This research explores the Amazon Plume region of the Western Tropical North Atlantic. Samples were collected during three oceanographic cruises: KN197 (May-June 2010, R/V Knorr) during the peak discharge period, AT2104 (July 2012, R/V Atlantis), during the falling discharge period, and MV1110 (September-October 2011, R/V Melville), during the low discharge period. Each cruise sampled a different set of planktonic habitats defined by Weber et al. (2019) and Pham et al. (2024): RI (Riverine Input), YPC (Young Plume Core), OPC (Old Plume Core), WPM (Western Plume Margin), EPM (Eastern Plume Margin), and OSW (Offshore Waters, Table 1 ) ( Figure 1 ).

We obtained hydrographic data using the shipboard underway flow-through system and a CTD-rosette equipped with a fluorometer, transmissometer, and PAR sensor. In brief, we collected unfiltered seawater samples directly from the ship’s underway system or CTD-rosette for measurement of the concentrations of dissolved nutrients (NO₃ ^-+NO₂ ^-, PO₄ ^-3, and SiO₂) using a Lachat QuickChem 8000 FIA system. We collected suspended particles for isotopic and elemental analysis by passing 2-18 L of seawater through pre-combusted (450˚C for four hours) 47mm GF/F filters under gentle pressure (5-10 psi) without acidification. Sample filters were dried at sea (60˚C) and stored over desiccant for analysis ashore (Weber et al., 2017).

We measured the elemental composition and natural abundance of ¹³C in suspended particles by continuous-flow isotope-ratio mass spectrometry (CF-IRMS) using a Micromass Optima or an Isoprime 100 interfaced to a Carlo Erba NA2500 elemental analyzer for online combustion and purification of sample carbon and nitrogen. We report all stable isotope abundances as δ¹³C values relative to VPDB. A size series of standards for elemental (methionine) and isotopic (peptone) composition were used to check instrument stability and correct analytical blanks (Montoya, 2008). We estimate that the overall analytical precision of our isotopic measurements is better than ±0.2‰.

We calculated the depth-weighted mean of the concentration of particulate carbon, [PC], and the depth-weighted mean δ¹³C of suspended particulate matter in the upper water column by trapezoidal integration (Landrum et al., 2011):

Where [PC] _i is the particulate carbon PC concentration (μM), and δ¹³C is the isotopic composition of PC in-depth interval Δz _i (m).

Similarly, we calculated the depth-weighted mean water column (MWC) concentrations of nitrate, phosphate, and silicate as:

In all cases, we integrated our data over the upper 100 m of the water column. We integrated through the entire sampling depth where the bottom depth was ≤ 100 m.

We tested for significant differences in surface and mean water column (MWC) values of PC concentration, elemental C:N ratio, and the δ¹³C among the habitat types defined by Weber et al. (2019) and Pham et al. (2024) by performing one-way ANOVAs. When tests were significant (p < 0.05); we additionally ran post hoc Tukey–Kramer tests to explore significant differences among habitats (α = 0.05). Additionally, we calculated principal component analysis (PCA) and Pearson correlation coefficients to investigate the relationships between hydrographic conditions and particulate matter characteristics. Our statistics and graphical data representations were performed using JMP Pro 17 software (SAS Institute Inc., Cary, USA) and R using RStudio (Team, 2022).

Cruise KN197 sampled five habitats ( Figure 1A ; Table 1 ) in the WTNA during the peak discharge period of spring 2010 (Pham et al., 2024; Weber et al., 2019). The plume core habitats (YPC and OPC) had the most stratified water column due to their higher surface temperature (mean SST=29.7°C) and lower surface salinity (mean SSS= 16.6 psu) relative to the surrounding oceanic waters. As the plume moved northward, it mixed with offshore water and became less coherent spatially. The eastern and western margins of the plume (EPM and WPM habitats) had lower surface temperatures (< 28.5°C) and higher surface salinities (>30 psu) and were less stratified compared to the plume core habitats. The average mixed layer depth (MLD) increased from less than 10 m in the YPC to more than 60 m in the OSW habitat. The depth of the deep chlorophyll-a maximum (ChlDM) deepened from a few meters in plume core habitats to about 120 m in the EPM habitat ( Figures 2A-C ).

The spatial distributions of nutrient concentrations in the surface water (depth <5m) were like those in the upper water column (down to 100 m). Specifically, we found higher nutrient values in the plume core habitats and gradually decreasing concentrations moving northward ( Figures 3A-C ). The surface [NO₃ ^-] was undetectable at most stations, with notable exceptions at Stations 4.04 and 9.43, which belonged to the OPC and WPM habitats. In contrast, the surface concentrations of [PO₄ ^-3] and [SiO₂] were notably higher in the YPC and OPC habitats but decreased sharply in the WPM, EPM, and OSW habitats. Below the surface, the MWC [NO₃ ^-] ranged from 1.9 ± 1.6 µM in the YPC habitat to 0.4 ± 0.3µM in the OSW habitat, while the MWC [PO₄ ^-3] ranged from 0.2 ± 0.1 µM in the YPC habitat to 0.05 ± 0.06µM in the OSW habitat. The MWC [SiO₂] ranged from 5.4 ± 4.6 µM in the YPC habitat to 1.2 ± 0.3µM in the OSW habitat.

Cruise AT2104 sampled four habitats during the late summer of 2012 (Pham et al., 2024), a period of weaker river discharge ( Figure 1B ; Table 1 ). The RI habitat was located nearest the river mouth and had the greatest freshwater influence, with surface salinity ranging between 0 psu to less than 8 psu. In contrast, we found surface salinities of 20-25 psu in the plume core habitats (YPC and OPC) and 30-35 psu in the WPM habitat. The surface waters in the plume core habitats were slightly warmer (SST~29.5°C) than in the RI and WPM habitats (SST~ 28.5°C). The MLD was shallow (~ 10m) at almost all our stations, with a few deeper values toward the northwest of the plume area (> 25m) in the WPM habitat. The ChlDM occurred near the surface (<10m) at all RI, YPC, and OPC habitat stations. The ChlDM deepened towards the north and reached depths of 50 m at some WPM stations ( Figures 2D-F ).

Nutrient distributions during Cruise AT2104 varied laterally among different habitat types and vertically through the water column ( Figures 3D-F ). Nutrient concentrations in the surface waters were notably elevated in the RI habitat compared to other sampled habitats (YPC, OPC, and WPM). Surface [NO₃ ^-] levels were generally high and detectable at most stations, with the RI habitat reaching a maximum of 11.1 µM. Surface [PO₄ ^-³] and [SiO_2] concentrations showed a similar trend, with higher values near the river mouth and gradually decreasing down the Plume. Due to the shallow depth of the RI habitat (< 10m), surface and mean water column (MWC) nutrient measurements were very similar. Further from the river mouth, MWC [NO₃ ^-] and [PO₄ ^-³] values were higher than those at the surface and decreased from the YPC to WPM habitats. MWC [SiO_2] was slightly lower than surface levels in all habitats, except for a notable decrease in the OPC habitat relative to the other habitats.

Cruise MV1110 sampled four habitats in the fall of 2011 (Pham et al., 2024) when the ARP was weaker and entrained by the NECC and retroflected to the northeast ( Figure 1C ; Table 1 ). The surface temperature was highest in the OPC habitat (~29.5°C) and lowest in the OSW habitat (~ 28.0°C). The stations in the EPM habitat showed the greatest variation in SST, ranging from 28.3°C to 30.5°C. Surface salinities ranged from 23 psu in the OPC habitat to slightly above 36 psu in the OSW habitat. The MLD was shallow at most stations of the OPC, WPM, and EPM habitats (< ca. 30m) and deeper in the OSW habitat (> 115m). The ChlDM showed more variation among habitat types, with a shallower ChlDM (< 40m) in the OPC and WPM habitats than in the EPM and OSW habitats (> 50m; Figures 2G-I ).

The spatial distributions of nutrients at the surface varied among habitats, with a consistent pattern of higher concentrations in the OPC habitat and lower concentrations in offshore waters ( Figures 3G-I ). Specifically, surface nitrate [NO₃ ^-] levels were generally below detection limits, except for six stations in the OPC habitat, where the average concentration was 0.13± 0.17µM. In contrast, surface phosphate [PO₄ ^-3] and silicate [SiO₂] concentrations were measurable at all sampling sites and showed elevated levels in the OPC and WPM habitats compared to the EPM and OSW habitats. In the water column, the MWC [NO₃ ^-] ranged from 1.18± 0.62 µM in the OPC habitat (N=6) to 3.63± 3.03 µM in the EPM habitat (N= 53), then dropped in the OSW (0.86± 0.71 µM, N=8). The MWC [PO₄ ^-3] and [SiO₂] were lower than surface values but showed a similar spatial distribution at the surface among habitats.

We observed lateral variability in the [PC], elemental (C:N) ratio, and δ¹³C across different habitats and vertical variation from the surface through the water column. During Cruise KN197, the YPC, OPC, and WPM habitats showed higher [PC] values near the surface (<5m) compared to the upper water column (~100m). In contrast, the EPM and OSW habitats had comparable [PC] levels at the surface and throughout the water column. The surface [PC] ranged from 64.6 µmol L^-1 in the YPC habitat to less than 2.3 µmol L^-1 in the OSW habitat, and MWC [PC] ranged from 13.0 µmol L^-¹ in the YPC habitat to 1.9 µmol L^-¹ in the OSW habitat ( Figure 4A ).

The surface C:N ratio was relatively high in the YPC and WPM habitats, averaging 10.2 ± 3.0 (N = 3) and 9.6 ± 1.9 (N = 6), respectively. In contrast, the OPC, EPM, and OSW habitats had lower surface C:N ratios, averaging C:N = 7.1 ± 2.7 (N = 3), 7.6 ± 1.2 (N = 5), and 8.3 ± 1.9 (N = 4), respectively ( Figure 5A ). Within the water column, the MWC C:N ratio varied less among habitats than the surface values. The highest average MWC C:N ratio of 9.0 ± 1.9 (N = 3) occurred in the YPC habitat, with a minimum value of 7.1 ± 1.4 (N = 3) in the OPC habitat. The average MWC C:N ratios in the WPM, OSW, and EPM habitats were 7.5 ± 0.6 (N = 6), 7.5 ± 1.5 (N = 4), and 7.3 ± 0.8 (N = 5), respectively ( Figure 5A ; Supplementary Figure S2 ).

Surface δ¹³C was generally higher in the YPC, OPC, and WPM habitats, averaging -19.7 ± 1.5‰ (N = 3), -18.2 ± 1.6‰ (N = 3), and -19.2 ± 2.6‰ (N = 6), respectively. In contrast, we found lower surface δ¹³C values in the EPM and OSW habitats, with means of -20.1 ± 1.2‰(N = 5) and -21.6 ± 0.5‰ (N = 4), respectively ( Figure 6A ). The MWC δ¹³C decreased from an average of -19.3 ± 1.5‰ in the YPC habitat to -22.1 ± 0.5‰ in the OSW habitat. Interestingly, the WPM habitat showed the greatest variability in δ¹³C both at the surface (-23.7‰ to -15.0‰) and in the water column (MWC δ ¹³C of -22.9‰ to -17.1‰; Figure 6A ).

During Cruise AT2104, the spatial distributions and vertical profiles of [PC], C:N ratio, and δ¹³C differed from those during Cruise KN197. Specifically, these parameters showed more heterogeneity among habitats and with depth ( Figures 4B , 5B , 6B ). The average surface [PC] varied across habitats, ranging from 64.6 ± 110.8 µmol L^-¹ (N=5) in the RI habitat to 5.3 ± 3.8 µmol L^-¹ (N=9) in the WPM habitat. In the YPC and OPC habitats, the average surface [PC] was 17.9 ± 12.3 µmol L^-¹ (N=3) and 7.8 ± 5.6 µmol L^-¹ (N=3), respectively. The MWC [PC] varied considerably across habitats. It was highest in the RI habitat, with an average of 182.1 ± 235 µmol L^-¹ (N=5), and then decreased to a minimum of 1.8 ± 0.9 µmol L^-¹ (N=3) in the OPC habitat. In the YPC and WPM habitats, the MWC [PC] was 12.0 ± 13.7 µmol L^-¹ (N=3) and 8.6 ± 12.3 µmol L^-¹ (N=9), respectively.

The surface C:N ratio was similar in the RI, YPC, and OPC habitats, with an average value of 8.5 ± 2.3 (N = 11). In the WPM habitat, the average surface C:N ratio decreased to 7.5 ± 0.5 (N = 9). Interestingly, the MWC C:N ratio exhibited more variation among habitats than the surface C:N ratios. Specifically, we found lower MWC C:N ratios in the OPC habitat (average 7.1 ± 0.5, N = 3) and higher ratios in the WPM habitat (average 8.2 ± 1.5, N = 9).

The surface and MWC δ¹³C values were notably lower in the RI habitat compared to the YPC, OPC, and WPM habitats. Specifically, the average surface δ¹³C was -26.0 ± 1.1‰ (N = 5) in the RI habitat and increased to -20.4 ± 0.9‰ (N = 3) in the OPC habitat. The average MWC δ¹³C values ranged from -26.4 ± 0.6‰ (N=5) in the RI habitat to -22.7 ± 0.9‰ (N=9) in the WPM habitat.

During Cruise MV1110, PC concentrations, C:N ratio, and δ¹³C values were higher at the surface than in the water column and tended to decrease offshore ( Figures 4C , 5C , 6C ). Surface [PC] decreased from an average value of 7.6 ± 2.1µmol L^-¹ (N=4) in the OPC and 8.3 ± 4.7µmol L^-¹ (N=7) in the WPM habitat to 2.8 ± 1.0 µmol L^-¹ (N= 37) and 2.5 ± 0.6 µmol L^-¹(N=6) in the EPM and OSW habitats, respectively. The average value of MWC [PC] decreased from 1.3 ± 0.6µmol L^-¹ (N=4) in the OPC and 2.9 ± 2.1µmol L^-¹ (N=7) in the WPM habitat, to 1.2 ± 0.6 µmol L^-¹ (N= 37) and 1.5 ± 0.6 µmol L^-¹(N=6) in the EPM and OSW habitats, respectively.

Surface C:N ratios varied more than MWC values among different habitats. For instance, the surface C:N ratio had an average value of 8.5 ± 1.0 (N=4) in the OPC habitat, then decreased to 6.3 ± 0.8 (N=6) in the OSW habitat. Similarly, the average MWC C:N ratio declined from 7.6 ± 1.7 in the WPM habitat to 6.4 ± 0.5 in the OSW habitat.

Surface δ¹³C values decreased from a maximum of -18.5‰ in the OPC habitat to a minimum of -22‰ in the OSW habitat, with averages of -19.6 ± 1.1‰ (N=4), -20.0 ± 1.4‰ (N=7), -20.6 ± 0.6‰ (N= 37), and -20.8 ± 0.9‰ (N=6) in the OPC, WPM, EPM, and OSW habitats, respectively. The MWC δ¹³C ranged from a maximum of -17.3‰ in the WPM to a minimum of -23.1‰ in the EPM habitat, with an average of -20.5 ± 0.1‰ (N=4), -19.8 ± 1.8‰ (N=7), -21.4 ± 0.7‰ (N= 37), and -20.9 ± 1.0‰ (N=6) in OPC, WPM, EPM, and OSW habitats, respectively.

We aggregated data from all three cruises to investigate variations in habitats sampled in multiple cruises/seasons ( Figures 7 – 9 ; Supplementary Figures S1 - S3 ; Table 2 ). The highlighted results are those with statistically significant differences (p < 0.05) in the ANOVA tests.

We sampled the YPC habitat during the spring and late summer and found surface δ¹³C values were notably higher during spring/Cruise KN197 than during summer/Cruise AT2104.

We sampled the OPC habitat during all three cruises and found no significant differences in the surface value of biogeochemical parameters across the seasons. However, MWC δ¹³C values were more positive during spring/Cruise KN197 and fall/MV1110 than during summer/Cruise AT2104.

The WPM habitat was sampled during all three cruises. The surface and MWC δ¹³C ( Supplementary Figure S3 ) were more positive during spring/Cruise KN197 and fall/MV1110 compared to less positive values during summer/Cruise AT2104.

The EPM habitat was sampled during the spring and fall seasons. We found surface and MWC PC and C:N ratios were higher during sping/Cruise KN197 than fall/Cruise MV1110.

Finally, we sampled the OSW habitat during the spring and fall cruises. We found that the surface C:N ratio was higher in the spring than in the fall. However, surface δ¹³C was more positive during fall/Cruise MV1110 than summer/Cruise AT2104.

Cruise KN197 sampled the ARP region during peak discharge in spring, a period when the plume delivers a substantial volume of buoyancy and terrigenous material into the ocean, profoundly affecting the hydrography and biogeochemical status over a large region of the Western Tropical Atlantic (DeMaster et al., 1996; Ryther et al., 1967; Smith and Demaster, 1996). Our hydrological measurements showed gradients in sea surface salinity, temperature, and turbidity ( Figure 2A ) extending from the plume core habitats to the offshore waters (Coles et al., 2013a; Liang et al., 2020). The physical structure of the water column transitioned from shallow stratification near the plume core to a deeper, well-mixed state offshore ( Figure 2B ). The impact of solar heating on the surface water causes strong thermal stratification of the upper water column, which increases offshore (Foltz and McPhaden, 2009).

During this cruise, the ARP region included a range of nutrient availability and potential limitations. Nitrate concentrations were below the detection limit at the surface of most stations ( Figure 3A ) due to the high demand and active biological uptake (Demaster and Pope, 1996; Edmond et al., 1981; Goes et al., 2014). In contrast, phosphate and silicate concentrations were uniformly measurable and decreased northward due to the mixing of plume water with oceanic water and biological uptake ( Figures 3A-C ). Weber et al. (2017) found that phosphate concentrations deviated positively from the conservative mixing line in the plume due to release from terrigenous materials. The high demand for nitrogen by coastal phytoplankton, composed primarily of diatoms, cryptophytes, and green-water Synechococcus spp., produced strong N-limitation at the surface (Goes et al., 2014). As the plume moved northward, the nitrogen supply from the riverine flow and coastal upwelling diminished while the phosphate and silicate concentrations were still high enough to support diazotrophy. The atmospheric dinitrogen fixers, mainly diazotrophic-diatom associations (DDAs), bloomed in the mesohaline area of the plume and Trichodesmium, found on the plume margins and oceanic water (Goes et al., 2014; Weber et al., 2017), supported new production and facilitated carbon export to the deep ocean (Demaster and Pope, 1996; Loick‐Wilde et al., 2016). Nutrient dynamics are crucial for phytoplankton niche partitioning in this region and, therefore, carbon budgets (Agawin et al., 2000).

In-situ chlorophyll fluorescence is a valuable proxy for phytoplankton biomass. During this cruise, elevated surface [Chl a]coincided with higher biomass ([PC]) and nutrient concentrations ([PO₄ ^3-]) in the YPC and OPC habitats. The [Chl a] decreased as the plume influence waned northward in the EPM and OSW habitats. The maximum [Chl a]value in our data set, 18.1 mg m^-3 in the YPC habitat, coincided with a high abundance of diatoms, dinoflagellates, and Cryptophytes (Goes et al., 2014; O'Reilly and Busch, 1984). Higher [Chla] at the surface in the YPC habitat is associated with a larger phytoplankton cell (Pham et al., 2024), as well as an elevated PC concentration (64.4 µM) and high δ¹³C (-17.7‰), and also supported by the finding of high rates of carbon fixation in the area (Alriyami et al., 2024 ¹ ; Montoya et al., 2019).

The ChlDM reflected the interaction between the availability of nutrients from subsurface nutrient-rich deep water and light from the above sunlight-abundant surface as mediated by phytoplankton physiology (Latasa et al., 2017; Letelier et al., 2004). The ChlDM frequently occurs at the nitracline, reflecting strong nutrient limitation in the well-illuminated waters above (Cullen, 2015). The ChlDM was near the surface in the YPC and OPC habitats and at some WPM stations ( Figure 2C ), where the nitracline was also shallow due to riverine nutrient input and coastal upwelling in the area (Demaster and Pope, 1996; Weber et al., 2019). Further offshore, the EPM and OSW habitats had deeper ChlDM values, reflecting the location of the nitracline ( Figure 10 ) in the thermally stratified water column (Chen and Chen, 2006; Marañón et al., 2000). The plume-proper habitats supported higher phytoplankton growth at the surface, while in the EPM and OSW habitats, growth was limited by nitrate availability on the surface, leading to deeper ChlDM values. The absolute [Chla]in the ChlDM varied from 6.8 mg m^-3 in the YPC habitat to 0.25 mg m^-3 in the EPM habitat. Due to variation in the intensity and duration of oceanic waters mixing with the plume margins, the WPM and EPM habitats showed high variation in ChlDM on a time scale of hours, compared to the vertically more stable water column in the YPC, OPC, and OSW habitats, reflecting the very dynamic nature of the plume along the continuum (Weber et al., 2017, 2019).

The [PC] was highest at the surface of the habitats nearest the river mouth and declined with depth. This pattern slightly changed in the offshore waters, where surface [PC] was low, and a subsurface [PC] maximum occurred at the depth above ChlDM. Specifically, the YPC, OPC, and some stations of the WPM habitat had the highest [PC] values at the surface, reflecting the contribution of the riverine input to particle loads (Smith and Demaster, 1996), enhanced production rates, and the high abundance of phytoplankton (Conroy et al., 2016; Goes et al., 2014). The strong correlations between [PC] and our measurements of turbidity, nutrients, and Chla concentration (R² = 0.82, 0.85, and 0.96, respectively, Station10.04, YPC habitat; Figure 10 ) further illustrated the combined influence of physical, chemical, and biological factors on PC dynamics over this area. In contrast, the EPM and OSW habitats had low particulate matter concentrations at the surface and throughout the water column ( Figure 10 ). The deep MLD restricted the vertical transport of nutrients to the surface, limiting surface production, thus generating a more uniform [PC] distribution throughout the water column ( Figure 4A ).

The high surface C:N ratio (>12) at some YPC and WPM stations suggested a high input from terrigenous organic matter or elevated production under a nitrogen limitation (Galbraith and Martiny, 2015; Kendall et al., 2001). However, most of our surface C:N ratios fell in the range of 9-6, which is typical of marine plankton (Moore et al., 2013; Redfield, 1958). The surface C:N ratio was lower than the Redfield Ratio (C:N= 6.6) at a few stations in the OPC (C:N= 4.5) and WPM (C:N= 6.0) habitats ( Figure 5A ), which may reflect production under nitrogen replete conditions due to diazotrophic N-fixation (Finlay and Kendall, 2007; Montoya, 2007) or localize eddies (Cherubin and Richardson, 2007). The MWC C:N ratio (10-6) was slightly lower than the surface C:N ratio (14-6). This observation suggests a stronger influence of terrigenous sources at the surface and a predominance of organic matter derived from phytoplankton at greater depths while indicating. Edmond et al. (1981) argued that the C:N ratio cannot resolve the contribution of different sources on the organic matter pool in the Amazon shelf, as the soil microbe (C:N= 16) is not significantly different than phytoplankton. Furthermore, the strong linear correlation between [PC] and [Chl a] in the water column (R² = 0.93), along with the relationship of our surface and MWC C:N ratios within the PC: Chla ratio of < 200 ( Supplementary Figure S4 ), underscores the significant contribution of living phytoplankton in the organic matter we sampled than terrestrial or detrital material (Foster et al., 2011; Hedges et al., 1986; Hofmann et al., 2000; Pan et al., 2014).

The δ¹³C of surface suspended particles decreased northward from the OPC habitat to the OSW habitat. Additionally, δ¹³C values decreased with increasing depth throughout the water column ( Figure 6A ; Supplementary Figure S3 ). The high surface δ¹³C in the OPC habitat coincided with high biomass (PC and Chla), likely produced by rapidly growing large phytoplankton cells including diatoms (Goes et al., 2014). The diffusion-limitation of dissolved inorganic carbon into algal cells may also result in high δ¹³C values of the organic matter produced (Burkhardt et al., 1999). The WPM habitat had the most significant variability in δ¹³C of suspended particles both at the surface (-23.7‰ to -15.0‰) and in the water column (MWC range: -22.9 ‰ to -17 ‰). This mesohaline habitat supported a diverse phytoplankton community, including DDAs, flagellates, and Trichodesmium, that vary in growth rate, cell size, and inorganic carbon source, and therefore, δ¹³C values (Goes et al., 2014; Laws et al., 1995; Smith, 1972).

On the other hand, the EPM and OSW habitats had the lowest surface and MWC δ¹³C values, which coincided with lower biomass (PC and Chla) and low production rates dominated by small cells (Alriyami et al., 2024 ¹ ; Goes et al., 2014; Montoya et al., 2019). Additionally, The high concentration of DIC in oceanic water allows phytoplankton cells to discriminate enzymatically against ¹³C through carboxylase activity, producing OM depleted in ¹³C compared to the organic matter produced in the plume water (Popp et al., 1998). The difference between surface and MWC δ¹³C likely reflects the impact of photosynthesis at the surface versus respiration at depth. Other factors, like the use of bicarbonate rather than dissolved carbon dioxide and shifts of community structure to smaller cells in response to changes in light and nutrients, generally lead to lower ¹³C abundance in organic matter (Laws et al., 1995).

During Cruise AT2104 ( Figure 11 ), conducted during late summer, the plume core habitats (YPC and OPC) had slightly warmer surface waters compared to the RI and WPM habitats, a reflection of both the weaker influence of riverine outflow and the regular seasonal drop in temperature (Muller–Karger et al., 1988). The RI habitat, closest to the river mouth, showed the most freshwater influence with an extremely low surface salinity (min SSS=0 psu). The MLD was shallow at the plume proper habitats, with deeper values observed northwest of the cruise track. The ChlDM varied among habitats and was slightly shallower than in spring, occurring near the surface in RI, YPC, and OPC habitats and deepening towards the north in the WPM habitat (Pham et al., 2024).

Nutrient concentrations were measurable in surface waters at most of our sampling stations except for deficient nitrate concentrations in the OPC habitat (Mean 0.13 ± 0.14 µM, N=3). Nutrient concentrations were generally higher below the plume than at the surface, highlighting the potential impact of mixing and upwelling in bringing nutrient-rich waters to the surface below the pycnocline (Lentz and Limeburner, 1995). Moreover, the high nutrient availability, especially at the surface of southernmost stations belonging to the RI habitat, may be amplified by riverine supply (Edmond et al., 1981), the remineralized particles from the spring bloom (DeMaster et al., 1991), nitrate production through nitrification (Choisnard et al., 2024), and seasonal changes in the nutrient recycling rate (Vital et al., 1999). These organic materials decompose and release nutrients back into the water column, providing an additional source of nutrients to support the primary producer’s growth (Harrison, 1980; Sarmiento et al., 1990). The low but measurable nitrate concentrations in the OPC habitat may stem from localized differences in nutrient utilization due to biological processes unique to the OPC habitat, such as higher growth and production rates or more grazing and heterotrophy.

The strong positive correlation between [PC] and [Chla] in the water column (R² = 0.64, Figure 12 ) and the relationship between the C:N ratio and PC: Chla ratio ( Supplementary Figure S4 ) suggested an elevated contribution of phytoplankton production in the particulate carbon pool in all but the RI habitat. We found very high surface and MWC [PC] in the RI habitat, reflecting its proximity to the river mouth and the extension of the plume to the bottom depth (Smith and Russell, 1995). Notably, the highest PC concentration in our dataset (~ 500 µmol L^-¹) was recorded in the subsurface waters of the RI habitat. A subsurface maximum [PC] is common in riverine estuaries, typically resulting from tidal mixing, redistribution of material within the water column, or resuspension of benthic sediments (DeMaster et al., 1986; Lohrenz et al., 1992).

The OPC habitat displayed elevated [PC] at the surface, which declined with depth. Nutrient data suggest active biological drawdown in the OPC zone; however, the accumulation and sinking of biomass to the deeper ocean may be inhibited by heterotrophic consumption at the surface. Through grazing and decomposition, heterotrophs break down organic matter into smaller, more degradable forms or respire it as CO₂, reducing the availability of larger particles that typically contribute to vertical flux (Lefèvre et al., 2017). While heterotrophs can repackage organic matter into fecal pellets, which usually enhance vertical flux, in this case, the intense surface heterotrophic activity appears to favor rapid recycling within the euphotic zone, thereby limiting the export of organic carbon to deeper waters (Calef and Grice, 1967). The surface and MWC [PC] variations among habitats during the summer cruise may be related to turbidity (in the RI habitat), productivity (in the YPC and OPC habitats), and density gradients (in the WPM habitat). For instance, turbidity is increased by the organic material load from river basin, increasing [PC] closer to the river mouth. High marine productivity contributes directly to [PC] via phytoplankton growth in habitats where the water column has sufficient light and nutrients. Where density gradients limit nutrient supply by vertical mixing, the [PC] is low throughout the water column as in the WPM habitat.

The average surface and MWC C:N ratios were similar in all four habitat types sampled during this cruise and showed lower values than those during the spring period ( Figure 5 ; Supplementary Figure S2 ). Given the relatively smaller scope of the sampling area during this cruise and the weakening river flow, these observations revealed the plume’s reduced influence on terrigenous material or marine production under replete nutrient conditions (Kendall et al., 2001).

The considerably depleted δ¹³C values in the RI habitat compared to values in the YPC, OPC, and WPM habitats suggested a major contribution of organic matter from terrestrial plants (Farquhar et al., 1982; Parker, 1964; Smith, 1972). We found highly enriched surface δ¹³C in the OPC and WPM habitats, which coincided with reduced nitrate concentration in the area ( Figure 3D ), high surface [PC], and average C:N ratios above the Redfield ratio, all could reveal high in situ production ( Figures 4 , 5 ; Supplementary Figure S3 ). Showers and Angle (1986) found that δ¹³C values in surface waters of 0 psu salinity of Amazon river mouth were isotopically depleted (-27.3‰), whereas δ¹³C values in outer shelf waters (35 psu), ranged from -19.5 ‰ at the surface to -25.3 ‰ near the seabed.

During the fall season (Cruise MV1110), the riverine outflow from the Amazon weakened, and the plume extended further northeast under the influence of the NECC (Muller–Karger et al., 1988) ( Figure 11 ). While surface temperatures decreased at most OPC, WPM, and OSW stations, the EPM habitat remained relatively warm. Although the gradient of surface salinity from the plume core to the surrounding oceanic water was less pronounced compared to our spring and late summer cruises, most stations sampled fell within the mesohaline range of surface salinity 30-35 psu (Subramaniam et al., 2008). The OSW habitat exhibited a much deeper MLD (>115 meters) than during the spring period, reflecting the intrusion of oceanic waters into the plume through intense vertical mixing during the fall season (Geyer and Kineke, 1995; McGowan and Hayward, 1978). However, we found considerable variation in the depth of the chlorophyll maximum (ChlDM) among habitats, with a pronounced deepening towards the northeast (Pham et al., 2024).

The spatial distribution of major nutrients (NO₃ ^-, PO₄ ^-3, and SiO₂) during fall was generally similar to what we observed during spring. The undetectable nitrate concentrations at the surface of most stations may reflect the influence of fall blooms (Longhurst, 1993).

The seasonal shift in riverine discharge influences the extent of autochthonous vs allochthonous productivity (Cai et al., 1988; Hedges et al., 1986). The surface [PC] exhibited high values in OPC and WPM habitats and decreased in the EPM and OSW habitats. Similarly, the MWC [PC] followed a similar trend, albeit with lower concentrations than the surface. According to our hydrographic and nutrient data, the outflow significantly boosts productivity and biomass at the surface of the OPC and WPM habitats, more so than in the EPM and OSW habitats. The river’s influence diminishes and weakens as it moves northeast, impacting the production of organic matter ( Figure 4C ).

The C:N ratio remained within a narrow range (9-6) across all our sampling sites and was notably lower than the spring and late summer ratios ( Figure 6C ).The observed range of C:N ratios provides evidence of the awakening influence of outflow in transporting terrestrial material in the fall compared to spring (Kendall et al., 2001). The relationship between the C:N ratio and the PC: Chla ratio ( Supplementary Figure S4 ) further supported that most organic matter came from living sources, mainly marine phytoplankton, rather than detrital or non-living sources (Cifuentes et al., 1988).

Surface δ¹³C peaked in the OPC and WPM habitats, where sufficient growth conditions led to a high carbon fixation rate, and δ¹³C decreased further offshore in the EPM and OSW habitats (Cifuentes et al., 1988; Popp et al., 1998). When examining the relationship between δ¹³C and C:N ratios, we observed that most of our particles originated from marine in-situ production, with minimal contributions from terrigenous sources compared to the spring and summer data ( Figure 13 ). The PC: Chla ratio was <60, and δ¹³C ranged between -18‰ to -24‰, typical of a phytoplanktonic signature, indicating the predominance of living material in the suspended particles stock (Kendall et al., 2001).

From the river mouth to the offshore area, surface C:N ratios decreased but remained above the Redfield ratio, reflecting the reduced influence of terrestrial materials or phytoplankton production under nutrient limitation (Goes et al., 2014; Montoya et al., 2019; Ryther et al., 1967; Weber et al., 2017). The RI habitat exhibited high surface C:N ratios, likely because of terrestrial C₃ plant’s input or higher remineralization rates and bacterial breakdown of riverine organic matter. This agreed with the hypothesis of preferential nitrogen uptake by microorganisms during organic matter remineralization (Geider and La Roche, 2002; Harrison, 1980; Martiny et al., 2014). The lateral variations in the surface C:N ratio among other habitats (from YPC habitat to OSW habitat) are largely driven by several physical and biochemical processes besides the degree of plume influence. The dominance of specific phytoplankton groups, like diatoms, dinoflagellates, and DDAs in the plume water, leads to higher C:N ratios. These larger cells have more carbon-rich structures, such as silica frustules or carbon storage compounds, which increase their carbon content relative to nitrogen. In contrast, oceanic waters are dominated by smaller cells, which have lower C:N ratios due to their higher nutrient efficiency and lower carbon content (Carpenter et al., 2004; Pham et al., 2024). However, changes in the surrounding environment may suppress the role of phytoplankton physiology. For instance, small cells (cyanobacteria and small eukaryotes) usually exhibited a higher C:N ratio than the canonical Redfield ratio in oligotrophic areas and a lower C:N ratio in nutrient-replete conditions (Moore et al., 2013). Additionally, photoautotrophs in the most productive regions (YPC, OPC, and WPM habitats) are susceptible to nitrogen limitation on the surface due to the high demand, leading to high C:N ratios (Martiny et al., 2014).

In this study, the surface C:N ratios showed higher values and a wider range during spring compared to late summer and fall ( Figure 5 , Supplementary Figure S2 ). The peak outflow facilitated higher biological activity via transporting more nutrients and supporting the organic matter pool with a considerable amount of terrestrial material (Liu et al., 2019). Meanwhile, the surface C:N ratios declined in the late summer and fall cruises and showed fewer habitat variations. This is due to the reduced terrigenous material delivered in the weakened outflow and the change in nutrients available for phytoplankton growth. This supports the hypothesis that the Amazon River is not the major nitrogen source for primary producers (Dippner et al., 2024; Umbricht et al., 2024).

The wide variability of δ¹³C in the surface (-27.3‰ to -15.7 ‰) and the MWC (-26.9‰ to -17.3 ‰) indicates that the particulate matter is likely a blend of terrestrial C₃ plants which have a typical δ¹³C value of approximately -27 ‰ to -32‰ (Peterson and Fry, 1987; Wada et al., 1987) and marine phytoplankton which have a typical δ¹³C range of -18‰ to -20 ‰ (Goericke et al., 1994), with more data fell into phytoplankton predominance. The highest δ¹³C values (averaging -20.9 ± 0.5‰.) were found in the coastal habitats (YPC, OPC, and WPM habitats), coupled with elevated nutrients, biomass (PC and Chla), and with the higher carbon fixation rate documented in the area (Alriyami et al., 2024 ¹ ; Montoya et al., 2019; Umbricht et al., 2024). Conversely, the most negative δ¹³C occurred in the RI habitat (-27.3‰), characterized by proximity to the river mouth, where terrestrial input is most dominant. This observation is further supported by the hydrographic data, having extremely low surface salinity (min 0psu) and the highest nitrate concentrations (12µM) in our data set ( Figures 2 , 3 ; Supplementary Figure S3 ).

The PC: Chla ratio provides an important indicator of the efficiency of the phytoplankton community in converting nutrients into biomass (Furuya, 1990). Deep cells within the euphotic zone, adapted to low light and close to the source of new nitrogen in the nitracline, tend to have low PC: Chla and C:N ratios. Conversely, cells higher in the euphotic zone, which are light-adapted but nutrient-depleted, may exhibit different ratios (Marañón et al., 2003). In our dataset, the PC: Chla ratios tended to be higher at the surface and decreased with depth, higher during spring than during summer and fall cruises ( Supplementary Figure S5 ). The relationship between the PC: Chla ratio and the C:N ratio further supports the idea that most PC came from living sources, particularly away from the river mouth (Cifuentes et al., 1988). The PC: Chla of living phytoplankton generally falls between 40 and 140 (g/g), and the higher values (> 200 g/g) indicate that detrital and degraded materials are significant components of the PC pool (Eppley and Peterson, 1979; Liu et al., 2019). Most of the OM in our study fell within the range of living material contribution, except the RI habitat, which appears dominated by terrestrial sources (high PC : Chla ratio) that might be colonized by heterotrophic bacteria (moderate C:N ratio). Similarly, the relationship of δ¹³C and PC : Chla in the surface and MWC emphasized the role of spring and fall bloom on the organic matter pool. The regression analysis indicated that the F-statistic was notably higher, with significant p-values observed in both spring and fall compared to late summer ( Supplementary Figure S6 ).

The PCA analysis explained 47% of the total variance (30% by PC1 and 17% by PC2). It showed that biogeochemical parameters (PC, C:N ratio, and δ¹³C) correlated positively with SST and negatively with MLD and nitrate concentrations. Warmer waters, shallower MLD, and low nitrate likely supported higher biomass stock, high C:N ratio, and more positive δ¹³C ( Figure 14 ). The plume core habitats had the warmest waters, shallower MLD, and higher nitrate concentrations, which enhanced phytoplankton growth and biomass (i.e. fluorescence), leading to increased organic carbon production (high [PC]) and a shift towards the carbon-rich organic matter (high C:N ratios). The elevated δ¹³C in warmer water might stem from the influence of temperature on phytoplankton growth and production rates. Liu et al. (2022) argued that water temperature might better predict δ¹³Csp than the DIC source. Given the seasonal and spatial variation of the measured SST in our study, this might have had a marginal effect in δ¹³C.

Further offshore, the thermally stratified water column limits nutrient replenishment from deeper waters, favoring the dominance of small phytoplankton that can thrive in nutrient-limited environments. The negative correlation between MLD and nitrate concentrations further supports this, as lower nitrate concentrations are typically associated with reduced nutrient input or active biological uptake, driving a shift towards higher C:N ratios indicative of nitrogen limitation. The more negative δ¹³C values observed under these conditions may reflect higher dissolved [CO_2aq] in oceanic waters or small cell dominants with lower growth rate. Collectively, these results highlight the importance of physical structure and nutrient dynamics in shaping the spatial and temporal distribution of biogeochemical parameters of organic matter pool.

This study investigates the role of environmental conditions and physical and biochemical parameters in shaping the productivity and particulate carbon composition of the Amazon River Plume and surrounding oceanic waters during three different outflow regimes.

We found that the plume waters greatly influenced the hydrodynamic process in the study area; therefore, the biogeochemical process related to the water column structures is also greatly influenced. Multiple indicators pointed towards the predominance of in situ phytoplankton synthesized organic matter at the surface and throughout the water column. Firstly, the spatial and vertical distribution trends of [PC] are consistent with favorable growth conditions of warm SST, high nutrient concentration, shallow MLD, and phytoplankton biomass (i.e. Chla). Also, as evidenced by average molar C:N ratios, which were within the typical range for phytoplankton (i.e., 6-10). Secondly, the δ¹³C values observed across different seasons indicate a phytoplanktonic origin, with the surface δ¹³C (-27.3‰ to -15.7 ‰) and the MWC (-26.9‰ to -17.3 ‰), with peak enrichment occurring in habitats associated with maximum production conditions and lowest δ¹³C value in the river mouth area. Additionally, the consistent linear correlation between PC and Chla across all seasons and PC: Chla ratios mostly below 200 (g/g) highlights in situ production with minimal terrestrial influence on the PC stock. The insights gained from this study provided a foundation for improving ecological models and predicting the impacts of environmental changes on the productivity of the river-influenced coastal systems.