A- A+
Alt. Display

# Sources of carbon to suspended particulate organic matter in the northern Gulf of Mexico

Ph.D

## Abstract

Suspended particulate organic carbon (POCsusp) in the Gulf of Mexico is unique compared to other seas and oceans. In addition to surface primary production, isotopic analysis indicates that microbial cycling of oil and riverine inputs are primary sources of carbon to POCsusp in the Gulf. To characterize POCsusp from seep sites and non-seep north central Gulf (NCG) sites potentially affected by the Deepwater Horizon (DWH) spill, we analyzed 277 and 123 samples for δ13C and Δ14C signatures, respectively. Depth, partitioned into euphotic (<300 m) and deep (>300 m), was the main driver of spatial δ13C differences, with deep depths exhibiting 13C depletion. Both deep depths and proximity to sources of natural seepage resulted in 14C depletion. A two-endmember mixing model based on Δ14C indicated that sources to POCsusp were 14–29% fossil carbon at NCG sites and 19–57% at seep sites, with the balance being modern surface production. A six-component Bayesian mixing model MixSIAR, using both 13C and 14C, suggested that riverine inputs were an important carbon source to POCsusp contributing 34–46%. The influence of seeps was localized. Below the euphotic zone at seep sites, 46 ± 5% (n = 9) of the carbon in POCsusp was derived from environmentally degraded, transformed oil; away from seeps, transformed oil contributed 15 ± 4% (n = 39). We hypothesized that, at NCG sites removed from hydrocarbon seep sources, isotopic signatures would be depleted following the spill and then shift towards background-like enriched values over time. At deep depths we observed decreasing Δ14C signatures in POCsusp from 2010 to 2012, followed by isotopic enrichment from 2012 to 2014 and a subsequent recovery rate of 159‰ per year, consistent with this hypothesis and with biodegraded material from DWH hydrocarbons contributing to POCsusp.

##### Knowledge Domain: Ocean Science
How to Cite: Rogers, K.L., Bosman, S.H., Weber, S., Magen, C., Montoya, J.P. and Chanton, J.P., 2019. Sources of carbon to suspended particulate organic matter in the northern Gulf of Mexico. Elem Sci Anth, 7(1), p.51. DOI: http://doi.org/10.1525/elementa.389
Published on 19 Dec 2019
Accepted on 11 Nov 2019            Submitted on 19 Sep 2019
Domain Editor-in-Chief: Jody W. Deming; School of Oceanography, University of Washington, US
Associate Editor: Lisa A. Miller; Institute of Ocean Sciences, Fisheries and Oceans Canada, CA

## Introduction

The introduction of fossil hydrocarbon-derived material, whether by anthropogenic inputs or natural seepage, provides a unique source of carbon source to the sea. In most areas of the Atlantic and Pacific oceans, surface primary production is the main carbon source to the deep ocean. Typically, only about 1% of the carbon fixed at the surface reaches the deep seafloor. Along the way, most of the organic matter is consumed and degraded, exchanging between the different carbon pools in the water column — dissolved inorganic carbon (DIC), dissolved organic carbon (DOC), and sinking and suspended particulate organic carbon (POCsink, POCsusp), before the residual amount finally reaches the seafloor.

Of these pools, POCsusp is uniquely capable of providing insights into the sources of carbon to the water column and those fueling the microbial loop. The small particle size and relatively short residence time that characterize POCsusp make it more sensitive than other carbon pools to recording variations in inputs. The different carbon pools can be defined operationally by size. The smallest end of this size continuum is DOC, which we define as organic carbon that passes through a filter of 0.7-µm pore size. POCsusp is any organic matter collected on the 0.7-µm filter, while POCsink is comprised of those particles typically larger than 50 µm (Deuser, 1986). Due to the small difference in size, DOC and POCsusp are more similar to each other chemically than to POCsink (Druffel et al., 1996). As DOC is partially controlled by microbial processes, the DOC-POCsusp connection provides a link between microbial processes and the larger particles that can move carbon up the food chain (Chanton et al., 2012; Cherrier et al., 2014). Linkage with the microbial loop has also been observed in the microbial uptake of dissolved inorganic nitrogen and possible methanodiazotrophy through δ15N isotope analysis (Montoya et al., 1990; Fernandez et al., 2016).

The residence times of DOC, POCsink, and POCsusp range widely, resulting in different degrees of sensitivity of each carbon pool to different inputs. DOC is the second largest carbon reservoir in the ocean, amounting to about 650 Pg of mostly recalcitrant carbon, with a residence time of 1000–6000 years (Williams and Druffel, 1987). The concentrations of POCsusp and POCsink in the water are much lower than DOC, but the flux of POCsink through the water column is much greater than POCsusp, with a residence time of about a month (Deuser, 1986). POCsink is determined primarily by surface phytoplankton production (Chanton et al., 2018), which draws on the DIC pool, the largest carbon reservoir in the ocean at 38,000 Pg (Hansell and Carlson, 2014). POCsusp floats in the water for 5–10 years (Bacon and Anderson, 1982). Its low concentrations in the open ocean, typically from less than 10 µM C in surface waters to about 1 µM C at depths below 500 m (McNichol and Aluwihare, 2007), and short residence times increase the sensitivity of this pool to other carbon sources, although the DOC and POCsink pools have also been observed to reflect variations in carbon input associated with the Gulf of Mexico (GOM) Deepwater Horizon (DWH) spill (Yan et al., 2016; Walker et al., 2017; Chanton et al., 2018; Geiring et al., 2018).

Studies in the late 1980s and early 1990s used stable and radiocarbon isotope analysis of POC to determine sources of oceanic particulates. Druffel et al. (1992, 1996, 2003) analyzed stable and radiocarbon isotopes of particulates from the Sargasso Sea and central North Pacific which indicated that POCsink and POCsusp are derived primarily from surface phytoplankton production. POCsusp is enriched in radiocarbon from being formed at the surface and becomes more depleted with depth. In the GOM, δ13C values for surface production range from –20 to –22‰ (Chanton and Lewis, 2002), and, at the time of the oil spill, Δ14C values for surface production ranged from 39 to 41‰ (Chanton et al., 2012, 2018).

In marginal seas, the sources of POCsusp can vary. Bauer et al. (2002) found highly depleted δ13C and Δ14C values for POCsusp at depth along the Mid-Atlantic Bight (MAB). The radiocarbon depletion near the seafloor of POCsusp has been attributed to resuspension of old sediment or organic matter and adsorption of DOC onto POCsusp (Druffel et al., 1992, 1996, 2003; Bauer and Druffel, 1998; Bauer et al., 2002). Flocculating particles due to heterotrophic activity could also play a role in depleting PO14Csusp (Druffel et al., 1992). Bauer et al. (2002) suggested that deep shelf PO14C from the MAB could be caused by natural hydrocarbon seepage; however, at the time of collection there was no evidence of such seepage, leading Bauer et al. (2002) to conclude that the depletion was due most likely to resuspended sediment. The similar correlation of δ13C and Δ14C observed between particulates from the MAB (Bauer et al., 2002) and the Desoto Canyon of the Gulf of Mexico (Figure 1) (Cherrier et al., 2014) suggests similar sources of carbon. In 2014, Skarke et al. (2014) reported the discovery of a major hydrocarbon seep field in the same area of the MAB that Bauer et al. (2002) had sampled. The hydrocarbons from this seep field could well be the cause of the correlation between the depleted δ13C and Δ14C of POC from the MAB (Figure 1).

Figure 1

δ13C and Δ14C signatures of POCsusp and DIC in the ocean. Data for POCsusp from Pacific Station M (bold dashes; Druffel et al., 1996) showed no trend, indicating a single source, surface primary production, to the POCsusp. The covariation in δ13C and Δ14C for POCsusp from the Mid-Atlantic Bight (MAB, open squares; Bauer et al., 2001, 2002) and Desoto Canyon in the Gulf of Mexico (solid triangles; Cherrier et al., 2014) indicates the incorporation of another carbon source. Data for DIC from MAB are from Bauer et al. (2001). For data fit to linear regression analysis for Desoto Canyon 2010–2011: y = 49.137x + 1277.5, r = 0.929, n = 18, p < 0.0001; for MAB 2002: y = 47.708x + 1081.4, r = 0.845, n = 106, p < 0.0001. DOI: https://doi.org/10.1525/elementa.389.f1

In April of 2010, the DWH Blowout released 717–789 million liters (4.5–4.9 million barrels) of oil and 500,000 t of gaseous hydrocarbons into the northern central Gulf of Mexico (Lehr et al., 2010; Joye et al., 2011). An estimated 30% of the released hydrocarbons formed a deep-water hydrocarbon plume between 1000-m and 1200-m depths (Valentine et al., 2010; Ryerson et al., 2012). The bulk of the gaseous hydrocarbons were primarily methane (Joye et al., 2011), but less than 0.01% of the gases reached the surface (Kessler et al., 2011; Yvon-Lewis et al., 2011). Crespo-Medina et al. (2014) measured methane oxidation rates in the water column following the DWH event. At the depth of the deep-water hydrocarbon plume, concentrations of methane and the gene methane monooxygenase (pmoA) were elevated, as were methane-oxidation rates. Cherrier et al. (2014) presented evidence that this DWH-derived CH4 was found in the POCsusp of the Gulf in 2011–2012 (Figure 1). Assimilation of methane by methanotrophs has been found to be very efficient in other systems, e.g., converting 63–85% of methane into biomass at landfill sites (Börjesson et al., 1998, 2001). Du and Kessler (2012) estimated, using theoretical calculations of oxygen usage from the dissolved oxygen anomaly present in the deep-water hydrocarbon plume, that hydrocarbon degradation generated 0.36 ± 0.11 mg biomass per mg hydrocarbon. They also estimated that 0.10 ± 0.11 Tg of hydrocarbons, primarily methane, were converted into microbial biomass within the deep-water hydrocarbon plume. This biomass, including after cell senescence and viral lysis, would be an input to the POCsusp pool.

Methane can also be generated microbially in the oceanic water column under aerobic conditions (Karl et al., 2008). This process occurs in the Gulf of Mexico (Rakowski et al., 2015), as evidenced by CH4 concentrations and relative microbial abundances co-varying significantly from the seafloor to the euphotic zone. Thus, our characterization of the sources contributing to POCsusp included characterizing the isotopic composition of biogenically produced methane.

Several studies following the DWH event analyzed POC and plankton in the GOM, finding depleted δ13C and Δ14C signatures (Graham et al., 2010; Chanton et al., 2012; Cherrier et al., 2014). Chanton et al. (2012) and Cherrier et al. (2014) found a linear relationship between δ13C and Δ14C signatures, from modern photosynthetic production to a hydrocarbon endmember, with both the plankton and POC falling along the line, indicating the incorporation of material originally sourced from hydrocarbons, as well as the movement of this material up the food web (Wilson et al., 2016).

The purpose of this study was to characterize δ13C and Δ14C signatures of POCsusp in the GOM following the oil spill and as the system recovered from it, determining a new post-spill baseline for δ13C and Δ14C signatures of POCsusp in the GOM in the process. (For parallel work on POCsink, see Chanton et al., 2018.) In the Atlantic and Pacific Ocean basins, the baseline derives from a single dominant source, modern photosynthetic production. No other carbon source contributes more depleted 13C or 14C to the pool of POCsusp, so that co-variation between the isotopes (as in Figure 1) is not observed. In the GOM, however, the presence of two distinct carbon sources, one associated at times with anthropogenic activity, drives the depletion of both δ13C and Δ14C of POC, resulting in the co-variations depicted in Figure 1. The continuous input of hydrocarbon-derived material, petrocarbon, from natural seeps could also cause baseline signatures of the GOM to be more depleted than those from the Atlantic or Pacific oceans where input of hydrocarbon-derived material is quantitatively unimportant.

In this study we pursued three goals. First, we tested the hypothesis that, at sites with one-time (DWH) inputs of petrocarbon derived from methane and oil, initial depletion of the carbon isotopic signatures of POCsusp would be followed by recovery, shifting the depleted values observed by Cherrier et al. (2014) towards more enriched baseline-like signatures. Assessing baseline signatures of POCsusp in the Gulf prior to the DWH spill in 2010 has been difficult, as no PO14C data were collected in the GOM prior to that time. Second, we addressed the question, to what extent are the carbon isotopic values of POCsusp in the GOM affected by the seep sites that provide a continuous source of hydrocarbon-derived material to the Gulf as opposed to the one-time input from the DWH? Third, we aimed to determine the relative importance of modern surface marine production and riverine inputs to the different carbon sources in the Gulf, as reflected in POCsusp. In this study, we analyzed the stable carbon and radiocarbon isotopes of POCsusp collected from across the northern GOM to determine the carbon sources to these particulates. For sources we considered surface marine primary production, riverine input, sediment, two sources of biodegraded methane, and biodegraded oil.

## Material and Methods

### Sampling and sample preparation

POCsusp samples were collected during fourteen cruises over six years from 2010 to 2017 (except 2011), from a total of 43 separate sites across the northern Gulf of Mexico (Figure 2). At the time of collection, sites were classified as seep or non-seep, with seep samples collected directly over areas of seafloor seepage, while non-seep samples (designated north central Gulf, NCG) were collected in areas not directly influenced by natural seepage. These determinations were based on map data from MacDonald et al. (2015) and shipboard acoustics used to detect hard bottoms or bubbly streams indicative of a seep site. Over the course of sampling we collected particles from 13 seep and 30 NCG sites.

Figure 2

POCsusp collection stations in the north central Gulf of Mexico during 2010–2017. The Deepwater Horizon (DWH) site is indicated by a white X in the upper right of the main map and emphasized by a red arrow. North central Gulf (NCG) sites are indicated by green triangles; seep stations, by black circles; western GOM (WGOM) sites, by purple triangles. Data from Cherrier et al. (2014) in the Desoto Canyon are indicated by orange triangles. Sampling sites for biogenic methane in the water column are indicated by pink triangles. The inset map shows an enlarged view of the DWH site (black X) and surrounding sampling sites. The southern biogenic methane sampling site (pink triangle) was approximately 5,900 m east of a seep site. DOI: https://doi.org/10.1525/elementa.389.f2

Water column samples were collected by CTD-Rosette, filtering 1–20 L of water through pre-combusted 47-µm 0.7 GF/F borosilicate filters in plastic housings under gentle pressure filtration (5–10 psi). Filters were stored frozen in combusted aluminum foil and brought back to the lab for acidification in a filter housing unit with dilute (1N) HCl (Fernández-Carrera et al. 2016). Stable carbon isotope ratios of POCsusp were analyzed on subsections of the filters using a Carlo-Erba elemental analyzer connected to a Finnegan MAT delta Plus XP Stable Isotope Ratio Mass Spectrometer (EA-IRMS) at the National High Magnetic Field Laboratory. The results were converted into δ13C with respect to VPDB (Vienna Pee Dee Belemnite). Samples analyzed after 2014 had a small split, about 10% of the total sample, of CO2 removed prior to graphitization to be analyzed for δ13C. After δ13C analysis, the remaining filter was combusted, and the resultant CO2 was purified cryogenically using the methods of Peterson et al. (1994). The purified CO2 was flame-sealed in a 6-mm ampule and sent to Woods Hole National Ocean Sciences Accelerator Mass Spectrometry (NOSAMS), University of Georgia Center for Applied Isotope Studies (UGA) or Lawrence Livermore National Laboratory Center for Acceleration Mass Spectrometry (LLNL CAMS) for analysis of natural abundance of radiocarbon. The radiocarbon signatures are reported in the Δ14C notation as described in Stuiver and Pollach (1977). The blank correction as described in Fernández-Carrera et al. (2016) was applied to both δ13C and Δ14C values. Forty coal samples, representing fossil 14C dead carbon, were run to access our procedural blank over the course of this study. The average Δ14C value was –995 ± 7‰. We also ran 25 azalea leaf standards collected in Tallahassee, Florida, in 2013. The average Δ14C value was 31 ± 8‰. There was no variation between AMS labs in these samples or the coal blanks.

To estimate the DOC blank adsorbed onto the filters, we attached a second GF/F filter below the filter collecting the POCsusp. The top filter would collect the POC, leaving the second filter to adsorb only DOC (if that were occurring). From this process, we estimated the DOC blank on the filters to be 0.12 µmoles CO2, representing 0.3 to 2% of the amount of carbon on the filters.

For water-column CH4 and its δ13C isotopic composition, water samples were collected by CTD-Rosette and dispersed to glass bottles in June and July of 2013 at two sites in the northern GOM at 28.669°N; 88.3584°W, and at 28.32554°N and 88.3865°W (Figure 2). Methane concentrations were determined by the methods detailed in Magen et al. (2014). The stable isotopic composition of water-column methane was determined from 4-L bottles preserved with KOH as described in Magen et al. (2014). A headspace was introduced into the bottles and flushed into cryogenic trapping system, cryo-focused and run on a Thermo Finnegan Delta V Isotope Ratio Mass Spectrometer at Florida State University. The results were converted into δ13C with respect to VPDB (Vienna Pee Dee Belemnite).

### Temporal trends in non-seep site data

The weighted average of the NCG POCsusp per collection year for both Δ14C and δ13C was calculated to estimate the inventory of carbon and their isotopic signatures in the water column. The weighted average of radiocarbon was calculated by multiplying the total µmoles CO2 sent for radiocarbon analysis for each year by the individual sample size of µmoles CO2. This proportion was then multiplied by the Δ14C for each sample and summed for the overall weighted average for that year. For the δ13C samples, the value for mg C per subsample used for δ13C analysis was calculated from the regression of the %C and δ13C of known standards. This value was extrapolated to the whole filter, assuming the sample was spread evenly. The value for total mg C for each sample was converted to µmoles and then summed following the radiocarbon method above.

### Mixing models

A two-endmember mixing model based on Δ14C was used to estimate the percent carbon incorporated from photosynthesis and from all petrocarbon sources, combining methane and oil. The following equation was used to determine the percent carbon from modern surface production, with the denominator equaling the total range of radiocarbon from 39‰ (for marine production; Chanton et al., 2018) to –1000‰:

${%}_{\text{modern}}=\left(\left[1000+{\Delta }^{14}{\text{C}}_{\text{POC}}\right]/1039\right)*100$

The percent from hydrocarbons is 100 – %modern. We completed a sensitivity test for the two-endmember model by adjusting the total range of Δ14C by the standard deviation of the modern endmember. The Δ14C of the modern endmember was the average GOM plankton value from Chanton et al. (2018), 39 ± 26‰ (n = 79).

In addition to the two-endmember mixing model we also employed the Bayesian mixing model MixSIAR Version 3.1 (Stock and Semmens, 2016) to determine the contribution from other potential sources of organic carbon in the GOM. This R version uses probabilities from a Bayesian method to estimate the percent contribution from multiple sources. Using Δ14C and δ13C as our tracers, we assumed no fractionation between the sources and the isotopic signatures of the POC. We report the contribution of each source at the mean, including the standard deviation, resulting after 3 × 106 iterations. Our model was run nesting depth within site type, including the residual * process errors with uninformative priors. Our carbon sources included (mean ± standard deviation [S.D.] for Δ14C and δ13C, respectively) surface productivity (38.8 ± 25.8‰, and –21 ± 2‰; Chanton et al., 2012, 2018), riverine organic carbon (–154 ± 68‰ and –26 ± 1‰; Cai et al., 2015), sedimentary organic carbon (–200 ± 29‰, and –22 ± 1‰; Chanton et al., 2015), biogenic methane in the water column (38.8 ± 25.8‰, n = 79, and –41 ± 1‰, n = 19; this study), as well as DWH methane (Δ14C = –1000‰ and δ13C = –57.4‰; Crespo-Medina et al., 2014) and Macondo oil (Δ14C = –1000‰ and –27‰; Graham et al., 2010).

### Statistics

Statistics were performed using R 3.1.3 R Core Team (2015). The data were not normally distributed, as indicated by the results of Levene’s test. Therefore, the non-parametric Mann-Whitney U Test was used to compare the different groups for both δ13C and Δ14C. We continued the designation of seep versus NCG (non-seep, north-central Gulf) and divided our samples further into two depth categories (euphotic <300 m and deep water >300 m). The four categories we examined were as follows: seep euphotic, seep deep, NCG euphotic, and NCG deep. We used the adjusted p-value of 0.008 to indicate significance, accounting for the multiple comparisons (α = 0.05, 6 comparisons). From the z value we calculated the effect size:

$r=\frac{z}{\sqrt{N}}$

where r is the effect size, z is the z score, and N is the sample size.

## Results

Overall, we collected 277 POCsusp samples in the GOM. The δ13C signatures (n = 277), and Δ14C values (n = 123) are summarized in Table 1. POCsusp from the NCG euphotic zone (<300 m) had δ13C signatures ranging from –17.8 to –35.4‰ (n = 108), with Δ14C signatures from 54 to –515‰ (n = 55). Deep-water particles (>300 m) from the NCG had δ13C signatures ranging from –20.6 to –35.2‰ (n = 65), with Δ14C signatures from –48 to –603‰ (n = 39). Seep euphotic POCsusp had δ13C signatures ranging from –19.3 to –28.8‰ (n = 62), with Δ14C signatures from 71 to –468‰ (n = 14). Deep-water suspended particles from seep sites had δ13C signatures ranging from –21.4 to –34.3‰ (n = 33), with Δ14C signatures from –263 to –756‰ (n = 9). POCsusp collected from the euphotic zone in the western GOM (WGOM, west of 94° longitude) had δ13C signatures ranging from –22.8 to –29.2‰ (n = 8), with Δ14C signatures from 51 to –204‰ (n = 7). All data are provided in Table S1.

Table 1

Summary statistics for blank-corrected δ13C and Δ14C signatures of POCsusp from all study sites during 2010–2017. DOI: https://doi.org/10.1525/elementa.389.t1

Locationa Depthb δ13C Δ14C

Range (‰) Mean ± S.D. (‰) n Range (‰) Mean ± S.D. (‰) n

Overall Euphotic –17.8 to –35.4 –24.3 ± 2.8 178 71 to –515 –96 ± 144 76
Deep –20.6 to –35.2 –27.1 ± 2.9 98 –48 to –756 –314 ± 197 48
NCG Euphotic –17.8 to –35.4 –24.1 ± 3.0 108 54 to –515 –98 ± 143 55
Deep –20.6 to –35.2 –27.1 ± 3.0 65 –48 to –603 –258 ± 162 39
Seep Euphotic –19.3 to –28.8 –24.4 ± 2.5 62 71 to –468 –128 ± 164 14
Deep –21.4 to –34.3 –27.1 ± 2.6 33 –263 to –756 –558 ± 139 9
WGOM Euphotic –22.8 to –29.2 –25.2 ± 2.1 8 51 to –204 –16 ± 85 7

a North central Gulf (NCG) samples were collected away from distinct areas of seepage; seep samples, over seep areas; western Gulf of Mexico (WGOM) samples, at the surface west of 94° longitude.

b Euphotic samples were collected above 300 m; deep samples, below 300 m.

The δ13C and Δ14C signatures for all POCsusp samples, across all collection depths and sampling years, were highly variable, as seen in Figure 3 where the δ13C and Δ14C signatures of NCG POCsusp are color-coded by year. Suspended particles from seep sites were not color-coded by year, as the majority of the samples were collected in 2013. We observed two trends of δ13C and Δ14C co-variation in the POCsusp data (Figure 4). One trend, the lower limb, indicated co-variation based on blending of modern surface production and petrocarbon input, observed for both NCG and seep sites. The upper limb, observed primarily for NCG sites, reflected the addition of another carbon source to modern production, with depleted δ13C but more enriched Δ14C signatures, possibly associated with the biodegradation of biogenic methane produced in the water column (Rakowski et al., 2015). In this study, we used two different mixing models to characterize both the co-variation based on petrocarbon input and the variation based on all of the sources that could contribute to GOM POCsusp.

Figure 3

δ13C and Δ14C by depth for POCsusp collected in the GOM during 2010–2017. δ13C (upper) and Δ14C (lower) signatures of POCsusp by depth, color coded by collection year: orange for 2010; aqua, 2012; purple, 2013; green, 2014; red, 2015; blue, 2016; and black, 2017. Seep samples from all years are shown as open circles. Western Gulf of Mexico (WGOM) samples from 2016 (west of 94° longitude) are shown as plus symbols. DOI: https://doi.org/10.1525/elementa.389.f3

Figure 4

δ13C vs Δ14C of POCsusp collected in the GOM during 2010–2017. Sites classified as: NCG (non-seep; diamonds), seep (open circles), and western GOM (WGOM, plus signs). Stars show main potential carbon sources to GOM POCsusp, including surface production (green), biogenic methane (orange), riverine input (purple), sediment (gray), fossil methane (red), and oil (black). DOI: https://doi.org/10.1525/elementa.389.f4

Study-wide concentrations of POCsusp followed an expected gradient with highest concentrations at the surface decreasing with depth (Figure 5). Concentrations in the euphotic zone (<300 m) ranged from 0.32 to 62.5 µM (mean ± S.D.: 4.71 ± 9.38, n = 78). The four highest concentrations at the surface came from non-seep sites that were heavily influenced by riverine input. Concentrations of POCsusp in deep water (>300 m) ranged from 0.16 to 12.02 µM C (mean ± S.D.: 1.44 ± 2, n = 72).

Figure 5

Carbon concentrations (µM) by depth for POCsusp collected in the GOM during 2010–2017. Data are from all stations sampled in this study (Figure 2). DOI: https://doi.org/10.1525/elementa.389.f5

## Temporal trends in carbon isotopes in POCsusp

We tested the hypothesis that δ13C and Δ14C of POCsusp in the north central Gulf at non-seep sites would vary temporally, becoming increasingly enriched in heavy isotopes following their depletion associated with the 2010 injection of fossil hydrocarbons into the water column from the DWH oil spill (Cherrier et al., 2014; Fernandez et al., 2016; Weber et al., 2016). We calculated the weighted averages of the non-seep NCG particles collected each year to create an inventory that accounts for the quantity of organic carbon contributing to the δ13C and Δ14C signatures (Table 2). Data from Cherrier et al. (2014) were included in 2011 and 2012. Data were separated by depth, into NCG euphotic and deep water (Figure 6). The δ13C and Δ14C of euphotic POCsusp and δ13C of deep-water POCsusp (Figure 6A–C) exhibited depletion from 2010 to 2011. Afterwards the signatures increased in 2012, before decreasing again until 2014 and then increasing again and stabilizing by 2015. The Δ14C of deep-water particles (Figure 6D) showed the clearest indication of fossil carbon incorporation, over a longer time period from 2010 to 2012 with recovery from 2012 to 2014, stabilizing in the following years (2015–2017) at around Δ14C = –160‰. During the recovery period of 2012–2014, the linear regression calculated between these two years suggested a recovery rate (in ‰ per year towards more 14C enriched values) of 159‰ (Figure 6D).

Table 2

Weighted averages for δ13C and Δ14C signatures of POCsusp from NCG sites during 2010–2017. DOI: https://doi.org/10.1525/elementa.389.t2

Year Euphotic POCsusp Deep POCsusp

POCsusp (µM) Wt.Avg Δ14C (‰) Wt.Avg δ13C (‰) POCsusp (µM) Wt.Avg Δ14C (‰) Wt.Avg δ13C (‰)

2010 26.2 –18 –22.2 20.7 –291 –25.9
2011 61.4 –64 –27.4 18.8 –415 –34.4
2012 234.5 –11 –20.7 50.4 –528 –26.2
2013 122.4 –120 –24.8 42.8 –427 –26.6
2014 188.1 –149 –27.6 35.2 –152 –31.0
2015 14.5 20 –24.5 0.5 –161 –28.7
2016 11.1 –52 –23.7 1.1 –147 –26.7
2017 4.2 –19 –24.2 1.8 –185 –27.1
Figure 6

Temporal trends in δ13C and D14C of POCsusp collected from NCG sites during 2010–2017. A) δ13C and B) Δ14C of POCsusp from NCG (non-seep) euphotic (<300 m), and C) δ13C and D) Δ14C of POCsusp from NCG deep (>300 m). Red squares indicate the weighted mean for each sampling year; red lines are visual guides of possible trends. Black dashed line from 2012 to 2014 in D) indicates linear regression (y = 159.58x – 321604, n = 43, r = 0.7258, p < 0.0001) as a measure of recovery rate. Each panel includes data from Cherrier et al. (2014) for 2011 and 2012. DOI: https://doi.org/10.1525/elementa.389.f6

## Biogenic methane

Dissolved CH4 concentrations in the water column varied from 2.6 to 11.6 nM, while the isotopic composition of methane varied from –37 to –52‰. A subsurface maximum in methane concentration was observed in both profiles within the euphotic zone at 60–75 m depth (Figure 7). The average δ13C value, weighting the two profiles equally, was –41.4 ± 1.0‰ (n = 19). For the mixing model, we assumed that this methane was produced from modern photosynthetic carbon, not derived from nearby seeps, and had a Δ14C value of 39 ± 26‰ (n = 79). The δ13C value we observed was similar to those measured in the Atlantic and Pacific oceans which varied between –43 and –45‰ (Holmes et al., 2000). Karl et al. (2008) have suggested that oceanic water column CH4 is produced aerobically as a by-product of methylphosphonate decomposition in phosphate-stressed waters, supporting our assumption of a modern 14C value for this methane. Rakowski et al. (2015) observed depletion of phosphate in the euphotic zone at the methane maximum, where we similarly observed it. The 13C value is consistent with production from a methylated substrate in limited supply that is consumed quantitatively (Kelley et al., 2012; Tazaz et al., 2013).

Figure 7

Depth profiles of biogenic methane concentration and δ13C signature. A) Methane concentration and B) δ13C for methane at two sites: 28.6690 N, 88.3584 W, closed symbols; and 28.3255 N, 88.3865 W, open symbols (see Figure 2). DOI: https://doi.org/10.1525/elementa.389.f7

## Mixing models

The two-endmember mixing model indicated that the bulk of the carbon in POCsusp from the NCG euphotic (<300 m), seep euphotic and NCG deep (>300 m) sites was derived from modern surface production (Table 3). In contrast to seep euphotic, seep deep POCsusp had incorporated the most petrocarbon, averaging 57% ± 13 (n = 9), while NCG deep POCsusp averaged 29% ± 16 (n = 39) petrocarbon (Table 3). Our sensitivity test showed the greatest variation in the euphotic POCsusp, where Δ14C was close to the modern endmember. The two-endmember model estimations of the %modern for the euphotic test samples were within 2–3% of the model values, and the %petrocarbon estimations also varied by 2–3%. The deep-water source estimations varied by 0–1% for both %modern and %petrocarbon.

Table 3

Percent (%) contributions of carbon sources to POCsusp from a two-endmember mixing model and the MixSIAR model. DOI: https://doi.org/10.1525/elementa.389.t3

Site type Sample deptha Two-endmember mixing model MixSIAR mixing model

Modern surface production Petrocarbon n Modern surface production Riverine input Sediment Oil Fossil methane Biogenic methane n

Mean ± SD Range Mean ± SD Range Mean ± SD Mean ± SD Mean ± SD Mean ± SD Mean ± SD Mean ± SD

NCGb Euphotic 86 ± 14 47–100 14 ± 14 0–53 53 45.1 ± 11.0 41.2 ± 12.5 4.3 ± 5.6 2.0 ± 1.2 2.2 ± 1.9 5.2 ± 3.5 55
Deep 71 ± 16 38–92 29 ± 16 8–62 39 19.9 ± 10.0 46.3 ± 11.8 6.0 ± 6.0 15.4 ± 4.1 4.3 ± 2.9 8.1 ± 4.8 39
Seep Euphotic 81 ± 15 51–98 19 ± 15 2–49 12 39.0 ± 12.4 44.5 ± 13.7 3.8 ± 5.9 8.2 ± 3.6 1.5 ± 1.4 3.0 ± 2.5 14
Deep 43 ± 13 23–71 57 ± 13 29–76 9 11.6 ± 6.1 33.7 ± 8.2 3.4 ± 3.8 45.7 ± 5.3 2.3 ± 1.8 3.4 ± 2.6 9

a Euphotic indicates <300 m; deep, >300 m.

b Non-seep north central Gulf (NCG) sites.

The MixSIAR model (Table 3) suggested that POCsusp in the north central GOM is heavily derived from riverine inputs (up to 46%), followed by modern surface production (up to 45%), and, at seep deep sites, by oil (up to 46%). All deep-water POCsusp had higher contributions from hydrocarbons than euphotic POCsusp. Euphotic POCsusp at seep sites also had higher contributions from oil-derived carbon than at NCG euphotic sites; i.e., 8.2 ± 3.6% (n = 14) compared to 2.0 ± 1.2% (n = 55). Sediment, fossil methane, and biogenic methane contributed very little to the organic carbon in POCsusp, with high standard deviations of their means.

To characterize POCsusp in the broader context of the GOM, we plotted the δ13C and Δ14C signatures for other carbon reservoirs in the GOM, including: POCsink, non-seep sediment, seep sediment, and DIC (Figure 8). We also included signatures (as provided in Methods) for the different potential carbon sources to these pools, including modern surface production, riverine input, sediment, biogenic methane, DWH methane, and oil (Figure 8).

Figure 8

Carbon source endmembers and other carbon pools in the GOM. Plot of δ13C vs Δ14C of carbon endmembers and of POCsusp (this study and Cherrier et al., 2014, for NCG Deep 2011 and 2012), POCsink (Yan et al., 2016), GOM sediment (Chanton et al., 2015), GOM seep sediment (Chanton, 2018a), and GOM DIC (Chanton, 2018b). Data for POCsusp are presented by depth, with NCG euphotic (<300 m) from 2010–2017 grouped together (green open diamond) and NCG deep (>300 m) separated by year and listed at the bottom of the inset legend. Seep site POCsusp is indicated by blue triangles. Endmembers include surface production (green, δ13C = –21.2 ± 1.5‰, n = 82; Δ14C = 39 ± 26‰, n = 79), fossil methane (red, δ13C = –57.4 ± 0.4‰, Crespo-Medina et al., 2014; Δ14C = –1000‰), and oil (black, δ13C = –27‰; Δ14C = –1000‰), riverine input (purple, δ13C = –26.3 ± 1.1‰; Δ14C = –154 ± 68‰, Cai et al., 2015), sediment (grey, δ13C = –21.5 ± 0.8‰; Δ14C = –200 ± 29‰, Chanton et al., 2015) and biogenic methane (orange, δ13C = –41.4 ± 1.0‰, n = 19; Δ14C = –39 ± 26‰, n = 79). DOI: https://doi.org/10.1525/elementa.389.f8

## Statistics

The data were non-normally distributed; therefore, the non-parametric Mann-Whitney U tests were used to analyze the variation of δ13C and Δ14C signatures of POCsusp, from 2010 to 2017. We compared the importance of depth in the water column (euphotic <300 m or deep >300 m) and site type (NCG or seep) in determining the isotopic signatures of POCsusp (Tables 4 and 5) using the adjusted p-value of 0.008 to define significance. There were significant differences in δ13C signatures when comparing between depths, regardless of site classification. For instance, the median values for δ13C of POCsusp from NCG euphotic (–24.1‰) and NCG deep (–27.0‰) were significantly different (U = 1656, p < 0.001, r = 0.43), as were those for NCG deep (–27.0‰) and seep euphotic (–24.8‰) (U = 992, p < 0.001, r = 0.42). Comparisons δ13C of POCsusp involving the same depth zones yielded similarities: the median value for NCG euphotic (–24.1‰) did not differ from that for seep euphotic (–24.8‰) (U = 3065, p = 0.27, r = 0.08), nor did the median for NCG deep (–27.0‰) differ from that of seep deep (–27.0‰) (U = 1034, p = 0.96, r = 0.003). For radiocarbon, comparisons between different depth zones revealed significantly different Δ14C signatures, except when comparing median values for NCG deep (–224‰) and seep euphotic (–78‰), which were similar (U= 132, p = 0.007, r = –0.37). POCsusp from the NCG euphotic and euphotic seep (medians of –60‰ and –78‰, respectively) were the same (U = 359, p = 0.56, r = 0.07), but unlike δ13C, there were significant differences between NCG deep (median = –224‰) and seep deep (median = –552‰) (U = 28, p < 0.001, r = 0.56) (Table 5).

Table 4

Mann-Whitney U Test for δ13C comparisons for samples collected during 2010–2017. DOI: https://doi.org/10.1525/elementa.389.t4

Treatment pair Median Range n U P r

NCG euphotic vs NCG deep –24.1 –17.8 to –35.4 110 1656 p < 0.001 0.43
–27.0 –20.6 to –35.2 63
NCG euphotic vs seep euphotic –24.1 –17.8 to –35.4 110 3065 p = 0.27 0.08
–24.8 –19.3 to –28.8 62
NCG euphotic vs seep deep –24.1 –17.8 to –35.4 110 755 p < 0.001 0.42
–27.0 –21.4 to –34.3 33
NCG deep vs seep euphotic –27.2 –20.6 to –35.2 63 992 p < 0.001 0.42
–24.8 –19.3 to –28.8 62
NCG deep vs seep deep –27.2 –20.6 to –35.2 63 1034 p = 0.96 0.003
–27.0 –21.4 to –34.3 33
Seep euphotic vs seep deep –24.8 –19.3 to –28.8 62 8486 p < 0.001 0.43
–27.0 –21.4 to –34.3 33

Table 5

Mann-Whitney U Test for Δ14C comparisons for samples collected during 2010–2017. DOI: https://doi.org/10.1525/elementa.389.t5

Treatment pair Median Range n U P r

NCG euphotic vs NCG deep –60 54 to –515 57 394 p < 0.001 0.53
–224 –48 to –603 37
NCG euphotic vs seep euphotic –60 54 to –515 57 359 p = 0.56 0.07
–78 71 to –468 14
NCG euphotic vs seep deep –60 54 to –515 57 12 p < 0.001 0.57
–552 –263 to –756 9
NCG deep vs seep euphotic –224 –48 to –603 37 132 p = 0.007 –0.37
–78 71 to –468 14
NCG deep vs seep deep –224 –48 to –603 37 28 p < 0.001 0.56
–552 –263 to –756 9
Seep euphotic vs seep deep –78 71 to –468 14 3 p < 0.001 0.77
–552 –263 to –756 9

## Discussion

The first goal of this study was to characterize any temporal trends in the δ13C and Δ14C signatures of suspended POC in the northern Gulf of Mexico following the DWH oil spill in 2010. Isotopically depleted values for POCsusp indicating a fossil petrocarbon source were observed following the spill (Figure 6), particularly in the 14C content of suspended particles below the euphotic zone at NCG sites. The influence of apparent DWH-derived material was greatest in 2011 and 2012, with recovery beginning thereafter and proceeding until 2014 when the isotopic composition of POCsusp reached an asymptotic value (Figure 6).

Yan et al. (2016), Chanton et al. (2018), and Geiring et al. (2018) described the effects and recovery of the POCsink pool following the blowout. Yan et al. (2016) found elevated levels of barium, a component of drilling mud, in POCsink from August 2010 through January 2011, when they returned to pre-spill baseline levels. Chanton et al. (2018) found that POCsink recovered in 1–3 years depending on the tracer that was evaluated. δ34S and PAH indicated an approximate 2-year recovery time, while Δ14C indicated a recovery time of ~3 years. These recovery periods are on a similar time scale to our estimate of a 4-year recovery period in the Δ14C of POCsusp in deep water at NCG sites (Figure 6).

A second goal was to determine the extent of fossil carbon influence on suspended particles. We found a wide range of natural variability in both δ13C and Δ14C signatures of POCsusp across the northern GOM, from seep and non-seep sites and a range of depths, from surface to 1900 m (Figure 3). Compared to suspended particles in the Sargasso Sea and Pacific Station M, the GOM exhibits more variability and greater depletion in δ13C and Δ14C signatures (Figure 1; Druffel et al., 1992, 1996). The primary carbon source to the Sargasso and Pacific particulates is modern photosynthetic production, which does not create a co-variation of δ13C with Δ14C. The depletion in Δ14C in the Sargasso and mid-Pacific was not observed to be greater than –100‰, even to depths of 4000 m. The δ13C value of the Pacific and Atlantic suspended particles was generally –20 to –22‰ without depth variation. The co-variation of δ13C and Δ14C observed in the GOM and the Mid-Atlantic Bight (as presented in the Introduction) are due to the incorporation of a second source that is depleted in both 14C and 13C, consistent with petrocarbon-derived material. In the Southern Gulf of Mexico from 20° to 22°N, Gonzalez-Ocampo et al. (2007) reported POCsusp depth trends in δ13C, with 13C depletion at depth reaching values as low as –23.7 ± 0.5‰. Values in surface water were –22.5 ± 0.5‰.

We admit some reservations about the results of the MixSIAR mixing model, as two of our sources, riverine input and sedimentary organic carbon had some surprising results. The MixSIAR model was used to constrain six carbon sources with two isotopic tracers. The riverine input (34–46%) was estimated to be greater than the input from surface production (11.6–45.1%) for all sites except NCG euphotic (riverine: 41%; surface production: 45%). For the workings of the model, the riverine endmember was located isotopically in the middle of the bulk of the POCsusp values, rather than along the boundary of our data (Figure 4). This location could cause the model to estimate a higher percent contribution to POCsusp because of the isotopic similarities between the POCsusp and riverine input. The data might well represent mixing between modern carbon and a more depleted source. On the other hand, the apparent high riverine contribution may be due to the differences in lability between the riverine and modern sources. Riverine carbon is less labile than fresher photosynthetic production, which causes it to cycle more slowly than surface production (Wang et al., 2004). The salinity at the stations where we collected POCsusp varied (Table S1), but most sites did not indicate major mixing with freshwater sources. However, Wang et al. (2004) found that δ13C and C:N ratios of POCsusp from the Mississippi and northern GOM exhibited non-conservative behavior when mixing with higher salinity waters. A decoupling occurs between the POCsusp and the freshwater input which allows the 2.30 Tg POC yr–1 exported from the Mississippi (Cai et al., 2015) to mix with GOM POCsusp and accumulate over the POCsusp residence time of 5–10 years, increasing the contribution from riverine POCsusp.

Whereas the riverine contribution to POCsusp was higher than expected, the sedimentary contribution was low and consistent throughout the water column. Chanton et al. (2018) found that sinking POC, collected from traps 30 m above the seafloor, did not carry a strong signal from resuspended sediment, but POCsusp integrates over longer time scales. Diercks et al. (2018) detected both small-scale and hurricane-sized resuspension events, which could play a role in the transport of sedimented petrocarbon. The number and overall scale of resuspension events in the GOM is unknown, but they potentially introduce more than 4–6% into the POCsusp pool, especially near the seafloor. The sedimentary organic carbon endmember is similar in isotope space to riverine input (Figure 4), making the two sources difficult to separate. Employing sulfur isotopes and lithogenic silica content might better separate sedimentary and riverine sources.

Unlike the MixSIAR model, the two-endmember model is simpler and better constrained. This model indicated the local influence of seeps, particularly on deep-water POCsusp, and the importance of modern surface production on POCsusp away from seeps (Table 3). Nonetheless, petrocarbon still contributed about 30% of POCsusp in the deep GOM, even away from seep sites, a phenomenon not observed in the Atlantic or Pacific. Even though the two-endmember model does not capture the full complexity of all of the potential sources to POCsusp in the GOM, the results of the MixSIAR model, using only two isotopic measurements, can only be fully interpreted with reservations, for the aforementioned reasons. Therefore, we have greater confidence in the two-endmember approach.

We estimated the new, post-spill baseline signatures for NCG (non-seep) POCsusp in the GOM to be δ13C = –24.1 ± 0.4‰ (n = 15) and Δ14C = –17 ± 36‰ (n = 15) for the euphotic zone and δ13C = –27.5 ± 1.1‰ (n = 12) and Δ14C = –164 ± 19‰ (n = 7) for deep-water suspended particles. These values are the means of the POCsusp weighted averages from the NCG for the last three sampling years (2015–2017; Figure 6). Following the recovery of deep-water Δ14C signatures in 2014, we suggest that POCsusp reached a post-blowout baseline, as both the δ13C and Δ14C signatures had stabilized by these years. In comparison to baselines from the Sargasso Sea and Pacific Ocean, the baseline for POCsusp from the GOM was more depleted for δ13C and Δ14C. We estimated the δ13C and Δ14C baselines for POCsusp collected in the Sargasso and Pacific (Druffel et al., 1992, 1996, 2003) for our depth zones to be: euphotic δ13C = –22.1‰ (n = 41) and Δ14C = 73 (n = 42); and deep POCsusp δ13C = –21.2‰ (n = 82) and Δ14C = 16‰ (n = 83). The differences in δ13C between the GOM and the Sargasso and Pacific are due to differences in the increased relative importance of hydrocarbon and terrestrially sourced material to the GOM, while the Δ14C differences are caused by both collection years and the relative importance of differing carbon sources. The gap of 22–32 years between the collection of the Sargasso and Pacific samples and our samples results in the older samples being more enriched in 14C. This effect is due to the atmospheric nuclear testing that caused radiocarbon values to spike and mix from the atmosphere into the biosphere and hydrosphere, including the ocean. The mixing process caused a lag between atmospheric CO2 radiocarbon signatures and DIC in the ocean (Levin and Hesshaimer, 2000; McNichol and Aluwihare, 2007).

Unlike POCsusp from the Sargasso Sea and Pacific Ocean, depth played a significant role in the variation of δ13C of POCsusp in the GOM over the period of 2010–2017. The significant differences observed between euphotic (<300 m) and deep (>300 m) reflect the relative importance of the two sources, with petrocarbon-derived material increasing in importance below 300 m (Tables 2 and 4). Suspended particles in deep water were depleted due to the hydrocarbon input potentially from seep sites and/or the DWH blowout, while POCsusp from the same depth (whether euphotic or deep) had similar δ13C, regardless of site type (seep or NCG).

We also found significant differences between the Δ14C of POCsusp in euphotic and deep POCsusp for both site types (seep or NCG) (Table 5). This finding suggests that suspended particles in the GOM, including at non-seep sites, are more depleted in 14C in deeper waters than suspended particles in other oceans, probably due to the natural hydrocarbon seepage in the GOM, although completely ruling out the lingering petrocarbon from the oil spill is difficult at this point. The significant differences between the Δ14C of deep-water POCsusp from NCG and seep areas were not observed for the δ13C results, as δ13C is less sensitive to variations in the input terms (Bosman et al., 2016). The more depleted Δ14C of POCsusp found at seep sites suggests that the presence of natural hydrocarbon seepage significantly affects the Δ14C of suspended particles in the Gulf.

## Conclusions

Based on our assessment of the δ13C and Δ14C signatures of POCsusp, petrocarbon is an important carbon source to suspended particles in the GOM, in contrast to the situation in the Atlantic and Pacific oceans. In the north central Gulf during our study period, POCsusp was isotopically depleted relative to POCsink or sediment (Figure 8). DIC fixed by marine primary production is the primary source of carbon to POCsink and to the non-seep sediment. We found deep POCsusp from seep sites to be composed of about 45% oil-derived petrocarbon, while deep-water POCsusp from the NCG sites may contain as much as 15% oil-sourced petrocarbon and 3.5% methane-sourced petrocarbon. In the Gulf of Mexico, there are at least three clear and separate carbon sources (Figure 8): one driven by surface primary production, observed in POCsink and non-seep sediments; the second attributed to the microbial cycling of methane and oil, observed to a greater extent in POCsusp and seep sediments; and the third, a riverine contribution, pervasive but more challenging to quantify unambiguously.

## Data Accessibility Statement

Data deposition: Data are publicly available through the Gulf of Mexico Research Initiative Information & Data Cooperative (GRIIDC) at https://data.gulfresearchinitiative.org, 10.7266/N7FX77C7.

## Acknowledgements

AMS samples were run at Lawrence Livermore Center for Accelerator Mass Spectrometry, the University of Georgia Center for Applied Isotopic Studies, and the National Ocean Sciences Accelerator Mass Spectrometry facility (NOSAMS) at Woods Hole Oceanographic. We thank Alexander Cherinsky, Tom Guilderson, Ann McNichol, Kathryn Elder, and Mark Roberts. Samples were collected from the RV Endeavor, RV Pelican and RV Weatherbird and we thank their crews. We thank Burt Wolff and Yang Wang for use of the facilities at the National High Magnetic Field Laboratory, which is supported by National Science Foundation Cooperative Agreement No. DMR-1644779 and the State of Florida. We especially thank the editor, Dr. Jody Deming, for her thorough review of our work and her detailed attention to our manuscript. We thank associate editor Lisa Miller, reviewer Brett Walker, and an anonymous reviewer.

## Funding information

This research was made possible by grants from The Gulf of Mexico Research Initiative through its consortiums: Ecosystem Impacts of Oil and Gas Inputs to the Gulf (ECOGIG), The Center for the Integrated Modeling and Analysis of the Gulf Ecosystem (C-Image), and Deep Sea to Coast Connectivity in the Eastern Gulf of Mexico (Deep-C). This is ECOGIG Contribution #523.

## Competing interests

The authors have no competing interests to declare.

## Author contributions

• KLR wrote the paper with JPC, collected samples, analyzed samples and data
• SB edited the paper, collected samples, analyzed samples and data
• SW collected samples, analyzed samples
• CM collected samples, analyzed samples
• JPM collected samples analyzed data
• JPC co-wrote the paper, analyzed data

## References

1. Bacon, MP and Anderson, RF. 1982. Distribution of Thorium isotopes between dissolved and particulate forms in the deep sea. J Geophys Res 87(C3): 2045–2056. DOI: 10.1029/JC087iC03p02045

2. Bauer, JE and Druffel, ERM. 1998. Ocean margins as a significant source of organic matter to the deep open ocean. Nature 392: 482–485. DOI: 10.1038/33122

3. Bauer, JE, Druffel, ERM, Wolgast, DM and Griffin, S. 2001. Sources and cycling of dissolved and particulate organic radiocarbon in the northwest Atlantic continental margin. Global Biogeochem Cy 15(3): 615–636. DOI: 10.1029/2000GB001314

4. Bauer, JE, Druffel, ERM, Wolgast, DM and Griffin, S. 2002. Temporal and regional variability in sources and cycling of DOC and POC in the northwest Atlantic continental shelf and slope. Deep Sea Res Pt II 49: 4387–4419. DOI: 10.1016/S0967-0645(02)00123-6

5. Börjesson, G, Chanton, J and Svensson, BH. 2001. Methane oxidation in two Swedish landfill covers measured with carbon-13 to carbon-12 isotope ratios. J Environ Qual 30(2): 369–376. DOI: 10.2134/jeq2001.302369x

6. Börjesson, G, Sundh, I, Tunlid, A, Frostegård, Å and Svensson, BH. 1998. Microbial oxidation of CH4 at high partial pressures in an organic landfill cover soil under different moisture regimes. FEMS Microbiol Ecol 26(3): 207–217. DOI: 10.1111/j.1574-6941.1998.tb00506.x

7. Cai, Y, Guo, L, Wang, X and Aiken, G. 2015. Abundance, stable isotopic composition, and export fluxes of DOC, POC, and DIC from the Lower Mississippi River during 2006–2008. J Geophys Res Biogeosci 120: 2273–2288. DOI: 10.1002/2015JG003139

8. Carlson, CA and Hansell, DA. 2014. DOM sources, sinks, reactivity, and budgets. In Hansell, DA and Carlson, CA (Eds.), Biogeochemistry of marine dissolved organic matter (second edition). Maine: Elsevier Inc. DOI: 10.1016/B978-0-12-405940-5.00003-0

9. Chanton, J. 2018a. Sediment organic isotope data collected in the northern Gulf of Mexico seafloor on different cruises from 2010-05-01 to 2017-06-18. Distributed by: Gulf of Mexico Research Initiative Information and Data Cooperative (GRIIDC), Harte Research Institute, Texas A&M University-Corpus Christi. DOI: 10.7266/N7Q52N7D

10. Chanton, J. 2018b. Dissolved Inorganic Carbon 14C values, northern Gulf of Mexico, May 2011 to May 2012. Distributed by: Gulf of Mexico Research Initiative Information and Data Cooperative (GRIIDC), Harte Research Institute, Texas A&M University-Corpus Christi. https://data.gulfresearchinitiative.org/pelagos-symfony/data/R4.x268.000%3A0104. DOI: 10.7266/N7W37TWR

11. Chanton, J and Lewis, FG. 2002. Examination of coupling between primary and secondary production in a river-dominated estuary: Apalachicola Bay, Florida, U.S.A. Limnol Oceanogr 47(3): 683–697. DOI: 10.4319/lo.2002.47.3.0683

12. Chanton, J, Zhao, T, Rosenheim, BE, Joye, S, Bosman, S, Brunner, C, Yeager, KM, Diercks, AR and Hollander, D. 2015. Using natural abundance radiocarbon to trace the flux of petrocarbon to the seafloor following the deepwater horizon oil spill. Environ. Sci. Technol 49: 847–854. DOI: 10.1021/es5046524

13. Chanton, JP, Cherrier, J, Wilson, RM, Sarkodee-Adoo, J, Bosman, S, Mickle, A and Graham, WM. 2012. Radiocarbon evidence that carbon from the Deepwater Horizon spill entered the planktonic food web of the Gulf of Mexico. Environ Res Lett 7(4). DOI: 10.1088/1748-9326/7/4/045303

14. Chanton, JP, Giering, SLC, Bosman, SH, Rogers, KL, Sweet, J, Asper, VL, Diercks, AR and Passow, U. 2018. Isotopic composition of sinking particles: Oil effects, recovery and baselines in the Gulf of Mexico, 2010–2015. Elem Sci Anth 6: 43. DOI: 10.1525/elementa.298

15. Cherrier, J, Sarkodee-Adoo, J, Guilderson, TP and Chanton, JP. 2014. Fossil carbon in particulate organic matter in the Gulf of Mexico following the Deep Water Horizon event. Environ Sci Technol Lett 1: 108–112. DOI: 10.1021/ez400149c

16. Crespo-Medina, M, Meile, CD, Hunter, KS, Diercks, A-R, Asper, VL, Orphan, VJ, Tavormina, PL, Nigro, LM, Battles, JJ, Chanton, JP, Shiller, AM, Joung, D-J, Amon, RMW, Bracco, A, Montoya, JP, Villareal, TA, Wood, AM and Joye, SB. 2014. The rise and fall of methanotrophy following a deepwater oil-well blowout. Nat Geosci 7: 423–427. DOI: 10.1038/ngeo2156

17. Deuser, WG. 1986. Seasonal and interannual variations in deep-water particle fluxes in the Sargasso Sea and their relation to surface hydrography. Deep Sea Res 33: 225–246. DOI: 10.1016/0198-0149(86)90120-2

18. Diercks, AR, Dike, C, Asper, VL, DiMarco, SF, Chanton, JP and Passow, U. 2018. Scales of seafloor sediment resuspension in the northern Gulf of Mexico. Elem Sci Anth 6(32): DOI: 10.1525/elementa.285

19. Druffel, ERM, Bauer, JE, Griffin, S and Hwang, J. 2003. Penetration of anthropogenic carbon into organic particles of the deep ocean. Geophys Res Lett 30(14). DOI: 10.1029/2003GL017423

20. Druffel, ERM, Bauer, JE, Williams, PM, Griffin, S and Wolgast, D. 1996. Seasonal variability of particulate organic radiocarbon in the northeast Pacific Ocean. J Geophys Res 101(C9): 20543–20552. DOI: 10.1029/96JC01850

21. Druffel, ERM, Williams, PM, Bauer, JE and Ertel, JR. 1992. Cycling of dissolved and particulate organic matter in the open ocean. J Geophys Res 97(C10): 15639–15659. DOI: 10.1029/92JC01511

22. Du, M and Kessler, JD. 2012. Assessment of the spatial and temporal variability of bulk hydrocarbon respiration following the Deepwater Horizon oil spill. Environ Sci Technol 46(19): 10499–10507. DOI: 10.1021/es301363k

23. Fernández-Carrera, A, Rogers, KL, Weber, SC, Chanton, JP and Montoya, JP. 2016. Deep Water Horizon oil and methane carbon entered the food web in the Gulf of Mexico. Limnol Oceanogr 61: S387–S400. DOI: 10.1002/lno.10440

24. Gonzalez-Ocampo, M, Escobar-Briones, E and Morales-Puente, P. 2007. Composición y caracterización isotopica δ13C de carbono organico particulado en aguas oceanicas del suroeste de Golfo de Mexico. In: Hernandezdela Torre, B and Castro, GG (eds.). Carbon en ecosistemas acuaticos de Mexico. Secretaria de Medio Ambiente y Recursos Naturales, Instituto Nacional de Ecologiea, Centro de Investigación Cientifica, y de Educación Superior de Ensenada . Ensenada, BC, Mexico.

25. Graham, WM, Condon, RH, Carmichael, RH, D’Ambra, I, Patterson, HK, Linn, LJ and Hernandez, FJ, Jr. 2010. Oil carbon entered the coastal planktonic food web during the Deepwater Horizon oil spill. Environ Res Lett 5(4): 045301. DOI: 10.1088/1748-9326/5/4/045301

26. Holmes, ME, Sansone, FJ, Rust, TM and Popp, BN. 2000. Methane production, consumption and air-sea exchange in the open ocean: An evaluation based on carbon isotopic ratios. Global Biogeochem Cy 14(1): 1–10. DOI: 10.1029/1999GB001209

27. Joye, SB, MacDonald, IR, Leifer, I and Asper, V. 2011. Magnitude and oxidation potential of hydrocarbon gases released from the BP oil well blowout. Nat Geosci 4(3): 160–164. DOI: 10.1038/ngeo1067

28. Karl, DM, Beversdorf, L, Björkman, KM, Church, MJ, Martinez, A and Delong, EF. 2008. Aerobic production of methane in the sea. Nat Geosci 1: 473–478. DOI: 10.1038/ngeo234

29. Kelley, CA, Poole, JA, Tazaz, AM, Chanton, JP and Bebout, BM. 2012. Substrate limitation for methanogenesis in hypersaline environments. Astrobiology 12(2): 89–97. DOI: 10.1089/ast.2011.0703

30. Kessler, JD. 2011. A persistent oxygen anomaly reveals the fate of spilled methane in the deep Gulf of Mexico. Science 331: 312–315. DOI: 10.1126/science.1199697

31. Lehr, W, Bristol, S and Possolo, A. 2010. Federal interagency solutions group, oil budget calculator science and engineering team. Oil Budget Calculator . Technical document. Available at http://www.restorethegulf.gov/sites/default/files/documents/pdf/OilBudgetCalc_Full_HQ-Print_111110.pdf.

32. Levin, I and Hesshaimer, V. 2000. Radiocarbon – a unique tracer of global carbon cycle dynamics. Radiocarbon 42(1): 69–80. DOI: 10.1017/S0033822200053066

33. MacDonald, IR, Garcia-Pineda, O, Beet, A, Daneshgar Asl, S, Feng, L, Graettinger, G, French-McCay, D, Holmes, J, Hu, C, Huffer, F, Leifer, I, Muller-Karger, F, Solow, A, Silva, M and Swayze, G. 2015. Natural and unnatural oil slicks in the Gulf of Mexico. J Geophys Res Ocean 120(12): 8364–8380. DOI: 10.1002/2015JC011062

34. Magen, C, Lapham, LL, Pohlman, JW, Marshall, K, Bosman, S, Casso, M and Chanton, JP. 2014. A simple headspace equilibration method for measuring dissolved methane. Limnol Oceanogr: Methods 12: 637–650. DOI: 10.4319/lom.2014.12.637

35. McNichol, AP and Aluwihare, LI. 2007. The power of radiocarbon in biogeochemical studies of the marine carbon cycle: insights from studies of dissolved and particulate organic carbon (DOC and POC). Chem Rev 107(2): 443–466. DOI: 10.1021/cr050374g

36. Montoya, JP, Horrigan, SG and McCarthy, JJ. 1990. Natural abundance of 15N in particulate nitrogen and zooplankton in the Chesapeake Bay. Mar Ecol Prog Ser 65: 35–61. DOI: 10.3354/meps065035

37. Peterson, B, Fry, B, Hullar, M, Saupe, S and Wright, R. 1994. The distribution and stable carbon isotopic composition of dissolved organic carbon in estuaries. Estuaries 17(1B): 111–121. DOI: 10.2307/1352560

38. Rakowski, C, Magen, C, Bosman, S, Rogers, KL, Gillies, LE, Chanton, JP and Mason, OU. 2015. Methane and microbial dynamics in the Gulf of Mexico water column. Front Mar Sci 2: 69. DOI: 10.3389/fmars.2015.00069

39. R Core Team. 2015. R: A language and environment for statistical computing. Vienna, Austria: R Foundation for Statistical Computing. Available at http://www.R-project.org/.

40. Skarke, A, Ruppel, C, Kodis, M, Brothers, D and Lobecker, E. 2014. Widespread methane leakage from the sea floor on the northern US Atlantic margin. Nat Geosci 7: 657–661. DOI: 10.1038/ngeo2232

41. Stock, BC and Semmens, BX. 2016. MixSIAR GUI User Manual. Version 3.1. https://github.com/brianstock/MixSIAR. DOI: 10.5281/zenodo.47719

42. Stuiver, M and Pollach, HA. 1977. Discussion: Reporting of 14C data. Radiocarbon 19(3): 355–363. PDF, University of Arizona, 1999. DOI: 10.1017/S0033822200003672

43. Tazaz, AM, Bebout, BM, Kelley, CA, Poole, J and Chanton, JP. 2013. Redefining the isotopic boundaries of biogenic methane: Methane from endoevaporites. Icarus 224(2): 268–275. DOI: 10.1016/j.icarus.2012.06.008

44. Valentine, DL, Kessler, JD, Redmond, MC, Mendes, SD, Heintz, MB, Farwell, C, Hu, L, Kinnaman, FS, Yvon-Lewis, S, Du, M, Chan, EW, Garcia Tigreros, F and Villanueva, CJ. 2010. Propane respiration jump-starts microbial response to a deep oil spill. Science 330(6001): 208–211. DOI: 10.1126/science.1196830

45. Walker, BD, Druffel, ERM, Kolasinski, J, Roberts, BJ, Xu, X and Rosenheim, BE. 2017. Stable and radiocarbon isotopic composition of dissolved organic matter in the Gulf of Mexico. Geophys Res Lett 44: 8424–8434. DOI: 10.1002/2017GL074155

46. Wang, X-C, Chen, RF and Gardner, GB. 2004. Sources and transport of dissolved and particulate organic carbon in the Mississippi River estuary and adjacent coastal waters of the northern Gulf of Mexico. Mar Chem 89: 241–256. DOI: 10.1016/j.marchem.2004.02.014

47. Weber, SC, Peterson, L, Battles, JJ, Roberts, BJ, Peterson, RN, Hollander, DJ, Chanton, JP, Joye, SB and Montoya, JP. 2016. Hercules 265 rapid response: Immediate ecosystem impacts of a natural gas blowout incident. Deep-Sea Res Pt II 129: 66–76. DOI: 10.1016/j.dsr2.2015.11.010

48. Williams, PM and Druffel, ERM. 1987. Radiocarbon in dissolved organic matter in the central North Pacific Ocean. Nature 330: 246–248. DOI: 10.1038/330246a0

49. Wilson, RM, Cherrier, J, Sarkodee-Adoo, J, Bosman, S, Mickle, A and Chanton, JP. 2016. Tracing the intrusion of fossil carbon into coastal Louisiana macrofauna using natural 14C and 13C abundances. Deep Sea Res Pt II 129: 89–95. DOI: 10.1016/j.dsr2.2015.05.014

50. Yan, B, Passow, U, Chanton, JP, Nöthig, E-M, Asper, V, Sweet, J, Pitiranggon, M, Diercks, A and Pak, D. 2016. Sustained deposition of contaminants from the Deepwater Horizon spill. Proc Natl Acad Sci USA 113(24): E3332–E3340. DOI: 10.1073/pnas.1513156113

51. Yvon-Lewis, SA, Hu, L and Kessler, J. 2011. Methane flux to the atmosphere from the Deepwater Horizon oil disaster. Geophys Res Lett 38: L01602. DOI: 10.1029/2010GL045928