SeaFlow is an underway flow cytometer that provides continuous shipboard observations of the abundance and optical properties of small phytoplankton (<5 μm in equivalent spherical diameter, ESD). Here we present data sets consisting of SeaFlow-based cell abundance, forward light scatter, and pigment fluorescence of individual cells, as well as derived estimates of ESD and cellular carbon content of picophytoplankton, which includes the cyanobacteria Prochlorococcus, Synechococcus and small-sized Crocosphaera (<5 μm ESD), and picophytoplankton and nanophytoplankton (2–5 μm ESD). Data were collected in surface waters (≈5 m depth) from 27 oceanographic cruises carried out in the Northeast Pacific Ocean between 2010 and 2018. Thirteen cruises provide high spatial resolution (≈1 km) measurements across 32,500 km of the Northeast Pacific Ocean and 14 near-monthly cruises beginning in 2015 provide seasonal distributions at the long-term sampling site (Station ALOHA) of the Hawaii Ocean Time-Series. These data sets expand our knowledge of the current spatial and temporal distributions of picophytoplankton in the surface ocean.
|Measurement(s)||planktonic material • temperature of water • salinity • light irradiance • plankton size distribution|
|Technology Type(s)||flow cytometer • Temperature Sensor Device • salinometer • photometer|
|Factor Type(s)||time • location|
|Sample Characteristic - Organism||Cyanobacteria • Micromonas pusilla • Navicula transitans • Thalassiosira pseudonana • Thalassiosira weissflogii • Geminifera cryophila • Crocosphaera • Synechococcus sp. WH 8012 • Synechococcus sp. WH 6501 • Prochlorococcus eMED4 • Prochlorococcus eMIT9312 • Prochlorococcus AS9601 • Prochlorococcus 1314|
|Sample Characteristic - Environment||oceanic sea surface microlayer biome • sea water|
|Sample Characteristic - Location||North Pacific Ocean|
Machine-accessible metadata file describing the reported data: https://doi.org/10.6084/m9.figshare.10110755
Background & Summary
Marine phytoplankton are responsible for about half of the planet’s annual production of oxygen and organic carbon, and thus play a significant role in mediating global biogeochemical cycles1. Quantitative information on the temporal and spatial distributions of phytoplankton populations in the ocean is critical for understanding how these organisms interact with their environments. Individual phytoplankton species range in diameter from ≈0.6 μm to over a millimeter2, with a predominance of the smaller phytoplankton (less than a few micrometers in size) in open ocean environments. In oligotrophic subtropical gyres, phytoplankton communities are numerically dominated by the cyanobacteria of the genus Prochlorococcus (<1 μm in diameter), which are well-adapted to low nutrient conditions3. The nitrogen gas-fixing cyanobacteria Crocosphaera (2–5 μm in diameter) are also sporadically observed in nitrogen-limited subtropical gyres; a portion of the nitrogen fixed by these organisms is made available to other phytoplankton4. In colder, more productive subpolar gyres, the cyanobacteria Synechococcus (1–2 μm in diameter) and picophytoplankton and nanophytoplankton (2–5 μm in diameter) numerically dominate phytoplankton communities5,6.
The abundance and distribution of different groups of phytoplankton reflect a combination of prevailing environmental conditions and resulting food-web dynamics. Flow cytometry is well-suited to mapping the distribution of the small phytoplankton (<5 μm in diameter) because of their relatively high abundance and the innate fluorescence of their pigments; for example, all phytoplankton possess chlorophyll a and a subset additionally possess phycoerythrin (e.g., Synechococcus and Crocosphaera). Models based on compilations of flow cytometry measurements from 1987–2011 predict that the distributions of cyanobacteria, picophytoplankton and nanophytoplankton may change significantly in future oceans5,6 as the surface waters warm and nutrient supply is reduced3. However, because the dim cellular chlorophyll fluorescence of Prochlorococcus in oligotrophic surface waters is near the detection limit of most commercially-available flow cytometers7, information on the broad-scale distribution of Prochlorococcus in surface waters remains limited.
SeaFlow is a custom-built shipboard flow cytometer developed for high-resolution observations of picophytoplankton in surface waters, including Prochlorococcus8. SeaFlow eliminates the traditional need for a sheath fluid by employing a unique optical system that relies on three photodetectors, including two position-sensitive detectors, to create a virtual core in the sample stream within which the properties of particles are accurately measured. This enables the instrument to continuously sample surface seawater from a ship’s flow-through seawater system.
Here, we present SeaFlow datasets consisting of over 69,000 data files collected in surface waters in the Northeast Pacific Ocean (Fig. 1 and Table 1). From 2010–2018, SeaFlow was deployed on 27 cruises conducted across 32,500 km. Data files are aggregated over three-minute intervals to yield a spatial resolution of ≈1 km along the cruise track (for a ship cruising at 11 knots). Beginning in 2015, SeaFlow was deployed on near-monthly cruises in the North Pacific Subtropical Gyre, at or near the long-term Hawaii Ocean Time-series (Station ALOHA, 22.75 degN, 158 degW). Primary data are cell abundances of phytoplankton populations, optical measurements of light scatter, red and orange fluorescence associated with the pigments chlorophyll a and phycoerythrin, respectively. The classification of particles into cell populations was conducted uniformly across all samples using a combination of manual gating and unsupervised clustering algorithms9. The data sets were expanded to include equivalent spherical diameter (ESD) and carbon quotas derived from light scatter measurements. ESD was estimated by applying Mie light scattering theory to a combination of flow cytometry calibration beads and cultured organisms of determined size. Carbon quotas were then estimated from ESD using a volume-to-carbon conversion factor10. The estimates of cell abundance, light scatter, fluorescence emissions, ESD and carbon quotas include a measurement error based on the uncertainties in the virtual core volume and light scatter conversion. Sample metadata includes location, time, underway sea surface temperature, salinity and photosynthetically active radiation (PAR) and were merged with the SeaFlow data sets. These data are available without restrictions at the Zenodo open access research data repository.
Each ship’s flow-through seawater system provided continuous flow of seawater collected at an assumed depth of ≈5 m (3–8 m depending on the research vessel and sea state). The water passed through a 100-μm stainless steel-mesh filter before it was sampled to prevent clogging of the 200-μm SeaFlow sampling nozzle.
A real-time broadcast of position, time, temperature, salinity and light irradiance available over the ship’s network was recorded as-is by the SeaFlow computer. Any missing ship data were retrieved from the Rolling Deck to Repository.
Four data processing steps are employed to transform raw SeaFlow data into processed data (Fig. 2). First, the filtration step identifies in-focus particles positioned within the SeaFlow virtual core8, a cross-sectional area within the sample stream determined by the field of view of the optical system. This field of view is a function of the magnification of the objective-tube lens system and the width of the field stop. Two position detectors (D1 and D2) determine the lateral position of a particle. Particles that scatter light equally on both detectors (aligned particles) and scatter more in the forward direction than on the two position detectors (in-focus particles) are considered optimally-positioned particles (OPP). The relationship between forward scatter and the two position detectors of OPP can be described by two linear regression models intersecting at the 1-μm calibration bead coordinates (Fig. 3). The uncertainties around the two slopes of the linear regression models are used to assign a confidence interval for each OPP (2.5%, 50% or 97.5% interval confidence). Each data file is linked to a unique filtration identification number that refers to the parameters used to discriminate OPP.
Second, OPP are classified into cell populations by forward scatter (457/50 bandpass filter), red fluorescence (572/28 bandpass filter) and orange fluorescence (692/40 band-pass filter). Sequential manual gating is used to cluster Synechococcus, small-sized Crocosphaera and 1-μm calibration beads (Invitrogen F8823), as they each have distinguishing optical characteristics that do not overlap with other cell populations. Prochlorococcus particles are clustered using a supervised clustering algorithm that emulates a sequential bivariate gating strategy based on cell density9. High forward scatter particles with high red fluorescence were classified as “picoeukaryote” phytoplankton. Each data file is linked to a unique gating identification number that refers to the coordinates and analysis parameters used for particle classification. Cell abundance is calculated by dividing the number of particles in each population by the volume of the virtual core, which is estimated by the ratio of OPP to the total detected particles and by the volume of the sample analyzed by the instrument8. The sample volume is obtained after calibration of the water stream flow rate. Standard error of cell abundance represents the uncertainties in flow rate calibration.
Third, the equivalent spherical diameter (ESD) of individual cells is estimated from SeaFlow-based light scatter by the application of Mie light scatter theory to a simplified optical model. Since the optical geometry of the SeaFlow is complicated by scatter occurring within the sample stream, an optimization procedure was used to minimize differences between the measured forward scatter and the scatter intensity predicted by Mie light scatter of homogeneous spherical particles. The ESD of each phytoplankton cell was estimated from the optimized Mie model based on three refractive indices (1.35, 1.38 and 1.41) that cover the range applicable to marine phytoplankton11, relative to refractive index of seawater (1.34).
In the final step, carbon quotas were estimated from ESD using the equation fgC cell−1 = 0.261 × Volume0.860 10, assuming spherical particles.
Quality control procedure
The stability of stream pressure and the rate of particles detected per second are used to evaluate instrument performance. Data files are identified as outliers if the stream pressure deviates by more than 5% of the mean value for a given cruise or if data acquisition exceeds 18,000 particles per second (corresponding to 200–500 particles per second in the virtual core), when coincidence of particles is likely8. The quality of estimates for ESD, carbon quotas and cell abundance was assessed by applying the Chauvenet criterion12, which defines outliers as data points falling outside a band around the mean corresponding to a probability of 1 − 1/(2N) (where N = total number of data points).
The dataset is a compilation of data assembled from different research cruises conducted since 2010. Each data record represents the cell abundance, median, 25% and 75% percentile of optical properties (chlorophyll and phycoerythrin fluorescence, forward scatter), ESD and carbon quotas for each population estimated at a certain point in space and time. Each data record belongs to a cruise, with cruise identification retrieved from the Rolling Deck to Repository, and is linked to its associated metadata such as time, location, depth, sea surface temperature and salinity, and PAR. Online-only Table 1 lists the variables, their definition and units. The dataset is accessible as a.csv file through Zenodo open access research data repository13.
Equivalent spherical diameter and carbon quotas
The optimized Mie theory was applied to SeaFlow-based scattering measurements of calibration beads of known refractive index (1.60) and diameter (0.3, 0.5, 0.75, 1, 1.83, 3.1 and 5.7 μm). Mie-predicted bead diameters were in good agreement with diameters provided by the manufacturer (R2 = 0.98, p < 0.0001) (Fig. 4a).
To evaluate the applicability of Mie-predicted cell diameters to phytoplankton cells, a Coulter Counter Multisizer equipped with a 15-μm and 30-μm orifice was used to measure cell diameters of axenic, exponentially growing cyanobacteria (Prochlorococcus MIT9312 and MED4, Synechococcus WH8012, WH6501 and sp.) and eukaryotic phytoplankton (the diatoms Navicula transitans, Thalassiosira pseudonana, Thalassiosira weissflogii and the crytophyte Geminifera cryophila) under non-limiting light conditions (150 μmol quanta m−2 s−1). These independent measurements were then compared to the equivalent spherical diameter derived from the Mie-based lookup table. The Mie-predicted ESD using the mid-range refractive index for phytoplankton (1.38) was in good agreement with observations (R2 = 0.96, p < 0.0001), however discrepancies were observed for the diameter of the larger phytoplankter T. weissflogii), suggesting a higher refractive index for this organism.
A second set of experiments was conducted to compare measurements of carbon quotas with those estimated from Mie-predicted ESD. Carbon per cell was determined for 6 axenic cyanobacteria cultures (Prochlorococcus MED4, MIT9312, AS9601 and NATL12A, Synechococcus WH7803 and WH8012) and 4 different eukaryotic phytoplankton cultures (Micromonas pusilla, Navicula transitans, T. pseudonana 3367 and 1135). Particulate C and N collected on pre-combusted 0.3-μm GF-75 or 0.7-μm GF/F filters were analyzed on a Carlo Erba CHNS analyzer (model NA1500) in the Oregon State University Stable Isotope Laboratory using cystine (29.99% C and 11.66% N by weight) as the primary standard. For each culture, aliquots of growth media filtered through three pre-combusted GF-75 and GF/F glass fiber filters were used as blanks to correct for background carbon concentration on filters before filtration and DOC adsorption onto filters. Carbon quotas were obtained by normalizing the concentrations of blank-corrected particulate carbon to cell abundance measured with a BD Influx cell sorter. Mie-predicted ESD based on light scatter measurements from SeaFlow was converted to carbon quotas using the equation fgC cell−1 = 0.261 × Volume0.860 11, assuming spherical particles. We found that carbon quotas were in good agreement with our light scatter-based estimates using a refractive index for phytoplankton of 1.38 (Fig. 4c) (R2 = 0.96, p < 0.0001), consistent with our ESD results (Fig. 4b).
The abundance of cells within a given phytoplankton population is dependent on the ratio of OPP to the total detected particles8. While a single linear regression was previously used to discriminate OPP8, here we applied the combination of two linear regression models, which better defined the relationship between forward light scatter and the position-sensitive detectors (Fig. 3) for particles less than or greater than 1 μm in ESD. We compared the resulting SeaFlow-based cell abundances of Prochlorococcus, Synechococcus and eukaryotic phytoplankton (<5 μm in ESD) with fixed samples collected concurrently on 17 cruises (n = 201) and measured on a BD Influx Cytometer. Particle counts for the three phytoplankton groups were in good agreement between the two instruments (R = 0.92, n = 603, slope of the regression line = 0.91) (Fig. 5), with 74% of the estimates (444/603) showing less than a 2-fold difference. 3% (17/603) of the estimates showed 1–2 order of magnitude difference, likely reflecting natural variability rather than instrument counting error.
Raw SeaFlow data are analyzed using our custom R package available on Github at https://github.com/armbrustlab/popcycle. The repository also includes a tutorial on the use of the software. Additional Github repositories are available for the virtual-core calibration, conversion of light scattering to cell size and conversion of light scattering to carbon quotas.
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We thank the officers, crew and chief scientists aboard the research vessels Kaimikai O. Kanaloa, Kilo Moana, T.G. Thompson and Western Flyer for their assistance during the cruises. We thank Tara Clemente, Edward F. Delong, David M. Karl and the SCOPE operation team for supporting SeaFlow deployment and data collection on HOT cruises, funded partially by the Simons Foundation (#329108 to E.F.D. and D.M.K.). We thank Erin Horn, John MacMillan and Rhonda Morales for processing flow cytometry samples, Megan Schatz and Camilo Perez for processing electronic particle counter samples and Katie Watkins-Brandt for processing particulate organic carbon samples. We also thank Alexandra Worden for her support of C.P. and SeaFlow deployment on cruises in the eastern California Current funded by MBARI and the Gordon and Betty Moore Foundation grant (#3788 to A.W.). S.C. was funded by a Moore/Sloan Data Science and Washington Research Foundation Innovation in Data Science postdoctoral fellowship. This work was supported by grants from the Simons Foundation (#574495 to F.R., #329108 to E.V.A. and A.E.W. and #426570SP and #549894 to E.V.A.), the Gordon and Betty Moore Foundation (#3776 to E.V.A.) and the National Aeronautics and Space Administration (#80NSSC17K0561 to F.R.).
The authors declare no competing interests.
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Ribalet, F., Berthiaume, C., Hynes, A. et al. SeaFlow data v1, high-resolution abundance, size and biomass of small phytoplankton in the North Pacific. Sci Data 6, 277 (2019). https://doi.org/10.1038/s41597-019-0292-2
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