6 ± 8.5%, while the factor ranged from 1.5 to 2.9 with an average of 2.1 ± 0.4. Picoeukaryotes showed the largest diel variation in abundance. The CV% of picoeukaryotes ranged from 8.8 to 64.5% with an average of 30.9 ± 19.2%, while its factor ranged from 1.3 to 6.6 with an average of 2.8 ± 1.8. Heterotrophic bacteria seemed to have the least diel variation. The CV% of heterotrophic bacterial abundance ranged from 6.6 to 33% with an average of 15.7 ± 9%, while the factor ranged from 1.2 to 2.3 with an average of 1.6 ± 0.4.

Picophytoplankton was mostly observed within the upper 100 m and had insignificant numbers below a depth of 150 m at SEATS station in the South China Sea (Liu et al., 2007). Prochlorococcus and picoeukaryotes tended to accumulate at subsurface depths of mostly ca. 40 to 60 m in the warm seasons (Supplementary Figures 7, 9), while Synechococcus tended to peak at the surface (Supplementary Figure 8). Such a difference in vertical distribution between Prochlorococcus and Synechococcus is well recognized (Campbell et al., 1997; Durand et al., 2001), indicating different light adaptation strategies (Ting et al., 2002). Prochlorococcus seemed to be well adapted to low light (Partensky et al., 1993) and had higher absorption efficiency for blue light, which is predominant in deep waters (Morel et al., 1993), favoring the formation of subsurface maxima. Moreover, Prochlorococcus was also ultraviolet sensitive, which could induce DNA damage (Boelen et al., 2000) and, therefore, restrict Prochlorococcus growth at the surface. On the other hand, Synechococcus developed a phycobilisome antenna system, which contained phycobiliproteins (for example, phycoerythrin and phycocyanin) and had a high capability for light-harvesting at the surface (Biller et al., 2015). Boelen et al. (2000) also found that, in comparison to Prochlorococcus, Synechococcus was more resistant to UVB damage. These factors helped to form the difference in the vertical distributions between Prochlorococcus and Synechococcus. Picoeukaryotes peaked at subsurface depths in the warm seasons along with the subsurface chlorophyll maximum. The subsurface maximum of Prochlorococcus, picoeukaryotes, and Chl-a disappeared during the winter, which was also observed in Liu et al. (2007). Winter mixing broke water column stability and the subsurface maximum. After strong mixing, the stratification and then the subsurface maximum were reestablished in the following warm seasons (Olson et al., 1990; Li, 1995). The vertical distribution of heterotrophic bacterial abundance appeared high at the surface and gradually decreased with depth (Supplementary Figure 10), corresponding to the DOC concentrations (Supplementary Figure 5). Heterotrophic bacteria accompanied with total DOC were also reported in the Mediterranean Sea, indicating a tight coupling with photosynthetically released DOC (Gasol et al., 1998). Overall, the vertical distributions of picoplankton were affected by the depths associated with surrounding environmental parameters (including light, temperature, and substrate/nutrient supply).

Seasonal variation in picophytoplankton communities has been recorded in tropical and subtropical oceans (Campbell et al., 1997; Durand et al., 2001; Liu et al., 2007). Our results showed that Prochlorococcus abundance appeared low in the winter and higher with insignificant differences among the warm seasons. Synechococcus abundance peaked in the winter and decreased but was relatively constant in the warm seasons. Picoeukaryotes abundance did not have a clear seasonal pattern with exceptionally high values in the winter of 2011. These observations were slightly different from those in the report at the subtropical Bermuda Atlantic Time-Series Study (BATS) station, where Prochlorococcus abundance peaked in the summer and fall and had low cell numbers in the winter, while Synechococcus and picoeukaryotes abundance peaked during the spring bloom and decreased in the summer (Durand et al., 2001). Compared to a previous survey at the SEATS station, Liu et al. (2007) observed similar seasonal patterns as those of BATS, showing that Prochlorococcus peaked in the summer and appeared low in the winter, whereas Synechococcus and picoeukaryotes peaked in the winter and decreased in the summer. However, more complicated seasonal patterns were observed at the Hawaiian Ocean Time-Series (HOT) station ALOHA (Campbell et al., 1997). At the HOT station, Prochlorococcus showed a minimum abundance in the winter but an unclear seasonal pattern in the warm seasons. Synechococcus and picoeukaryotes usually peaked in the winter and early spring. However, such peaks did not appear every year. In this study, we found that the seasonal variation in picophytoplankton at the SEATS station was more similar to that at the HOT station than to previous observations. In summary, picophytoplankton at the SEATS station could be distinguished between warm and cold seasons. This phenomenon could be partially explained by Bunse and Pinhassi (2017), who suggest that the seasonality of picoplankton could become less obvious when approaching the equator. However, the different results from those of previous observations at the SEATS station indicated that the seasonal succession dynamics of the picoplankton community structure in the South China Sea might be more complicated than previously thought.

Heterotrophic bacterial abundance was high in the winter and spring based on a previous study at the SEATS station (Liu et al., 2007). However, we observed an unclear seasonal pattern of heterotrophic bacterial abundance (Table 1). Heterotrophic bacterial abundance has been reported to peak in the summer at the BATS station (Carlson and Ducklow, 1996), while high abundance appeared in summer and fall at the HOT station (Campbell et al., 1997). However, undetectable seasonality in heterotrophic bacterial abundance has also been reported in the subtropical Red Sea (Al-Otaibi et al., 2020).

In terms of cell numbers, Prochlorococcus was the most abundant picophytoplankton. Our Prochlorococcus abundance (depth-averaged mean ranging from 1.85 to 9.43 × 10⁴ cells ml⁻¹) was at the lower end of the tropical and subtropical reports, at 18.3 ± 11.1 × 10⁴ cells ml⁻¹ in the North Atlantic Ocean (Buck et al., 1996) and 17.6 × 10⁴ cells ml⁻¹ at the HOT station (Table 2, Campbell et al., 1997). Synechococcus abundance (depth-averaged mean ranging from 3.14 to 6.01 × 10³ cells ml⁻¹), on the other hand, was comparable to 9.3 ± 13 × 10³ and 1.4 × 10³ cells ml⁻¹ in the North Atlantic and the North Pacific Subtropical Gyre, respectively (Table 2, Buck et al., 1996; Campbell et al., 1997). Mann et al. (2002) found that Prochlorococcus is inhibited by free copper, whereas Synechococcus is resistant to copper. However, whether the low abundance of Prochlorococcus at the SEATS station is due to copper toxicity needs further investigation. The abundance of picoeukaryotes (depth-averaged mean ranging from 1.08 to 6.18 × 10³ cells ml⁻¹) was at the higher end of the global subtropical and tropical values (1.7 ± 0.1 × 10³ cells ml⁻¹; Table 2) (Agusti et al., 2019). The different picophytoplankton community structures reflected biomass carbon composition at the SEATS station.

The integrated biomass of total picophytoplankton ranged from 0.414 to 1.080 g C m⁻² in this study, which is comparable to previous investigations (Liu et al., 2007). However, the contributions from the three picophytoplankton groups were quite different from the previous study from the same station and other subtropical reports. Prochlorococcus has been recognized as the major component of biomass in tropical and subtropical regions. At the HOT station, Prochlorococcus accounted for 72.6 ± 16.6% of the total picophytoplankton biomass, followed by picoeukaryotes (24.2 ± 11.5%) and Synechococcus (3.2 ± 1.9%) (Campbell et al., 1997). In the investigation at the STEATS station by Liu et al. (2007), Prochlorococcus constituted 70 to 80% of the picophytoplankton biomass in the summer and fall and decreased to less than 40% in the winter, whereas Synechococcus became more important in the winter. In our results, picoeukaryotes and Prochlorococcus displayed equal importance in the warm seasons (accounting for 48.7 ± 8.6% and 43.3 ± 7.7% of the total picophytoplankton biomass, respectively). Picophytoplankton community dynamics during the winter in the SCS appear complicated. Liu et al. (2007) found a “winter bloom” of Synechococcus and picoeukaryotes in 2001 and 2002, respectively. Similar phenomena appeared in this study, with a “winter picoeukaryotes bloom” (88.5 ± 1.2% of picophytoplankton biomass) in 2011 and a “winter Synechococcus bloom” (52.6 ± 6.7% of picophytoplankton biomass) in 2013, while Prochlorococcus decreased to less than 15% of the total picophytoplankton biomass. The strong winter mixing (deeper MLD) accompanied by more available nutrients could possibly drive the winter bloom of relatively larger-sized groups of picoeukaryotes and Synechococcus.

Heterotrophic bacteria had undetectable seasonality in this study. Their abundance of 1.77 to 6.50 × 10⁵ cells ml⁻¹ was slightly less but still comparable to that in the North Atlantic Ocean (6.59 ± 3.42 × 10⁵ cells ml⁻¹) (Buck et al., 1996), the HOT station (7.10 ± 0.16 × 10⁵ cells ml⁻¹) (Campbell et al., 1997), and the previous SEATS station (2.5 to 12 × 10⁵ cells ml⁻¹) (Liu et al., 2007). The integrated biomass of heterotrophic bacteria generally exceeded that of autotrophic picoplankton (six out of eight; Figure 2), ranging from 0.353 to 1.300 g m⁻². In contrast, autotrophic picoplankton-exceeding heterotrophic bacteria have been previously reported at the SEATS station (Liu et al., 2007). This was basically due to the choice of bacterial carbon conversion factors. The cellular carbon content of 11 fg cell⁻¹ in Liu et al. (2007) led to approximately a half of bacterial biomass compared with a commonly used estimate of 20 fg cell⁻¹. In fact, heterotrophic bacteria are more important in terms of biomass in tropical and subtropical oceans than in other oceans. For example, a basin-wide investigation from the equator to 20°N in the North Atlantic Ocean suggested that the overall integrated biomass of heterotrophic bacteria slightly surpassed that of autotrophic picoplankton (Buck et al., 1996).

During the eight diel surveys, diel patterns of picoplankton were not clear from an individual data set. Therefore, we transformed the depth-averaged abundance as follows and superimposed it on a 24-h scale.

where A_n,t and A_t denote the normalized and original depth-averaged abundance at the time t during a given cruise, respectively;  At¯ denotes the arithmetic mean of the depth-averaged abundance during the given cruise; and σ(A_t) denotes the standard deviation of the depth-averaged abundance during the given cruise. After normalization, a non-linear fitting was conducted.

where X and Y denote the time in 24 h and the predicted A_n,t, respectively. A₀, A₁, and A₂ denote fitting coefficients. The results showed that three out of eight cruises for Synechococcus peaked at 1 a.m. (Figure 3B), followed by Prochlorococcus (also three out of eight cruises), peaking at ~2 a.m. (Figure 3A). These diel patterns were similar to those in the equatorial Pacific, where Synechococcus peaked at 12 a.m., followed by Prochlorococcus peaking at 2 a.m. (Vaulot and Marie, 1999). Our picoeukaryotes (four out of eight cruises), on the other hand, peaked at ~7 to 8 p.m., which was similar to observations in the equatorial Pacific (Blanchot et al., 1997). In fact, the timing of division from various strains in a given picophytoplankton group could be variable (Jacquet et al., 2001). Generally, phytoplankton tends to photosynthesize and grow during the daytime, followed by division during the night (Durand and Olson, 1998). In addition to intrinsic genetics (Jacquet et al., 2001), the phasing of cell division in natural environments could be regulated by light intensities (Vaulot et al., 1995) and nutrient conditions (Vaulot et al., 1996), possibly causing different diel patterns.

Heterotrophic bacteria exhibited two different diel patterns. The night-peak type had a high abundance at 7 p.m. (Figure 3D), whereas the day-peak type exhibited a high abundance at noon (Figure 3E). These two opposite diel patterns were also observed in the Mediterranean Sea (Gasol et al., 1998). Bacteria peaking during the daytime are usually subjected to high-bacterial production associated with the release of photosynthetically fixed carbon (Gasol et al., 1998). On the other hand, bacterial abundance peaking at night usually corresponds with picophytoplankton increases (e.g., Lefort and Gasol, 2014).

Although we expected to see diel patterns in picoplankton, many of the cruises in this study did not present a clear 24-h periodicity. Previous studies have also shown a lack of diel periodicity in picoplankton (Jacquet et al., 1998; Lefort and Gasol, 2014). In fact, cell abundance tightly reflects the combination of gain and loss terms. Cell division, as the major gain term, usually exhibits its intrinsic “biological clock”(Johnson et al., 1996). However, the lost terms, including viral lysis, predator grazing, and physical processes, such as disturbance or advection, could play an important role in shaping the diel patterns. Viral lysis may account for daily losses of up to 20% of picoplankton (Suttle, 1994; Mojica et al., 2016), while grazing could be equivalent or more important than cell lysis (Pernthaler, 2005). Sherr et al. (1992) found preferential protozoa grazing on dividing prokaryotes. Peters (1994) further estimated that the protozoan ingestion rate increases by ~70% when prey is divided at 100%. Moreover, the diel pattern of heterotrophic nanoflagellates (HNF) directly affects picoplankton diel cycles. HNF has been observed as high-grazing rates during either day (Ng and Liu, 2016) or night (Christoffersen, 1994). Physical processes could have both positive and negative effects on picoplankton abundance, essentially due to the mixing of different water masses. Generally, mixing and turbulence increase nutrient fluxes for picoplankton growth. However, Peters and Gross (1994) observed that turbulence enhanced protozoan grazing rates on picoplankton-sized particles. Lefort and Gasol (2014) further suggested that a climate event with increased turbulence potentially disrupts the diel pattern of picoplankton. All loss terms may shape, weaken, or even dissipate the diel patterns.

Whether picoplankton displayed diel patterns, large diel variabilities were clearly observed. Picoeukaryotes had the largest CV% at 30.9 ± 19.2%, followed by Synechococcus (26.6 ± 8.5%), Prochlorococcus (22. ± 6.2%), and heterotrophic bacteria (15.7 ± 9.1%). The results were similar to, although slightly higher than, those in the Mediterranean, which also showed the highest CV% of picoeukaryotes (30%), followed by Synechococcus (16.5%), Prochlorococcus (16.5%), and heterotrophic bacteria (10.5%) (Lefort and Gasol, 2014). However, the maximum/minimum factor for picophytoplankton, ranging from 1.9 to 2.8, is apparently larger than that of ~1.5 in the equatorial Pacific (André et al., 1999).

Prochlorococcus has usually been observed in high temperature and low-nutrient waters, while Synechococcus and picoeukaryotes are frequently dominant in relatively low-temperature waters with higher nutrient concentrations (Partensky et al., 1999). Among the factors that may regulate picoplankton distribution, temperature and nutrient concentration have been recognized to potentially affect picoplankton community size structure (Morán et al., 2010; Marañón et al., 2012). Morán et al. (2010) suggested that a temperature rise could lead to a shift toward smaller primary producers. From a geographical point of view, the contribution of picophytoplankton to total phytoplankton biomass increases when moving from temperate regions to the equator (Marañón et al., 2001). However, Marañón et al. (2012) suggested that temperature is independent of the picoplankton community structure. On the other hand, nutrient availability controls the partitioning of biomass between different picoplankton groups. A geographical distribution where a higher fraction of picoplankton biomass appeared in oligotrophic oceans than in coastal-nutrient-replete waters supports the resource control hypothesis (Marañón et al., 2001). We found that the contribution of picophytoplankton to total phytoplankton biomass appeared to not be significantly affected by temperature or nutrient supply (represented as the MLD). The MLD has long been considered an indicator of the nutrient supply and was used for the estimate of phytoplankton growth (e.g., Sverdrup, 1953; Yentsch, 1990). Although temperature and nutrient supply hypotheses were rejected in this study, we observed that the sea surface temperature (SST) and the MLD could both well predict the seasonal fluctuations in picophytoplankton biomass (Table 3), with better correlations with SST (Table 3; Figure 4). Unfortunately, none of the SST or MLD presented suitable predictions for heterotrophic bacterial biomass. Prochlorococcus biomass was positively correlated with SST (p < 0.01) and negatively correlated with MLD (p < 0.05). On the other hand, Synechococcus biomass was negatively correlated with SST (p < 0.01). Picoeukaryotes were similar to Synechococcus, showing a negative correlation with SST and a positive correlation with MLD (both p < 0.05). Total picophytoplankton biomass behaved as larger-size groups of picoeukaryotes and Synechococcus, showing a negative correlation with SST and a positive correlation with MLD (both p < 0.01). The positive correlation with temperature and negative correlation with nutrient supply in Prochlorococcus biomass were consistent with global regressions in tropical and subtropical oceans (Agusti et al., 2019). However, the negative correlation between temperature and Synechococcus (and picoeukaryotes) was opposite to the projection by Agusti et al. (2019). In fact, the temperature usually changes concurrently with nutrient availability. The higher temperature, the less nutrients are available. Boyd et al. (2010) summarized that nutrient supply is likely to be the most important factor controlling the abundance and distribution of Synechococcus. In this study, the SST here in the regression possibly reflected the index of nutrient supply rather than the temperature effect itself. In brief, inorganic nutrient supply and temperature (for Prochlorococcus) were the major factors controlling picophytoplankton distribution at the SEATS station in the South China Sea. Since the nutrient supply is likely the controlling factor in the distribution of picophytoplankton biomass, other sources of nutrients should be considered. Previous studies showed that large-scale eddies and internal waves could bring extra nutrients to the surface and enhance phytoplankton growth in the SCS (Li et al., 2018; Shih et al., 2020). The SST and the MLD were both demonstrated to appropriately predict the distribution of picophytoplankton. This is the first time showing a good relationship between SST and the depth-integrated picophytoplankton biomass in the South China Sea (coefficient of determination, R² = 0.83). The models projected that Prochlorococcus became dominant when the SST reaches 28.8°C or more, while picoeukaryotes dominated in the rest of the temperature regimes (Figure 4). It is widely known that picophytoplankton contributes a significant fraction of primary production and carbon exports in the open ocean (Richardson and Jackson, 2007). In the future warmer SCS, Prochlorococcus could become more and more important regulating the carbon cycles. With small diel variabilities and ease to obtain from the satellite, the SST was a powerful parameter to quickly predict picophytoplankton biomass, as well as the abundance, at the SEATS station in the South China Sea.