The Northern Gulf of Mexico is a very dynamic and high-contrast ecosystem. In the oligotrophic offshore regions, phytoplankton are nutrient-limited and primary production is low. Near the coast, the Mississippi River supplies nutrients (primarily nitrate) in such quantities that large regions become anoxic during summer (Turner et al., 2008). The Mississippi also carries large amounts of fine, suspended sediment, which settles near the Mississippi Delta and dominates the seafloor sediment there (Balsam and Beeson, 2003; Ellwood et al., 2006). This eutrophic river plume is advected by the strong currents in the Gulf of Mexico depending on the wind conditions and the position of the loop current (Walker, 1996; Walker et al., 2005; Schiller et al., 2011), and can at times be detected as far south as the Florida Straight (Hu et al., 2005; Schiller and Kourafalou, 2014). The complex interaction between different waters (with differing nutrient and trophic states) and highly variable currents leads to a very heterogeneous and dynamic system. This complexity likely affects particles that sink from the surface, ultimately supply carbon to the deep sea community, and play an important role in the carbon cycle. However, to date, knowledge of this important pathway and how it varies spatially and temporally in the Northern Gulf of Mexico is very limited (Davies et al., 2010; Mienis et al., 2012; Prouty et al., 2016). This limitation became especially apparent during the Deep Water Horizon (DWH) oil spill when it was realized that sinking particles were concentrating and transporting large amounts of oil to depth (Passow et al., 2012).
The Macondo DWH oil spill (from 20 April 2010 to 15 July 2010) was the second largest oil spill in history and unprecedented for several reasons, one of them being the observation that large amounts of the oil were incorporated into marine snow and deposited on the seafloor (Passow et al., 2012; Daly et al., 2016). This marine oil snow sedimentation and flocculent accumulation (MOSSFA) event was an unexpected fate for a large amount of the spilled oil: the estimates that 5–10% or even 15% of the released oil was transported to the sea floor via MOSSFA (Valentine et al., 2014; Chanton et al., 2015; Stout et al., 2017) are almost certainly too low (Passow and Ziervogel, 2016).
Marine snow originates in the surface ocean and forms via the interaction of phytoplankton, zooplankton, bacteria and lithogenic matter. Several of the organisms involved have unique elemental compositions and can produce minerals with high excess density (compared to seawater). For example, phytoplanktonic coccolithophores and zooplanktonic foraminifera and pteropods produce shells that contain calcium carbonate (CaCO3). Phytoplanktonic diatoms or radiolarians produce cell walls that contain the mineral biogenic silica (bSiO2). Most other planktonic organisms, such as bacteria and most zooplankton are composed primarily of organic compounds. In the open ocean, the composition of this marine snow is determined by the abundance and species composition of the plankton, with a higher abundance of coccolithophores causing higher CaCO3 concentrations in marine snow, whilst a higher abundance of diatoms causes a higher proportion of bSiO2. In near-shelf systems or areas with high dust inputs, terrestrial matter (in particular ‘lithogenic matter’) can make up a significant fraction of marine snow.
Marine snow particles can sink at a variety of speeds ranging from only few cm per day to several hundreds of meters per day (Turner, 2002; Alonso-González et al., 2010; McDonnell and Buesseler, 2010), but are commonly thought to sink at an average of 10–150 m d–1 (McDonnell and Buesseler, 2010; Villa-Alfageme et al., 2016). Depending on the sinking speed of an individual aggregate, marine snow can be transported horizontally over several hundreds of kilometers in regions with strong currents (Siegel and Deuser, 1997). The location where an aggregate eventually lands on the seafloor could thus differ markedly from the location where it was formed. Whilst sinking through the water column, marine snow is reworked and much of it is lost due to remineralization and grazing, leading to a rapid decline in flux with depth (Martin et al., 1987; Buesseler et al., 2008). On the other hand, aggregates also scavenge dissolved or non-sinking particles during sinking, which alters their composition (Passow and De La Rocha, 2006; De La Rocha and Passow, 2007).
Marine snow is known to transport contaminants including oil residues to the seafloor (Paasivirta et al., 1982; Broman et al., 1987; Baker et al., 1990; Lipiatou et al., 1993; Lee and Page, 1997). Hydrophobic organic contaminants can associate with particulate and dissolved organic carbons (Hites and Eisenreich, 1987; Wang and Zhang, 2014), which may lead to their incorporation into marine snow and subsequent settling to the seafloor. Oil residues in the form of polycyclic aromatic hydrocarbons (PAHs) have been found in sediment traps in lakes (Baker et al., 1991), coastal regions (Paasivirta et al., 1982; Broman et al., 1987), and the deep sea (deeper than 1000 m depth; Lipiatou et al., 1993; Yan et al., 2016).
After DWH, high amounts of petrogenic PAHs were found in sediment traps even months after the well was closed (Yan et al., 2016). To fully assess when the ecosystem and fluxes have returned to baseline levels after a spill, the background concentrations need to be known. Meeting this need is not trivial, because sinking aggregates can contain PAHs from a variety of sources, including naturally occurring PAHs that are petrogenic (petroleum-derived; e.g., from natural seeps) and pyrogenic (combustion-derived; e.g., from wildfires) as well as anthropogenic petrogenic (e.g., engine oils and chronic oil leakage) and pyrogenic (e.g., automobile, industrial and power plant emissions). For the Gulf of Mexico, a pre-spill baseline of measured marine snow fluxes does not exist, which has two consequences. Firstly, it is not known at what time point sedimentation rates return to usual conditions (both in terms of magnitude and PAH contents) – in other words, damage assessment is hampered. Secondly, a detailed understanding of seasonal and spatial variability in ‘background’ fluxes in the Gulf of Mexico is necessary for future oil spill response management when evaluating the potential for MOSSFA formation.
The purpose of this study was to identify what determines the magnitude, composition and temporal variability of deep (>1000 m depth) particle fluxes in the Northern Gulf of Mexico. We hypothesized that deep fluxes are strongly influenced by the Mississippi River discharge and the strong currents and that they normally do not carry large amounts of fossil carbon contaminants. We here present marine snow flux data collected using sediment traps from three sites in the Northern Gulf of Mexico from 2012 to 2016. Analysis of oil components in the flux offers additional insights into different aggregate transport pathways. These data provide a post-DWH particle flux baseline and novel insights into what drives particle export spatially and temporally in this region.
Three long-term monitoring sites were chosen in the Northern Gulf of Mexico (Table 1 and Figure 1). The first site – the ‘DWH site’ (R/V Oceanus Site 26; 28°40’N, 88°21.6’W; 1660 m deep) – is located in the Mississippi Canyon lease area in close proximity (~5 km) to the DWH blowout location and near the main Mississippi River Delta (~70 km southeast). This site, also referred to as ‘OC26’ in the literature, is monitored frequently and is the location of the sediment trap deployed after DWH (Yan et al., 2016). The second site – the ‘Seep site’ (27°22.5’N, 90°30.6’W; 1380 m deep) – is located in Green Canyon lease block GC600 within a very active natural oil seep area (Roberts et al., 2010), which often has extensive oil slicks at the surface ocean (Macdonald et al., 1993; MacDonald et al., 2002). This high seepage activity has recently been linked to elevated surface chlorophyll a concentrations (D’souza et al., 2016). Our third site – the ‘Reference site’ (27°31.5 N, 89°42.6 W; 1160 m deep) – will be used as an index for typical background conditions, although sediment analysis suggests that this site is also at times exposed to oil from natural seeps (Fisher et al., 2014). This site is located in Atwater Valley lease block AT357 at the largest currently known deep-water coral assemblage in the Gulf of Mexico (Doughty et al., 2014). Both Seep and Reference sites were not visibly impacted by DWH (Fisher et al., 2014). Temperatures at the traps were between 4.2 and 4.5°C at all sites. The average current speeds (±SD) ~45 m below the trap (~75 m above the bottom) were < 3.8 ± 2.0 cm s–1 (n = 19664) and < 4.9 ± 3.0 cm s–1 (n = 9645) at the DWH and Seep site, respectively (Diercks et al., 2017). Sediment trap data are generally considered reliable as long as current velocities remain under 10 cm s–1 (Gardner, 1980).
|Site||Position||Trap type (number of cups)||Deployment period||Collection period per cup (d)||Water depth (m)||Deployment depth (m)|
|DWH||28°40.8 N 88°21.7 W||McLane (21)||28 June 2012 to 12 September 2016||16 or 18||1660||1540|
|Seep||27°22.5 N 90°30.7 W||McLane (13)||16 April 2012 to 15 April 2016||11, 18, 24, 27, 28||1380||1260|
|Reference||27°31.5 N 89°42.6 W||Kiel-trap (20)||16 April 2012 to 25 April 2016||17 or 18||1160||1040|
Sediment traps (Parflux Mark 78H, McLane Research Laboratories and Kiel Trap, K.U.M. Umwelt- und Meerestechnik Kiel GmbH) have been deployed since April 2012, collecting sediment fluxes at 120 m above the sea bed (water depths of 1540 m, 1260 m and 1040 m at the DWH, Seep and Reference sites, respectively). Here we present data until September 2016. All three time-series traps had catchment areas of 0.5 m2, covered with a hexagonal lattice grid baffle that reduces wash-out. The multi-bottle turntables allowed for the collection of 13–21 time-series samples per deployment period (~1 year), collecting for 11–28 days each (Table 1). After each of the collection periods, traps were recovered and re-deployed within a few days to generate a continuous time series.
The DWH site trap was successfully deployed for the entire period. However, towards the end of several deployment periods, the trap funnel clogged and the subsequent samples were lost (26 June–15 September 2014, 29 March–15 September 2015, and 19 February–12 September 2016). This clogging was likely caused by high export rates, such that the average annual fluxes presented for the DWH site are likely underestimates (see Section 4.1). The trap at the Seep site sampled successfully for the entirety of all deployment periods. The trap at the Reference site sampled successfully between April 2012 and January 2015. However, during the 2014–2015 deployment a mechanical failure occurred after 22 August 2015 (during cup 7 out of 13) and the remaining samples were lost. The trap was serviced before redeployment for the next year but did not rotate, so that no samples were collected during the 2015–2016 deployment.
Prior to deployment, sample bottles were filled with filtered seawater to which NaCl (Pro analysis, Fisher) was added to a final salinity of ~40 and the preservative HgCl2 to a final concentration of ~0.14%. Using HgCl2 rather than buffered formalin allows for C-isotopic determinations. Upon retrieval, cups were stored dark and cold (4°C) until processing. First, cups were gently mixed and, after the material was allowed to resettle for 7 days, the supernatant was sampled for pH, salinity and nutrients. Lower pH, salinity or nutrient concentrations than expected indicates a preservation anomaly or wash out. Preservation was as expected in all cups and no signs of degradation were observed. Some cups with high sedimentation fluxes showed signs of bSiO2 dissolution, but potential dissolution (estimated by assuming that excess Si(OH)4 in the supernatant compared to ambient water originated from dissolution) was equivalent to < 10% of measured bSiO2 flux. We did not correct for potential dissolution, but note that high bSiO2 fluxes are potentially slightly underestimated (by < 10%).
Sample material was split repeatedly into five or ten subsamples, using a sample splitter (WSD–10, McLane Research Laboratories). During splitting artificial seawater was used for rinsing. The splitting introduces an error of about 3–5% in terms of mass flux (unpublished data; Honjo et al., 2008). Individual splits were used for different analyses. Appropriate split size for any biochemical measurement depended on the total amount of material collected per cup and on the method, varying between 1/10 and 1/2,500. Trap material was not screened or routinely picked before filtration, as we consider moults, carcasses, large shells or scales to be part of the flux. Detailed notes for each cup and split can be found in the raw data. (DOI: https://doi.org/10.7266/N7F47M6M, DOI: https://doi.org/10.7266/N79C6VHB, DOI: https://doi.org/10.7266/N7XK8CZS, DOI: https://doi.org/10.7266/N78W3BQJ, DOI: https://doi.org/10.7266/N7H993KF, DOI: https://doi.org/10.7266/N7CJ8BVQ, DOI: https://doi.org/10.7266/N7416VD0, DOI: https://doi.org/10.7266/N7PN93PS, DOI: https://doi.org/10.7266/N7JW8BXM, DOI: https://doi.org/10.7266/N7CR5RQT, DOI: https://doi.org/10.7266/N7VT1QGS, DOI: https://doi.org/10.7266/N7BR8QKF and DOI: https://doi.org/10.7266/N71C1V8T)
Total mass flux was calculated from dry weight (DW): quadruplicate splits were filtered onto pre-weighed (AE160, Mettler Toledo) and pre-combusted (450°C for 4–6 hours) GF/F filters (25-mm diameter, nominal pore size 0.7 µm, Whatman), briefly rinsed with Milli-Q water, dried at 60°C (4–6 hours), and weighed. DW was defined as the difference between dried and pre-weighed filter. The filters were then used to determine particular organic carbon (POC), particulate organic nitrogen (PON) and particulate inorganic carbon. Duplicate filters were fumed with 10% HCl to remove inorganic carbon. All filters were then analyzed using a CHN elemental analyzer (CEC 44OHA; Control Equipment, now Exeter Analytical). Particulate inorganic carbon was defined as the difference of the acidified and non-acidified particulate carbon (Shipe and Brzezinski, 2003). Calcite (CaCO3) content was calculated from particular inorganic carbon by assuming a molecular weight of 100. For some traps we also analyzed for combustible and non-combustible matter by combustion (450°C for 4–6 hours) and reweighing a third time, though the data are not presented here. Biogenic silica (bSiO2) was analyzed by filtering splits onto 0.6-µm polycarbonate filters (47-mm diameter, Millipore) (DeMaster, 1981; Mortlock and Froelich, 1989). Filters were hydrolyzed with Na2CO3, running a 0.5 to 5 hour time series, and analyzed colourimetrically (Shipe and Brzezinski, 2001). The change in the slope of dissolution rate indicates the shift from bSiO2 to lithogenic silica dissolution and was used to determine bSiO2 concentration. bSiO2 was assumed to have a molar mass of 67.
The concentration of lithogenic material (Lith) was calculated as:(1)
POC was converted to total organic matter using the commonly used conversion factor of 2.2 based on reported conversion factors ranging between 1.9 and 2.3 (Honjo, 1980; Tsunogai, 1987; Klaas and Archer, 2002; Boyd and Trull, 2007; Salter et al., 2010).
For analysis of transparent exopolymer particles (TEP), a series of three to five sub-splits (ranging between 1/2,500 and 1/12,500 or 1/12,500 and 1/62,500, depending on the TEP concentration and sample volume) were filtered in triplicate onto 0.4-µm polycarbonate filters (25-mm diameter, Whatman) as described in Passow and Alldredge, (1995), and corrected using unstained and blank filters as detailed in Passow et al. (2001). The slope of the linear relationship was used to calculate TEP concentration. Xanthan gum was used to calibrate the Alcian Blue solution, with TEP expressed as Xanthan gum equivalent.
Fluxes for each component (Fx) were calculated as:(2)
where m̅x is the average mass per cup (after normalizing for splitting), x is the component, A is the trap area (0.5 m2), and t is the collection period for each cup (in days). Where multiple replicates were analyzed, the standard deviation (SD) is stated. No SD is given for TEP and bSiO2 flux because these values were based on the slope of a linear regression of different sample concentrations.
Flux and composition of hydrocarbons (C16–C36n-alkanes, selected polycyclic hydrocarbons, pristane, phytane and hopanes) were measured for the period of April 2012–April 2013 for the Seep and Reference sites, and for the period between July and September 2012 at the DWH site. Analysis for hydrocarbons and olefins was carried out as described by Yan et al. (2016). A full list of all measured compounds can be found in the supplementary material (Table S1). ΣPAH fluxes were calculated by multiplying ΣPAH concentrations with DW flux. To distinguish between different sources, we used the sample indices and criteria used by Yan et al. (2016) to identify the hydrocarbon sources in marine snow after the DWH spill.
The carbon preference index (CPI) refers to the ratio of alkanes with an odd number of carbon atoms over those with an even number of carbon atoms. Higher (terrestrial) plants have been shown to produce a higher proportion of odd than even hydrocarbons with a CPI of ≥ 5. For phytoplankton, data are not conclusive, though they generally tend to produce shorter alkanes (Cn with n < 20) (Volkman et al., 1998). Fossil fuels have a CPI of ~1. We calculated the CPI index for alkanes between C24 to C36 following:(3)
As boundary values, we used the values applied by Yan et al. (2016), which indicate that samples with a CPI < 1.6 are dominated by crude-oil alkanes.
To distinguish between pyrogenic (combustion) and petrogenic (crude oil) sources, we used two indices. Pyrene is thermodynamically more stable than its homologue fluoranthene. As a consequence, high-temperature processes such as combustion lead to a higher ratio of the unstable to the stable homologue. A ratio of fluoranthene to fluoranthene + pyrene (Fl/(Fl+Py)) > 0.5 (i.e., a high ratio of unstable to stable homologue) suggests a dominance of pyrogenic PAH sources, while a Fl/(Fl+Py) < 0.4 suggests a dominance of petrogenic PAH sources (Budzinski et al., 1997; Yan et al., 2016). We also used the index C0/(C0+C1), which is the ratio of parent phenanthrene to phenanthrene plus its monomethyl homologues (2-methylphenanthrene, 1-methylphenanthrene, 3-methylphenanthrene, and 4-methylphenanthrene). Methylation occurs during the formation of PAHs, and crude oils are dominated by alkylated PAHs (Blumer, 1976). At high temperatures (i.e., combustion) the less stable alkyl group is lost, leading to low levels of methylation in combustion products. Following Yan et al. (2016), C0/(C0+C1) ≤ 0.5 was interpreted as a dominance of PAHs from crude oil.
Finally, we calculated the average chain length (ACL) of n-alkanes as:(4)
where Ci is the concentration of the n-alkane with i number of C atoms (Poynter and Eglinton, 1990).
To categorize the dominant hydrocarbon sources, we used overall PAH concentration, ACL, the three indices (CPI, Fl/(Fl+Py), C0/(C0+C1), and isotopic composition. In unclear cases, a final judgment was influenced by the occurrence and concentration of individual PAHs and their most likely source (for example, 5–6 ringed and methylated PAHs indicating pyrogenic and petrogenic sources, respectively).
Prior to isotopic analysis samples were dried, ground, treated with 10% HCl to remove carbonates, rinsed and freeze-dried. Samples for Δ14C-POC analysis were combusted in quartz tubes for 18 hours at 850°C, and purified CO2 was prepared as graphite targets and analyzed by accelerator mass spectrometry (Vogel et al., 1984). Values are reported according to the Δ notation put forth in Stuiver and Polach (1977). The Δ notation normalizes the radiocarbon content of a sample to a nominal δ13C value (–25‰) and the collection time. The scale is linear and starts at –1000‰ when a sample has essentially 0% modern carbon, which would represent petroleum residue (McNichol and Aluwihare, 2007). Analytical reproducibility was on the order of 3‰. For details see Chanton et al. (2017).
Primary production (PP) estimates were based on satellite data and the Vertically Generalized Production Model (VGPM) which estimates light-dependent, depth-resolved carbon fixation (Behrenfeld and Falkowski, 1997). Model results were obtained from the Ocean Productivity site (http://www.science.oregonstate.edu/ocean.productivity/). PP was calculated as the median for 8-day composites for 0.5-degree boxes around the study sites from January 2010 to November 2016.
Discharge and nitrate + nitrite (N) concentrations of the Mississippi River were obtained from USGS (https://waterdata.usgs.gov/) for the time period between 1 January 2010 and 9 September 2011 at Francisville, LA (site ID USGS 07373420; samples approximately every 2 weeks), and for the time period between 9 September 2011 and 31 December 2016 at Baton Rouge, LA (site ID USGS 07374000; high resolution sampling with several samples daily). The two sites are < 50 km apart from each other, and a comparison of discharge and nutrient concentrations at the two sites for 2012 showed that the stream conditions varied little between the two sites.
The topography of the study area was downloaded at 1-minute resolution from NOAA using the getNOAA.bathy function in the R package marmap (Amante and Eakin, 2009).
Seasonal patterns in POC flux and PP at the three sites were determined with a smoothing function that uses cyclic cubic regression splines from the mgvc package in R. As these patterns are for illustrative purposes, no further statistics were carried out. To calculate annual fluxes, measured fluxes were estimated for every day during the study periods using linear interpolation between the mid-points of each cup-sampling period. The running sum for 365 consecutive days was calculated, and average and SD were calculated for all running sums (n = 950, 1077 and 477 at the DWH, Seep and Reference sites, respectively). A higher number of observations n indicates a longer time series. The relationship between flux components was tested using simple linear regression. As the data were right-skewed and contained zeros; linear regression was performed on both untransformed and root-cube transformed data. The level of statistical significance was the same for both regressions (transformed versus untransformed), and the R2 values were similar (slightly higher for cube-root transformation in 17 out of 21 regressions). As the interpretation is not compromised, we state the results of the untransformed regressions here.
Hydrocarbon composition was analyzed using multivariate ordination analysis from the vegan package in R (R Core Team, 2015; Oksanen et al., 2016). In addition to our 2012–2013 samples, we included the sediment trap samples collected at the DWH site for the year following the spill (Yan et al., 2016).
We used 40 groups of hydrocarbons (Table S1) to calculate dissimilarities between samples using non-metric multidimensional scaling (NMDS). We applied Bray-Curtis dissimilarities, two dimensions, and Wisconsin double standardization, which reduces the influence of samples with high concentrations. The stress of the solution was low (stress = 0.12). The solution was centered and scaled so that one unit corresponds to halving the similarity between two samples. The solution was rotated so that the first axis approximates the gradient in ΣPAH concentrations, and the second axis approximates the shift from petrogenic to pyrogenic sources based on methylation and number of aromatic rings. Detailed explanations of the functions can be found in the metaMDS help package (Oksanen et al., 2016).
The differences between the three sites (DWH, Seep and Reference sites) and between the five periods identified for the Seep site (see Section 3.4) – referred to as a priori groups – were tested with non-parametric multivariate analysis of variance (PERMANOVA) (Anderson, 2001). Dissimilarity indices were calculated after transformation (as described above) using the vegdist function, whose results are identical to the metaMDS function but differ in its output format. Significant differences between a priori groups were tested using the adonis function with 999 random permutations. Significant differences in group centroids calculated using adonis can be caused either by differences in the centroid locations or by differences in data spread (‘dispersion’) (Anderson, 2006). We tested for differences in dispersion using the function betadisper and the ANOVA-like function permutes (with 999 random permutations) as well as Tukey’s test. Differences in dispersion never compromised the results of diagnosed differences in centroid location.
The DWH site was by far the most productive site. Located just offshore of the main Mississippi outlet, it showed the highest surface primary production (PP) rates of all three sites (mean ± SD of 1.2 ± 1.2 g m–2 d–1, n = 223) with a maximum of 6.7 g m–2 d–1 (Figure 2a). PP was lowest in autumn (September–October). The climatology suggests that the DWH site experiences an annual winter bloom consistently around February. During summer, the PP is more variable but suggests peak values around July, though this bloom does not appear to occur every year (Figure 2a).
The Seep and Reference sites show very similar annual PP rates (mean ± SD of 0.4 ± 0.2 g m–2 d–1 at both the Seep and Reference sites, n = 223) and maximum PP of < 1 g m–2 d–1 (Figure 2b, c). Similar to the DWH site, both sites consistently showed lowest PP values in September–October and a winter bloom in February. However, there was no obvious summer bloom (though occasionally slightly elevated PP rates were observed during June–July) and overall PP rates were much lower than at the DWH site.
At the DWH site, fluxes of all components, with the exception of CaCO3, were higher compared to the other two sites (Figure 3). Total matter fluxes indicated the transport of an annual mean ± SD of 175 ± 52 g DW m–2 year–1 at the DWH site, with average daily fluxes ranging from 99 to 2,228 mg DW m–2 d–1 (Table 2). In any one cup, the bulk of these fluxes was comprised of lithogenic material (mean of 69 ± 7%, n = 56), with organic matter (2.2 × POC), bSiO2, and CaCO3 making up roughly the same contribution (9 ± 3%, 9 ± 2% and 12 ± 8%, respectively; Table 2). POC fluxes averaged 17 ± 13 mg C m–2 d–1 (n = 58, range of 5–64 mg C m–2 d–1; Figure 2d, Table 2). Annual flux rates are likely underestimates, as peak fluxes were likely missed due to trap clogging (see Section 4.1).
|Site||Daily Fluxes (mg m–2 d–1)b||Annual Fluxes (g m–2 yr–1)c|
|avg ± sd||443 ± 347||17 ± 13||2 ± 2||45 ± 44||41 ± 37||47 ± 38||321 ± 289||14 ± 4||18 ± 8||14 ± 2||126 ± 51|
|DWH||min-max||99 – 2228||5 – 64||0 – 9||2 – 226||9 – 176||0 – 185||52 – 1940|
|%DW||4 ± 1||1 ± 0||9 ± 3||12 ± 8||69 ± 7|
|avg ± sd||255 ± 126||10 ± 5||1 ± 1||26 ± 14||21 ± 13||55 ± 62||160 + 94||8 ± 1||7 ± 2||17 ± 9||54 ± 12|
|Seep||min-max||27 – 643||1 – 26||0 – 4||3 – 56||4 – 56||0 – 350||0 – 495|
|%DW||4 ± 2||1 ± 0||9 ± 4||21 ± 17||61 ± 15|
|avg ± sd||103 ± 118||6 ± 5||1 ± 1||13 ± 10||10 ± 11||25 ± 35||58 ± 93||4 ± 1||3 ± 0||6 ± 2||19 ± 5|
|Ref.||min-max||3 – 639||1 – 25||0 – 5||1 – 45||0 – 48||0 – 178||0 – 504|
|%DW||7 ± 4||1 ± 1||9 ± 4||29 ± 31||50 ± 23|
At the Reference site, fluxes of all components were lowest (Table 2 and Figure 3). Average annual total matter fluxes were approximately 20% of the fluxes observed at the DWH site. Organic matter, bSiO2 and lithogenic annual fluxes were 25%, 16% and 15% of the respective fluxes at the DWH site. The exception was CaCO3, which was 46% of the flux observed at the DWH site. This exception is also reflected in the higher percentage of CaCO3 in fluxes in each cup (29 ± 31%, n = 46) compared to that of the DWH site (12 ± 8%, n = 58). Similar to the DWH site, lithogenic matter made up the bulk of the fluxes in any one cup (mean of 50 ± 23%, n = 46), albeit to a lesser extent than at the DWH site and with a more variable contribution. bSiO2 contributed 9 ± 4% (n = 46) of the flux. Average annual total matter fluxes were 32 ± 5 g DW m–2 d–1 at the Reference site, with fluxes in each cup ranging from 3 to 639 mg DW m–2 d–1 (Table 2). POC fluxes averaged 6 ± 5 mg C m–2 d–1 (range: 1–25 mg C m–2 d–1).
The Seep site appeared to be in between the DWH and Reference sites in terms of absolute fluxes and flux composition (Table 2), though it is farthest to the west (Figure 1). Average annual total mass flux was 85 ± 15 g DW m–2 d–1, with fluxes in each cup ranging from 27 to 643 mg DW m–2 d–1 (Table 2). Annual fluxes at the Seep site are thus ~50% of the fluxes at the DWH site during this time frame, but 2.5 times higher than those at the Reference site. In terms of average annual fluxes, lithogenic matter made up 60 ± 15% (n = 60) of the flux in any one cup, a contribution that is lower than that at the DWH site (69 ± 7%, n = 56) but higher than at the Reference site (50 ± 23%, n = 46). The contribution of biogenic minerals (bSiO2 and CaCO3) to flux was similar at the Seep and Reference sites (bSiO2: 9 ± 4% at both sites; CaCO3: 21 ± 17% and 29 ± 31%, respectively). Daily POC fluxes averaged 10 ± 5 mg C m–2 d–1 (range: 1–26 mg C m–2 d–1), and thus half of those observed at the DWH site but overall higher than those at the Reference site (Table 2).
Most flux compounds were significantly correlated with each other (Table 3). The strongest correlation was observed between total mass flux and lithogenic flux (R2 = 0.94, p < 0.01, n = 162), POC and PON (R2 = 0.94, p < 0.01, n = 166), and total mass flux and POC (R2 = 0.77, p < 0.01, n = 166). No correlation was observed between CaCO3 and any of the other compounds. The C:N ratios of sinking organic particles (mean of 9.2 ± 2.1 mol mol–1, n = 165) were in the range of those from traps at this depth (Schneider et al., 2003), with higher C:N ratios (9.9 ± 2.1 mol mol–1, n = 58) at the near-shore DWH site compared to the two more off-shore stations (8.9 ± 1.2 mol mol–1, n = 61, at the Seep site and 8.7 ± 2.6 mol mol–1, n = 46, at the Reference site).
|Flux componentsa||DW (mg m–2 d–1)||POC (mg m–2 d–1)||PON (mg m–2 d–1)||Bsi (mg m–2 d–1)||Lith (mg m–2 d–1)||TEP (mg XGeq m–2 d–1)|
|POC (mg m–2 d)||0.77
|PON (mg m–2 d)||0.72
|Bsi (mg m–2 d)||0.67
|Lith (mg m–2 d)||0.94
|TEP (mg XGeq m–2 d)||0.56
|CaCO3 (mg m–2 d)||0.10
All data are available at https://data.gulfresearchinitiative.org/ (see Section 2.2 for DOIs).
At the DWH site, fluxes followed a quasi-seasonal pattern except for CaCO3. CaCO3 fluxes did not show any regularity, but appeared to decrease throughout the sampling period: fluxes were higher and more variable during June 2012–June 2013 (57 ± 56 mg CaCO3 m–2 d–1, n = 19) than afterwards (42 ± 25 mg CaCO3 m–2 d–1, n = 39). Total mass flux, POC, PON, bSiO2, TEP and lithogenic matter fluxes were highest during March–May 2013, February 2014, January–March 2015 and January–February 2016 (Figure S1d). These dates correspond to the annual winter bloom observed at the DWH site (Figure 2a). Based on other evidence (see Section 4.1) we believe that a second, larger export event occurred later in the year, causing the clogging of our traps at the DWH site. Clogs occurred in July 2013, July 2014, April 2015, and February 2016. These clogs caused the loss of all subsequent samples, potentially leading to a significant underestimate of particle flux at the DWH site. No trap clogging was observed earlier, in 2012 (this study) or during 2011 (Yan et al., 2016).
At the Reference site, all fluxes except CaCO3 fluxes peaked in summer (April–May 2012, July 2013, May–July 2014) and were lowest around December (Figure S1). As for the DWH site, CaCO3 fluxes showed no seasonal cycle, but were higher in April–July 2012 (> 40 mg CaCO3 m–2 d–1) and consistently lower afterwards.
The Seep site did not show a clear seasonal cycle for any of the fluxes, and fluxes were relatively constant throughout the sampling period. The only exceptions were CaCO3 fluxes in 2012–2013, which were ~4 times higher than during the following years (Figure S1).
In the open ocean, particle flux at depth is generally linked to the production of particles in the surface waters. Particle fluxes are often compared to shallower fluxes or PP to characterize the system. For the Seep and Reference sites, we found that PP (as derived from satellite data for an area of ~50 × 50 km2 around the traps) and particle flux at depth (Figure 2) had no obvious relationship. At the DWH site, POC flux seemed to follow peaks in PP (Figures 2a, d and 4). The correlation between POC flux and concurrent PP estimates was significant (p < 0.01, n = 58; log-log transformation) but the explained variability in fluxes as a function of PP was low (R2 = 0.11).
Sinking material at the DWH site (June–September 2012) contained relatively high concentrations of the sum of all measured PAHs (∑PAH) at 0.27 ± 0.04 µg g–1 (n = 4), with a high proportion of 4–6-ringed PAHs (Figure 5). ∑PAH at the Seep site decreased in concentration throughout the study period, with the highest concentration observed during 10–20 June 2012 (1.8 µg g–1) and lowest in February–March 2013 (< 0.1 µg g–1). This decrease coincided with a decrease of 5–6-ringed and methylated PAHs, and a proportional increase in 3-ringed PAHs (Figure 5). Trapped material at the Reference site (April 2012–April 2013) included only low concentrations of ΣPAHs (0.07 ± 0.03 µg g–1, n = 18) which were dominated by low-weight molecular PAHs and no detectable 5–6-ringed PAHs (Figure 5). Based on ∑PAH at the Reference site, background levels of ∑PAH concentrations appeared to be < 0.15 µg g–1 (maximum concentration observed at the Reference site).
∑PAH fluxes were lowest at the Reference site with a mean of 0.006 ± 0.005 µg m–2 d–1 (April 2012–April 2013). Fluxes at the DWH site were higher and fairly consistent during the short sampling period (June–September 2012) with a mean of 0.125 ± 0.024 µg m–2 d–1. At the Seep site, ∑PAH fluxes had a mean of 0.283 ± 0.041 µg m–2 d–1 (April 2012–April 2013) and were highly variable, ranging from 0.010 to 0.413 µg m–2 d–1. Highest ∑PAH fluxes were observed between April and June 2012 with a maximum of 0.413 µg m–2 d–1. The values decreased after June, with average fluxes (over the entire sampling period) of 0.092 ± 0.103 µg m–2 d–1. Detailed figures of ΣPAH concentrations, fluxes and compositions of all three sites can be found in the supplementary material (Figures S2–S4).
Non-metric multidimensional scaling (NMDS) analysis of the composition of settled material based on 40 hydrocarbon groups confirmed significant differences between the three sites (p < 0.01; Figure 6). Whereas hydrocarbon composition remained relatively unchanged over time at the Reference site, there were clear temporal gradients in the hydrocarbon composition of samples within the DWH and Seep sites. For the DWH site, we compared the June–September 2012 samples to those from August 2010–September 2011 (Yan et al., 2016) and found the 2012 samples to be significantly different (p < 0.02) from the 2010–2011 samples: petrogenic hydrocarbons, which dominated total hydrocarbons in August–November 2010, decreased in importance from November 2010 to September 2011, and were even less prevalent during our sampling period in 2012 (Figure 6).
For the Seep site, we used seven indices to categorize the different time periods observed during 2012–2013 (Table 4). Between April and June 2012 (period A), the presence of crude oil was obvious as indicated by the high load of ΣPAH, low Fl/(Fl+Py), and prevalence of long n-alkanes. Within this period, there were strong variations in C0/(C0+C1) and CPI, which indicate combustion, de-methylation, and/or strong influences of biogenic alkanes during 27 April–29 May 2012 (cups 2–4). We distinguished two periods with high ΣPAH load and fluxes (around 16–27 April and 30 May–20 June 2012) as phase A1, and the remainder (27 April–30 May) as phase A2. Between June and August 2012 (period B), the ΣPAH load decreased to an average of 0.2 ± 0.1 µg g–1 (n = 7). The Fl/(Fl+Py) and C0/(C0+C1) values suggest a pyrogenic origin. The CPI was higher than during the preceding period, but during two intervals (20 June–1 July, cup 7; 23 July–14 August, cups 10 and 11) this index suggests the influence of petrogenic sources.
|Trap information||Polycyclic aromatic hydrocarbons (PAHs)||n-alkanes||POC|
|Site||Cup||Datea||Periodb||∑PAH contamination (µg g–1)||∑PAH flux (µg m–2 d–1)||Fl/(Fl+Py)c||C0/(C0+C1)d||CPIe||ACLf||Δ14Cg|
|Seeph||1,5,6||For A1||A1||1.0 ± 0.1||0.26 ± 0.10||0.4 ± 0.0||0.3 ± 0.2||1.2 ± 0.2||25.6 ± 0.3||–30 ± 12|
|2–4||For A2||A2||0.8 ± 0.7||0.14 ± 0.07||0.4 ± 0.0||0.6 ± 0.3||1.7 ± 0.5||26.2 ± 0.9||–34 ± 11|
|7–13||For B||B||0.2 ± 0.1||0.04 ± 0.03||0.5 ± 0.1||0.9 ± 0.0||1.5 ± 0.3||25.2 ± 0.8||–31 ± 31|
|1–8||For C||C||0.1 ± 0.0||0.04 ± 0.02||0.5 ± 0.0||0.7 ± 0.1||3.0 ± 0.4||23.9 ± 1.0||–119 ± 23|
|9–13||For D||D||0.1 ± 0.0||0.02 ± 0.01||0.5 ± 0.0||0.9 ± 0.2||3.1 ± 0.8||21.8 ± 2.9||–29 ± 33|
|DWHh||all||all||all||0.3 ± 0.0||0.11 ± 0.02||0.5 ± 0.1||0.8 ± 0.0||2.6 ± 0.5||23.6 ± 1.6||–46 ± 19|
|Referenceh||all||all||all||0.1 ± 0.0||0.00 ± 0.01||0.5 ± 0.1||1.0 ± 0.1||4.0 ± 1.6||19.7 ± 1.4||12 ± 29|
After September 2012 (periods C and D), ΣPAH contamination decreased to levels comparable to the Reference site. The low Fl/(Fl+Py) and high C0/(C0+C1) values strongly indicate that all of the PAHs originated from combustion products. The high CPI and low ACL values suggest that the majority of alkanes originated from biological sources. Interestingly, the Δ14C signal was unusually low between September 2012 and January 2013, and returned to baseline values after January 2013. We distinguished these two periods as C (low Δ14C signal) and D (high Δ14C signal), respectively.
These indices correspond well to the ordination of the NMDS analysis (Figure 6). According to the NMDS analysis, all periods (A1, A2, B, C and D) were significantly different from each other (p < 0.03) except for A2 versus A1 (insufficient data) and A2 versus B (p = 0.08). These exceptions reflect a transient period between A1 to B. Lastly, we tested whether period D at the Seep site, which was characterized by the lowest concentrations of ΣPAH, differed significantly from the Reference site, and found no significant difference (p > 0.05).
Deep (>1000 m) sedimentation rates at the three sites in the Northern Gulf of Mexico were markedly different in quality and quantity. Summarizing our analysis below, we conclude that the differences were largely driven by varying degrees of riverine, seepage and oceanic influences, which are determined by the highly variable mesoscale circulation (Liu et al., 2017). The DWH site, which is located ~70 km from the Mississippi River Delta, showed patterns of flux quantity and variability that were apparently stimulated by and also strongly linked to the variability in river discharge. The Seep and Reference sites were more influenced by the circulation pattern of the open Gulf of Mexico and differed in flux magnitude, composition and annual sedimentation rates. These differences were likely controlled by oceanic circulation at the mesoscale (10–300 km scale), and in particular by the position and variability of the Loop Current and Loop Current eddies (Liu et al., 2017). However, local influences, like natural seepage at the Seep site, also had measurable impacts on composition.
At the DWH site, we observed recurring trap clogging, which could have been caused by several processes, such as large sinking particles or sediment resuspension. Diercks et al. (2017) analysed the current velocities at the DWH trap and observed high currents (23 cm s–1) during the passage of Hurricane Issac. During this time (28 August–2 September 2012), resuspension was observed even at the depth of the DWH trap, yet the trap did not clog. Hence, even during periods of unusually high currents and resuspension, no clogging occurred, likely because resuspended material is mostly composed of mineral matter and tends to promote the formation of small aggregates (Passow and De La Rocha, 2006). We conclude that resuspension was unlikely to have caused the recurring clogging at the DWH site.
Instead, the temporal correlation between N discharge, PP and clogging (Figure 4) suggests that clogging is related to the surface community. As we do not have samples from the clogged periods, we have no direct information on what organisms may have caused the clog; however, we have indirect evidence strongly supporting our hypothesis that a sedimentation pulse caused the clogs. During the 2015–2016 collection period at the DWH site, we lost all samples after 19 February 2016 (cup 9) because of clogging. During this deployment period, we also deployed a sediment trap at 200 m depth which provided information on what was sinking out of the euphotic zone. The shallow DWH site trap collected highest total mass flux during January 2016 (cups 7 and 8), when the ratio of bSiO2 to POC was unusually high (2.9 ± 0.2 mg mg–1, n = 2, compared to 0.6 ± 0.4, n = 6, in the preceding four months), indicating export linked to diatoms or radiolarians. Microscopic analysis revealed few intact diatom frustules, but hydrolysis of organic matter revealed a great abundance of small bSiO2 fragments, which could be of either diatom or radiolarian origin. Heavy grazing is the most likely explanation for the fragmentation.
Diatom blooms have been linked to the formation of large, sticky aggregates that could cause clogging. Another prime candidate for causing the observed clogging of traps is the filamentous, N-fixing cyanobacterium Trichodesmium, which at times is common in the Northern Gulf of Mexico. Trichodesmium is known to generate large amounts of TEP during bloom termination (Berman-Frank et al., 2007), potentially causing sedimentation of mucus-rich aggregates (Bar-Zeev et al., 2013). Although Trichodesmium would no longer be recognizable in deep traps, their trichomes have been identified in shallower traps (Chen et al., 2003). Clogging could also be caused by large organisms falling into the sediment trap, such as jellyfish, which have increased in abundance in the Gulf of Mexico in recent years and are strongly linked to the Mississippi River discharge (Robinson and Graham, 2013). Lastly, we have observed that aggregates with protozoan (e.g. foraminifera and radiolarians) can be very mucus-rich and sticky at times; however, their role in flux measurements is largely unexplored.
The Mississippi River is a major driver of the nearshore ecosystem in the Northern Gulf of Mexico. It is the largest river in North America, has a catchment area of 3 million km2 and carries a high sediment load of which ~70% are fine sediments (< 63 µm, silt and clay; Thorne et al., 2008). Concentrations of fine sediments are relatively constant throughout the year, with median concentrations of 150–250 ppm (Thorne et al., 2008). The transport of Mississippi River water within the Gulf of Mexico is highly variable, spatially and temporally, and depends strongly on winds, mesoscale eddies and the loop current system (Schiller et al., 2011; Schiller and Kourafalou, 2014). Based on satellite images, the influence of Mississippi waters can be observed as far away as the Florida Straight (Hu et al., 2005). The freshwater intrusions of the Mississippi can often be detected by an increase in surface chlorophyll concentrations (Hu et al., 2005; Schiller et al., 2011; Schiller and Kourafalou, 2014). Moreover, the influence of Mississippi-derived sediment is clearly visible in the distribution of CaCO3 in seafloor sediments, where a ‘tongue’ with low-CaCO3 sediments (< 10% CaCO3 of sediment DW) extends from the mouth of the Mississippi River towards the Southeast (Balsam and Beeson, 2003; Ellwood et al., 2006). The DWH site is located directly within this low-CaCO3 region and, consistent with this long term geological signal, its average annual particle flux contained < 10% CaCO3. This low fraction of CaCO3 is a strong indicator that the DWH site is highly impacted by Mississippi discharge.
The influence of Mississippi River discharge is two-fold: (1) the high load of fine sediments and POC may lead to elevated suspended lithogenic and particulate organic material that is available for incorporation into marine snow aggregates, and (2) nutrients transported by the river enhance phytoplankton production. The percentage of lithogenic material in total mass flux at the DWH site varied little (69 ± 7%; n = 56; Table 2), suggesting that lithogenic matter was incorporated at a constant fraction. This effect may be because fine sediments (< 63 µm) occur at a relatively constant concentration in the pool of suspended matter originating from the Mississippi outflow (Thorne et al., 2008). As a comparison, fluxes at the Seep and Reference sites, which are farther away from the Mississippi River Delta and are much more influenced by currents (see below), have a lower and more variable lithogenic fraction (60 ± 15% (n = 60) and 50 ± 23% (n = 46) of the total matter flux, respectively). Any POC associated with the lithogenic load could also be transported into the traps, but unlike lithogenic material, POC is reworked and respired during transit. As a result, proportionally less riverine POC will enter the trap than lithogenic matter.
Regarding nutrient transport by the Mississippi River, the links between Mississippi discharge and PP and particle flux at the DWH site appear to be strong. During the period 2010–2016, N discharge by the Mississippi peaked generally once a year in late summer (Figure 4). Satellite-derived PP at the DWH site peaked systematically 2–3 weeks after the peak in N discharge (Figure 4), strongly suggesting a direct link between the autumn bloom at the DWH site and Mississippi discharge. This link is in line with observations that phytoplankton growth in the Northern Gulf of Mexico is nutrient-limited (Lohrenz et al., 1997; Quigg et al., 2011).
The pattern of POC flux at the DWH site approximately matched PP (Figure 2a, d) and Mississippi N discharge (Figure 4), though there were some periods of high N discharge and low POC fluxes (most pronounced in spring 2013). The potential link between particle flux and river N discharge was further obscured by the recurrence of trap clogging. Our data suggest that the region around the DWH site experiences a winter bloom typical for the Gulf of Mexico (see Section 4.3) and an annual surface bloom, which is driven by the Mississippi N discharge and can be readily observed by satellites. The surface bloom typically lasts ~3 weeks (based on satellite-derived PP data) and likely leads to large export that clogs the traps. Because of the clogs in our traps, we do not know the magnitude of these bloom export events, but they are potentially higher than the fluxes we observed with our sediment traps, and could thus be in excess of 100 mg C m–2 d–1.
Overall, we propose that particle flux at the DWH site is strongly influenced by the Mississippi River discharge through two discharge processes. (1) The fine lithogenic material from the Mississippi River remains in suspension in the water and is advected with the currents to off-shore regions. When marine snow forms, it scavenges and incorporates this material, leading to a transport of non-CaCO3 lithogenic material to the sediment. (2) Discharge of nutrients (in particular nitrate and nitrite) and advection of these nutrients with the currents cause marine organic particle production by fertilizing phytoplankton growth and stimulating the food web. This stimulation of biological activity will promote the formation of marine snow and enhance particle fluxes.
The seasonal flux pattern at the Seep and Reference sites (Figure 2e, f) had no obvious relationship with PP (Figure 2b, c), in stark contrast to the DWH site, where fluxes appeared to be linked to PP. The observed PP climatology at the Seep and Reference sites exhibits the same pattern observed in the open Gulf of Mexico (Muller-Karger et al., 2015): PP is highest in winter and lowest in autumn (Figure 2b, c).
High winter PP likely occurs because the light regime in the Gulf of Mexico is sufficient for growth all year round, and the limiting factor for phytoplankton growth is nutrient supply. In winter, when the mixed layer is deepest, nutrient supply is high, allowing increased phytoplankton growth (Figure 2a–c). Around summer/autumn, when the mixed layer is shallow, nutrient supply is low resulting in reduced PP (Figure 2b, c; Müller-Karger et al., 1991, 2015). A similar pattern has been observed in the South China Sea, where light is not limiting and the combined effect of convective overturn and strong winds extend the mixed layer below the nutricline (Tseng, 2005).
The inverse pattern of PP and flux at the two offshore sites, however, is unusual. Recently, such a delay in sedimentation after a period of high PP has been suggested to be caused by high production of transparent exopolymer particles (TEP) in relation to other particles (Mari et al., 2017). TEP are positively buoyant particles (Azetsu-Scott and Passow, 2004), such that TEP-rich aggregates may not sink (Jennings et al., 2017; Mari et al., 2017). A sinking event of organic matter will be delayed and the organic matter will linger in the surface layer until the remineralization of TEP, thought to be more rapid on average than for POC, permits sinking. Alternatively, seasonal differences in sinking velocity and the associated attenuation of sinking organic matter derived from primary production may cause a mismatch between primary production and deep flux.
Another possibility is that the current regime advected particles from the productive coastal regions to the trap. Analysis of the current and wind data in the Northern Gulf of Mexico suggests a seasonality that directs water from the shelf region towards the Reference site primarily during autumn (Smith and Jacobs, 2005). Particle backtracking models also suggest that particles reaching the trap were sometimes transported laterally over 100 km and that particles arriving at the Reference site trap in September 2012 originated at times from filaments of low salinity waters that wrapped around a Loop Current eddy (Liu et al., 2017). This hypothesis is also supported by the observation that, in regions with strong off-shore currents, transport of suspended POC through lateral advection can be higher than vertical fluxes (Alonso-González et al., 2009). We conclude that the most likely explanation for the unusual relationship between flux and PP at the Seep and Reference sites is lateral advection; e.g., that during summer the currents transport particles from the more productive onshore regions towards the central Gulf of Mexico.
While the influence of the Mississippi on flux at > 1000 m depth is relatively constant and predictable at the DWH site, we find that it is more occasional and less predictable at the Seep and Reference sites. The currents in the Northern Gulf of Mexico are highly variable. They are under strong influence of the Loop Current, which is a dominant current feature in the Eastern Gulf of Mexico. The Loop Current regularly sheds an anticyclonic eddy approximately every 6–11 months (Sturges and Leben, 2000), which travels west towards the Mexico shelf, where it dissipates (Vidal et al., 1992). Particle transport in the Northern Gulf of Mexico can thus be variable. Nevertheless, a persistent westward transport of fine sediment particles from the Mississippi has been suggested based on modern seafloor sediments (Balsam and Beeson, 2003), indicating that the Seep and Reference sites might be directly influenced by lithogenic particles from the Mississippi. A model analysis of the two study sites shows that the Seep and Reference sites are positioned in the transit area of the Loop Current eddies, and the source area of particles reaching the traps can be, at times, very large (500–600 km; Liu et al., 2017). Depending on the currents, particles collected at the Seep and Reference sites may have a similar origin and stem from close to the traps (such as the case for particles reaching the trap at the Reference site in January 2013), or may follow very different trajectories and originate from across the Gulf, including regions as far south as 24°N or the shelf area (as the case for particles reaching the Seep site in September 2012; Liu et al., 2017).
Resuspension from below the traps was not an important contribution to flux, as current speeds at the depth of the traps were below 10 cm s–1 except during Hurricane Issac (Diercks et al., 2017). Resuspension from shelf slopes, on the other hand, may be a more important process: in 2008, a sediment trap deployed at 700 m depth 25 km to the southwest of the Seep site collected lithogenic matter fluxes of 21 ± 22 mg m–2 d–1 (n = 28; Richey et al., 2014). These fluxes were lower than those we observed at 1260 m depth during 2012–2016 (160 ± 94 mg m–2 d–1; Table 2), and indicate the advection of terrestrial material offshore via deep downslope transport (Richey and Tierney, 2016).
The traps at the Seep and Reference sites can thus have a large and diverse source capture area and, depending on the position of the eddies and the Loop Current, may collect particles originating not only from the shelf (where the Mississippi River water is usually present year-round) but also from the central Gulf of Mexico. The central Gulf of Mexico is much less productive than the shelf waters, explaining why the fluxes and the contribution of lithogenic matter to total flux at these sites were overall lower and more variable than those observed at the DWH site (Table 2). Nevertheless, riverine inputs are likely still an important source of particles at the Seep and Reference sites (Liu et al., 2017), especially during summer months when waters of riverine origin are more commonly found offshore (Schiller and Kourafalou, 2014).
Apart from the quantity and the seasonal flux pattern, varying hydrographic conditions combined with variations in particle sources (including local inputs) strongly affected particle quality. In this section, we evaluate how the quality of sinking hydrocarbons varied between sites and temporally at one site, depending on the source area and local conditions. We focus on fluxes at the Seep site, as this site is located in an active seep region and, depending on the currents, is periodically influenced by the Mississippi discharge. As a comparison we present data on hydrocarbon fluxes observed at the DWH site directly after the spill and two years later, in 2012. Based on the hydrocarbon composition and radiocarbon isotope analysis, four distinct periods at the Seep site could be distinguished, which highlights the complex particle dynamics at this site.
Two time intervals where crude-oil-derived PAHs entered the traps in significant amounts (period A1, Table 4) were clearly observed. During these periods, PAH composition was markedly different from the remaining periods and sites (Figures 5 and 6) and characterized by a high concentration of methylated PAHs and hopanes which are indicative of fresh crude oil. We suspect that this crude oil was derived from active seeps in the vicinity of the Seep site trap and was scavenged during its ascent by sinking marine snow. As seep activity fluctuates in time (Garcia-Pineda et al., 2010, 2014), seepage is temporally and spatially very heterogeneous. Heterogeneous seepage combined with strongly variable small scale currents (Diercks et al., 2017) likely cause irregular advection of hydrocarbon-enriched waters and explain the intermittent nature of these crude-oil flux periods.
PAHs during the A2 period had similar composition and scores on the Fl/(Fl+Py) index, but fewer of the PAHs were alkylated (Table 4) and the C0/(C0+C1) value was higher than during A1. Loss of alkyl groups can be used to identify weathering (Sauer et al., 1998), and C0/(C0+C1) ratios increase during early weathering processes (Yan et al., 2016). These two indicators therefore suggest that particle fluxes during period A2 likely contained crude oil that had undergone a higher degree of weathering than those during A1. Crude oil from natural seeps rises towards the surface, where photo-oxidation, evaporation and biodegradation transform the oil. Natural surface oil slicks are often observed at and around the Seep site (Garcia-Pineda et al., 2010). Incorporation into newly formed marine snow aggregates can then transport this weathered oil back to the seafloor. In addition, the relatively high concentration of phenanthrene (which is preferentially lost during weathering) and the overall composition (Figures 5 and 6) suggest that sinking particles during A2 contained a large fraction of PAH from combustion-derived sources similar to those found during period B.
Analysis of the samples during period B indicates that PAHs had pyrogenic sources, though they also carried a weak petrogenic signal (Table 4). The most important dispersion route of combustion-derived PAHs is the release into the atmosphere (Abdel-Shafy and Mansour, 2016), from where PAHs are transported with the wind until removed from the atmosphere by either dry (as dust) or wet (with rain) deposition. Combustion-derived PAHs can thus reach the marine environment either directly (aeolian deposition at sea) or indirectly via rivers and groundwater discharge (deposition at land and subsequent run off; Abdel-Shafy and Mansour, 2016).
Similarly, we also observed a high load of combustion-derived PAHs at the DWH site, which makes sense considering the vicinity of the coast, the strong influence from Mississippi discharge in this area, and the particularly high combustion emissions in the Baton Rouge area and generally across the Mississippi catchment area (Caiazzo et al., 2013). An important note is that the ΣPAHs observed at the DWH site in 2012 were likely mostly from combustion and that the concentration of ΣPAHs in the flux material and overall ΣPAHs fluxes were lower (0.27 ± 0.04 µg ΣPAH g–1 and 0.11 ± 0.02 mg m–2 d–1, n = 4) compared to the fluxes throughout the year after the DWH spill (0.40 ± 0.10 µg ΣPAH g–1 and 0.22 ± 0.12 mg m–2 d–1 (n = 19) during August 2010–October 2011; Yan et al., 2016). However, isotope data also suggest that petrocarbon from the spill was still part of the sinking flux (Chanton et al., 2017).
At the Seep site, an interesting observation was revealed by the isotopic composition of the fluxes. Based on flux composition (both PAHs and biogeochemical composition), fluxes at the Seep site were indistinguishable during periods C and D (Table 4). Yet, the isotopic composition shows that the age of carbon in the organic matter during period C was much older. This finding seems contradictory at first, as ‘old carbon age’ is associated with crude oil. However, isotopes measure fossil carbon regardless of its current chemical state. When petrocarbon is incorporated into the marine food web (Chanton et al., 2012, 2015), the chemical composition of the organic carbon changes but the isotopic signature is retained. In other words, the carbon might not look like the original source (e.g., crude oil) anymore. We thus believe that during this period, released crude oil was biodegraded and taken up by the planktonic food web in sufficient amounts to alter the bulk isotopic composition. Subsequent organic matter production and sedimentation thus carried the age signal of the seepage.
Overall, our time series at Seep site illustrates comprehensively the different pathways that naturally released crude oil can take. Released crude oil may never reach the sea surface, instead being scavenged by sinking particles and returned to the benthos, or it may reach the surface where it undergoes weathering before being scavenged into marine snow and sinking, retaining most of its original signal (periods A1 and A2). Or it may enter the food web and sink in a completely different form, e.g., as detritus (period C). Small seepage, strong weathering and mixing with pyrogenic sources may obscure the presence of crude oil from seeps either by diluting or altering the composition (period B).
The high variability of hydrocarbon composition at the different sites and over time (particularly at the Seep site) clearly highlights the dynamic nature of the Northern Gulf of Mexico system. The hydrocarbon composition illustrates that the quality of particle flux is strongly influenced by transport processes like currents and winds, as well as by particle sources like natural seeps, primary production, and riverine material. Our data show that the quality of sinking particles can vary dramatically over short spatial and temporal scales, even if the main components of flux (POC, PON, bSiO2 and lithogenic matter) are relatively constant.
One of the problems in the aftermath of the DWH oil spill was the lack of a baseline for the Gulf of Mexico ecosystem. Sediment core analysis shows that large amounts of oil were deposited on the seafloor (Larson et al., 2013; Valentine et al., 2014; Brooks et al., 2015; Chanton et al., 2015). High fluxes of PAHs associated with crude oil were also found in sediment trap samples collected during August–November 2010 just after the well was sealed (15 July 2010; Yan et al., 2016). POC flux of the first of these samples was also 2–3 times higher than fluxes observed the 2 years afterwards, which leads to the suggestion that oil and black carbon promoted aggregation and more effective sedimentation. Whether the crude oil that was transported to the seafloor in September 2010 was carried by unusually high export fluxes or whether baseline export fluxes effectively collected large amounts of oil during aggregation and sinking through the water column is not clear. Unfortunately, no sediment traps in the near vicinity of DWH were deployed during the oil spill, so no direct measurement of total mass flux during the spill is available. However, our long-term time series of trap deployments at the DWH site gives us a good idea of the interannual variability and the drivers of particle flux in the Northern Gulf of Mexico.
Our data suggest that annual peak fluxes are often in excess of 100 mg C m–2 d–1. This excess, in turn, means that the magnitude of the high flux event in September 2010 (109 mg C m–2 d–1; Yan et al., 2016) was not unusual, but potentially typical for this site after N discharge. Peak N fluxes vary from year to year, but 2010 was similar to the years 2011, 2014 and 2015. In 2012, a drought caused unusually low N discharge (Figure 4; Van Metre et al., 2016), which explains why we did not observe high fluxes in 2012, and why Yan et al. (2016) deduced that the September 2010 flux was unusually high. This example illustrates how critical long-term monitoring is to fully understand export mechanisms and flux drivers.
Yet, the flux composition at the DWH site was different in September 2010 compared to the rest of our time series, suggesting that the export mechanism may have been different to other periods. The high accumulation rates of settled material on the seafloor also suggest that the annual sedimentation rate was elevated in 2010 compared to other years. Fluxes during September 2010 were very high in terms of bSiO2 (400 mg bSiO2 m–2 d–1 and 25% of total matter flux; Yan et al., 2016) and contained much less lithogenic matter (46% instead of the typical 70 ± 8%). These findings are in line with the observation that the high flux in September 2010 contained a high number of diatoms. There are two obvious explanations for the atypical flux composition: (1) the September 2010 flux contained additional C from sources atypical for the DWH site and related to the oil spill, or (2) the September 2010 flux was the tail end of several large sedimentation events which had collected and exported most suspended lithogenic matter from the water column.
One possibility is that additional POC was exported after the DWH oil spill that was atypical for the DWH site. The diatom aggregates in September 2010 could have collected the large aggregates that were observed in the water column (Daly et al., 2016) and formed as a response to the oil and dispersant (Passow et al., 2012; Joye et al., 2014). This trap contained a high proportion of oil-spill related carbon: e.g., black carbon made up 8% of the POC flux (Yan et al., 2016).
More likely, however, is our second hypothesis. During the DWH oil spill, several large flux events were observed that carried a significant fraction of the spilled oil and in situ burning residues to depth. The first of these events was likely caused by dead planktonic organisms (Passow et al., 2012) that were blooming during this time (Figure 4). Later, marine snow formation was likely caused by oil-degrading bacteria (Passow et al., 2012; Joye et al., 2014; Valentine et al., 2014; Chanton et al., 2015), eventually followed by the phytoplankton-driven export events such as the one observed in September 2010 (Yan et al., 2016). During this series of export events, marine snow formation may have incorporated most of the suspended lithogenic matter. If the resupply rate of suspended sediment matter by lateral advection and aeolian input was slower than incorporation into marine snow and subsequent export, aggregates formed in September 2010 would have incorporated much less lithogenic matter than usual. As a result, the POC-to-lithogenic matter ratio would be higher than during the other export events, which was indeed the case (10% in September 2010 compared to 5 ± 1% in the following 12 months). Modeling work based on coagulation theory, in which aggregation and sinking of a diatom bloom are simulated, suggests that the September 2010 trap collected the tail end of a large export event that happened shortly before the sampling period (Francis & Passow, pers. communication). Overall, we conclude that the magnitude of the total flux in September 2010 was not unusual, but that the composition differed with a clear petrocarbon signal.
Sedimentation dynamics in the Northern Gulf of Mexico are complex. Aggregation and export are enhanced in regions influenced by the Mississippi River, as its nitrogen discharge allows high phytoplankton growth in the otherwise nutrient-limited Northern Gulf of Mexico. We observed such tight coupling at the DWH site, where seasonality and quantity of flux reflected Mississippi discharge and subsequent primary production. A surface bloom, which was observed annually following the peak discharge in nitrogen, likely caused export events.
At our two offshore sites, fluxes did not reflect primary production and did not show a clear seasonality. The particle source regions for these sites were large and diverse, owing to strong currents and mesoscale circulation (Loop Current and numerous eddies). At these sites, low salinity, nitrogen-rich riverine waters and marine snow aggregates are at times carried for hundreds of kilometers before reaching the bathypelagic and/or seafloor (Liu et al., 2017). Sites in less productive regions, such as our two offshore sites, may thus be episodically exposed to high organic matter fluxes that are similar in magnitude and composition to fluxes at more coastal regions.
At all sites, total mass flux at ~1400 m depth predominantly consisted of lithogenic material (50–70%), which likely originated from the Mississippi plume. Organic matter, CaCO3 and bSiO2 made up the remainder with approximately equal contributions. The relative composition of inorganic material in the three traps reflects the respective composition in sediments below the traps (Balsam and Beeson, 2003).
Depending on the location and the state of the currents, marine snow also carried varying amounts and compositions of PAHs to depth. Our data show that the DWH site carried a relatively high load of petrogenic PAHs (compared to our Reference site), likely owing to its close vicinity to the shore and the strong influence by the Mississippi River plume. Comparison of our time series with the sediment trap samples collected during the year following the DWH oil spill (August 2010–October 2011; Yan et al., 2016) suggests that the particle fluxes had not recovered to baseline levels by October 2011 (Chanton et al., 2017).
In the vicinity of natural seeps, PAH fluxes tended to be higher than at our Reference site but lower and of different origin than at the DWH site. We also observed indications of three different pathways for “natural” oiled-snow sedimentation. First, fluxes at times contained a strong oil signal, which was likely caused by natural seepage that was incorporated into sinking aggregates; however, such events were episodic, highlighting the heterogeneity of seepage and currents. Second, combustion products dominated at other times, possibly introduced by advection from coastal areas. Last, PAH fluxes were similar to the Reference site, but isotopic composition suggested that the sinking carbon originated from oil seepage that had entered the food web and was converted to organic matter, hence losing the chemical oil signature but retaining the isotopic composition.
Data are publicly available through the Gulf of Mexico Research Initiative Information & Data Cooperative (GRIIDC) at https://data.gulfresearchinitiative.org.
The supplemental files for this article can be found as follows:
We thank the captain and crew of the RV Oceanus for help with the deployment of the sediment traps. We also thank Prof Jody Deming for valuable editing.
This research was made possible by a grant from The Gulf of Mexico Research Initiative to support the “Ecosystem Impacts of Oil and Gas in the Gulf” (ECOGIG) research consortium. This is ECOGIG contribution number 486.
The authors have no competing interests to declare.
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