Three deepwater hydrocarbon seep sites in the northern Gulf of Mexico that feature near-seafloor gas hydrates, MC118 (depth = 900 m), GC600 (depth = 1250 m) and GC185 (depth = 550 m), were investigated during the Remote Sensing and Sea-Truth Measurements of Methane Flux to the Atmosphere (HYFLUX) study in July 2009. Continuous measurements of air and sea surface concentrations of methane were made to obtain high spatial and temporal resolution of the diffusive net sea-to-air fluxes. The atmospheric methane fluctuated between 1.70 and 2.40 parts per million (ppm) during the entire cruise except for high concentrations (up to 4.01 ppm) sampled during the end of the occupation of GC600 and the transit between GC600 and GC185. In conjunction with air-mass back trajectory analysis, these high concentrations are likely from a localized methane source to the atmosphere. Methane concentrations in surface seawater and methane net sea-to-air fluxes show high temporal and spatial variability within and between sites. The presence of ethane and propane in the surface seawater indicates a thermogenic source in the plume areas, suggesting the surface methane could be at least partly attributable to transport from the deepwater hydrocarbon seeps. Results from interpolations within the survey areas show the daily methane fluxes to the atmosphere at the three sites range from 0.744 to 300 mol d−1. Extrapolating the highest daily sea-to-air flux of methane to other deepwater seeps in the northern Gulf of Mexico suggests that the net diffusive sea-to-air flux from deepwater hydrocarbon seeps in this region is an insignificant source to the atmospheric methane.
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 Methane (CH4), one of the most important greenhouse gases, has a warming potential 23 times that of carbon dioxide over a 100 year time horizon [Ramaswamy et al., 2001]. It is also actively involved in tropospheric ozone production and stratospheric ozone destruction. The total amount of methane reserved in the form of gas hydrate is about 2 × 106 Tg in a global inventory [Boswell and Collett, 2011]. It is comparable to about 400 times the total mass of the global atmospheric methane, 4850 (±242) Tg [Intergovernmental Panel on Climate Change, 2001]. Although the gas hydrate is an enormous methane reservoir, the contribution of the gas hydrate from the seafloor to the atmospheric methane budget is poorly characterized. It is estimated that marine seeps emit 18–48 Tg yr−1 of methane from the continental shelves to the overlying water column [Hornafius et al., 1999]. However, the global emission from gas hydrates to the atmosphere is less than 5 Tg yr−1 [Reeburgh, 2007].
 Methane released from the seafloor or produced in microenvironments in the water column [e.g., Cynar and Yayanos, 1991; de Angelis and Lee, 1994] can reach the atmosphere through turbulent diffusion or rising bubbles. In shallow water, rising bubbles are the predominant pathway for delivering methane from seeps to the atmosphere, while the net sea-to-air fluxes via diffusion are also considerable [Mau et al., 2007; Schmale et al., 2005]. In deep water systems, turbulent diffusion is a commonly cited pathway to deliver methane to the atmosphere, whereas it is still debatable whether or not bubbles are capable of surviving from the seafloor to the surface and, if so, how much methane would be displaced by other gases (i.e., oxygen, nitrogen etc.) as they are stripped out of the water as the bubble moves to the surface [McGinnis et al., 2006; Rehder et al., 2002, 2009]. Methane transport via rising bubbles from the deepwater seeps to the atmosphere depends on a variety of geological and physical parameters, including intensity and composition of the seepages, bubble initial size, release depth, bubble path, and dissolution rate [Leifer and MacDonald, 2003]. Most previous studies reported that the diffusive net sea-to-air fluxes of methane from deepwater seep systems (water depth >200 m) are insignificant [e.g.,Kessler et al., 2006; Reeburgh et al., 1991; Schmale et al., 2005; Yvon-Lewis et al., 2011]. However, one recent study suggests that the diffusive net sea-to-air flux of methane from the deepwater hydrocarbon seeps to the atmosphere could be considerable [Solomon et al., 2009].
 To better understand and quantify the diffusive net sea-to-air fluxes of methane from deepwater hydrocarbon seeps, we investigated three deepwater seeps featuring near-seafloor gas hydrate in the northern Gulf of Mexico. High spatial and temporal resolution measurements were made to determine the net sea-to-air fluxes of methane over these hydrocarbon seeps.
2.1. Location and Measurements
 The HYFLUX cruise took place in the northern Gulf of Mexico during July 2009 (4–19 July 2009) aboard the R/V Brooks McCall. Intensive surface surveys were conducted above three active seeps, MC118 (Rudyville, 28.8522°N, 88.4928°W, 900 meters below sea level (mbsl)), GC600 (Oil Mountain, 27.3652°N, 90.5642°W, 1250 mbsl), and GC185 (Bush Hill, 27.7823°N, 91.5080°W, 550 mbsl) (Figure 1), which were characterized by seafloor gas hydrate deposits that were partly exposed to seawater. Active oil and gas venting was confirmed by a remotely operated vehicle (ROV) at fixed locations within all three sampling sites. Air and surface seawater samples were analyzed continuously (except for brief maintenance intervals) during occupation of the sites and transits. The air-sea sampling plan had two modes: (1) a coarse regular grid, where samples were spaced at a kilometer scale and (2) a fine sampling scale that occurred as the ship loitered above the ROV, where samples were spaced ≤10 m. The ship speed was kept below 4 knots over most of the seep areas (Figure 2e).
 To measure the diffusive net sea-to-air fluxes of methane and infer its origin, atmospheric and surface seawater dissolved C1-C3hydrocarbons were measured continuously with an automated sampling system coupled to a Weiss-type equilibrator and a Gas Chromatograph/Flame Ionization Detector (GC/FID, Agilent 6850) system. This technique only quantifies the diffusive net sea-to-air flux of dissolved methane and not the direct bubble injection of methane to the atmosphere; however, direct bubble injection to the atmosphere could be manifested in the data as enhanced atmospheric concentrations relative to surface seawater.
 Air samples were pumped continuously at ∼6 L min−1through 0.63 cm ID Synflex tubing (Motion Industries, Texas) mounted on the railing on the top of flying bridge and running to the laboratory. Surface seawater (about 4 m below the sea surface) was pumped into the Weiss-type equilibrator at 15 L min−1. Equilibrator headspace and ambient air were alternately sampled every 6 min using a stream select valve. The sample stream passed through a 20 μL sampling loop after being dehumidified by a Nafion dryer (Permapure Inc). The Nafion dryer and the 20 μL sampling loop were flushed with the sample air at a rate of 25 mL min−1 for 90 seconds before injection into the GC/FID, which was equipped with a 15 m long, 32 μm ID GS-GasPro column (1 m precolumn and 14 m main column) with nitrogen carrier gas. Prior to the cruise, a series of standard mixtures (C1-C3) ranging from 0 to 1000 parts per million (ppm) were made using two known concentration standards (15 and 1000 ppm) from Scott Specialty Gases. Standards with methane concentrations at 0.09 (±0.01), 1.09 (±0.02), 1.69 (±0.02) and 2.88 (±0.06) ppm were also calibrated against a whole air tank, which was calibrated to the NOAA-04 methane scale. The standards with methane concentrations at 0.09–2.88 ppm were used to create a standard curve to calibrate the instrument. Higher concentration standards 15 (±1.5), 503 (±25) and 1000 (±50) ppm were also run and used as an alternate calibration curve when the measured concentration exceeded the lower calibration range. The precision of the system was determined from five standard injections. The precision for concentrations ≤3 ppm was 3% for methane, 2% for ethane and 3% for propane. The precision for concentrations >3 ppm was less than 1% for methane, ethane and propane.
 The sea surface temperature and salinity were continuously measured by a conductivity-temperature-depth (CTD) sensor from Sea-Bird Electronics (SBE 19 plus) at the outflow of the equilibrator. Wind speeds and directions were continuously measured by an anemometer at a height of ∼9 m above the sea level.
 Due to the different solubilities for different gases, the time needed for the trace gas concentration in the headspace to reach equilibrium with the incoming seawater is different for each trace gas. The headspace mass concentration, Ce, at a time, t, can be expressed with the following equation when the equilibrator vent flow, Qv, is zero [Johnson, 1999]:
where τ1 = ; Ve is the volume of the headspace, 12.5 L; Qw is the volumetric flow rate of the seawater, 15 L min−1; ε is a dimensionless equilibrator coefficient, which is typically about 0.3–0.4 [Johnson, 1999]; α is the Oswald solubility coefficient; Ci is the initial mass concentration in the headspace and Cw is the mass concentration of the trace gas in the incoming seawater.
 When the equilibrator vent flow, Qv, is not zero, the air in the headspace is removed and replaced by the ambient air at a rate of Qv. The trace gas concentration in the headspace can then be expressed by the following equation [Johnson, 1999]:
where τv = and = + ; Ca is the mass concentration of the trace gas in the ambient air.
 Under normal operating conditions, the equilibrator vent flow is zero except the duration when the instrument is flushing the dryer and sample loop (i.e., collecting the headspace air sample). Assuming the equilibrator vent flow is off for a period of t1 (min) and on for a period of t2 (min) at a rate of Qv (ml min−1), the trace gas concentration in the headspace at t1 + t2 can be expressed as
Since the trace gas concentrations in the ambient air and in the equilibrator headspace were measured, Ca, Ci, and Ce are known. The trace gas concentration in seawater can be expressed as a function of Ca, Ci, and Ce (equation (4))
In this study, the vent flow, 25 ml min−1, was only on for 2.5 min between two seawater measurements, resulting in only 1% of difference in the Cw compared to the case without the vent flow. Given such a small effect, we can simplify equation (4) by assuming the vent flow is 0 during t1 to t2. Then τv is equal to 0, and τ1 is equal to τ2. Equation (4) can be expressed as
In equations (1)–(5), it is assumed that the trace gas concentration in the seawater is constant during t1 and t2. However, in reality, this assumption may not be true especially when the ship speed is fast. Therefore, assuming the seawater concentration is constant during a very short time period (Δt) (i.e., <1 s) and the seawater concentrations are …, for each Δt (nΔt = t1+ t2), the trace gas concentration in the headspace can be expressed by
Therefore, the fractional contributions of the true seawater concentrations, …, to the corrected seawater concentration (Cw) are a1, a2, …, an−1, an. For the very soluble gases (i.e., CO2, N2O), a1, a2, …, an−1, an exponentially increase from 0 to 1 as a1 goes to an, and Cw is more representative of an instantaneous incoming seawater concentration. For the less soluble gases (i.e., CH4, CO), a1, a2, …, an−1, an are close to 1/n and Cw is more representative of an average seawater concentration during the last nΔt min. In this study, the seawater concentrations were calculated using equation (4), and they represent average seawater concentrations over a period of 12 min. As the ship speed was in a range of 0–4 knots when sampling, 12 min represents a distance of 0–1480 m.
 Atmospheric methane during this cruise ranged from 1.70 to 4.01 ppm with a mean of 2.03 ppm (Figure 2a). The atmospheric methane fluctuated around a background concentration of 1.92 ppm during the occupation of the sites and transits except at the end of GC600 and the transit to GC185 (Figure 2a). The surface seawater methane concentrations ranged from 1.76 to 23.5 nmol L−1 at MC118, 1.76 to 11.9 nmol L−1 at GC600, and 1.72 to 4.48 nmol L−1 at GC185 (Table 1). The presence of ethane (Figure 2b) and propane (Figure 2c) in the surface seawater over the seep area (mainly at MC118 and GC 600) indicates a thermogenic contribution from the deepwater hydrocarbon seeps. The maximum methane concentration observed in surface seawater during this study, 156 nmol L−1, was observed on year day (YD) 191 (10 July 2009) on the continental shelf offshore from Louisiana (Figures 1 and 2a). The corresponding atmospheric methane concentrations reached 2.10 ppm due to the net sea-to-air flux (Figure 2a). Increased ethane and propane along with elevated salinity and decreased temperature (Figures 2b–2d) suggest that the elevated methane in the surface seawater may be associated with upwelling of hydrocarbon enriched waters. A similar feature in the surface seawater was observed in the same region in June 2010 during the Persistent Localized Underwater Methane Emission Study (PLUMES) [Yvon-Lewis et al., 2011].
Table 1. Mean Atmospheric Methane Mixing Ratios, Seawater Methane Concentrations, Saturation Anomalies and Net Sea-to-Air Fluxes of Methane at the Three Seep Sitesa
W92 refers to the flux calculated using the Wanninkhof  gas transfer velocity parameterization.
S07 refers to the flux calculated using the Sweeney et al.  gas transfer velocity parameterization.
 The methane saturation anomaly is defined as the percent difference between the partial pressures of methane in surface seawater and air. They ranged from −51.8% to 7.43 × 103% (Figure 2f). The calculated net sea-to-air fluxes ranged from −4.68 to 416μmol m−2 d−1 (Figure 2f). The mean net sea-to-air flux at each of the three seep areas was 12.8 (MC118), 4.67 (GC600) and 1.07μmol m−2 d−1 (GC185) (Table 1). To compare the results from this study to those from previous studies, we calculated the flux using the gas transfer velocity from Wanninkhof  in addition to using the Sweeney et al. relationship described earlier. The calculated net sea-to-air methane fluxes from the deepwater hydrocarbon plume areas are 1–2 orders of magnitude lower than those from shallow water seep plume areas (Table 2) [Mau et al., 2007; Schmale et al., 2005]. For the deep water environment, the calculated fluxes from this study are in the same range as those determined from most previous studies (Table 2) [Reeburgh et al., 1991; Schmale et al., 2005; Yoshida et al., 2004; Yvon-Lewis et al., 2011]. However, they are three orders of magnitude lower than those reported by Solomon et al.  who investigated the same region as the current study including one of the same identified seep sites.
Table 2. Diffusive Net Sea-to-Air Fluxes of Methane From Different Marine Environments
 Based on the results above, four main issues will be addressed in the following discussion: (1) the source for the elevated atmospheric methane during the transit from GC600 to GC185; (2) the diffusive net sea-to-air fluxes of methane over three seep sites and the extrapolated total fluxes of methane over the deepwater seep area in the northern Gulf of Mexico; (3) potential causes for the large discrepancy between the results from this study and those reported bySolomon et al. ; and (4) the impact of small areas of high methane concentration hotspots on our regional air-sea flux estimate if extremely high concentrations existed in the surface seawater over a deepwater hydrocarbon plume area and were missed in this study.
4.1. Elevated Atmospheric Methane
 An area of elevated atmospheric methane with a maximum concentration of 4.01 ppm was observed on YD 197 (16 July) at GC600 (Figure 2a). The elevated atmospheric methane persisted for 19 h and extended over 50 km to the northwest of GC600 during the transit to GC185 (Figure 2a). Coincident elevated ethane and propane in the atmosphere suggest a thermogenic gas contribution (Figures 2b and 2c). The 24 h air-mass back-trajectories obtained from the NOAA Air Resources Laboratory (http://ready.arl.noaa.gov/HYSPLIT_traj.php) show that the air masses with increased atmospheric methane came from the same region as those with background concentrations of 1.81 ppm (Figure 3), suggesting a localized source rather than long-range transport. Since the methane concentrations in the underlying seawater were close to a seawater background concentration of 2.40 nmol L−1 (Figure 2a), methane transport via diffusive sea-to-air gas exchange is not the source of these high atmospheric concentrations.
 Although bubbles traveling over 1000 m from a deepwater seep site have been observed [Greinert et al., 2006], whether or not they can reach the surface is still debated [McGinnis et al., 2006; Rehder et al., 2009]. In this study, to increase the atmospheric methane concentration to 4.01 ppm (3.25 ppm averaged over the area with elevated methane concentrations), there would need to be 3 × 105 mol d−1 of methane released to the atmosphere assuming a marine boundary layer height of 700 m (data from http://ready.arl.noaa.gov/READYamet.php) and assuming that the elevated methane only spread out in a circle 100 m in diameter centered on the ship as it moved along the cruise track. It is not likely for direct methane transport via gas bubbles at GC600 to contribute such a large amount of methane to the atmosphere due to the strong pycnocline during the summer (Figure 4) and the 1200 m water depth at this site. While slicks were observed from the ship at this site along with intermittent oil droplets rising to the surface, surface water concentrations were 2.85 ± 0.73 (1σ) nmol L−1, suggesting that these droplets were not carrying high concentrations of methane. Since the observation of the elevated atmospheric methane to the northwest of GC600 does coincide with satellite data from 20 July showing very extensive oil slicks over this broad region of the Gulf, we could not completely exclude the possibility that methane could be transported inside of the oily bubbles to the atmosphere. However, we cannot provide an appropriate mechanism for this possibility.
 Fugitive release to the atmosphere directly from oil platforms around GC600 is possible (Figure 3). Given the fact that no significantly elevated atmospheric methane concentrations were observed near the recovery ships during the Deepwater Horizon oil spill, which were flaring tremendous amounts of gas [Yvon-Lewis et al., 2011], flaring itself is an unlikely source of methane to the atmosphere. Not flaring or accidentally releasing gas from the drilling oil platform during this time is not likely to be the explanation either based on the drilling records from the Drilling Rig OCEAN MONARCH (the rig close to GC600). A likely explanation could be an undetected leak from one or more of the nearby oil platforms.
4.2. Methane Net Sea-to-Air Fluxes Over the Seep Area in the Northern Gulf of Mexico
 High spatial variability was observed in sea surface methane and net sea-to-air fluxes over the three seep areas (Figures 5 and 6). Overall, MC118 had higher sea surface methane concentrations and higher net sea-to-air fluxes than either GC600 or GC185 (Tables 1 and 3 and Figures 5 and 6). GC600 is the oiliest site surveyed during this study. Although surfactants can inhibit bubble dissolution and enhance the methane transport, lower surface seawater methane concentrations and lower diffusive fluxes were observed than those at MC118. GC185 is the shallowest site occupied during this study. During a prior study at this site, a methane concentration of 608 nmol L−1at a water depth of ∼20 m was reported and used to determine a net sea-to-air flux of 3420μmol m−2 d−1 in the plume area [Solomon et al., 2009]. Therefore, higher methane concentrations in the air and sea surface as well as higher fluxes were anticipated. However, both the atmospheric methane and the sea surface (4 mbsl) methane were near background (Table 1). Spatial variability between sites is associated with characteristics of their geological and physical environment, e.g., seep intensity, oil-water ratio, water depth, currents, and mixed layer depth. Spatial variability within one seep site (Figure 5) is related with the rising angle of the bubbles and the directions of mid-depth and surface currents. High temporal variability within one seep site was also observed during our surface survey (Figures 2 and 6). The magnitudes of the fluxes and the elevated flux areal extent vary from day to day (Table 3 and Figure 6). The temporal variability of methane fluxes could be due to changes in seepage rates, currents, wind speeds, surface wave action, etc. [Clark et al., 2003, 2010; Greinert et al., 2006; Leifer and Boles, 2005; Leifer et al., 2006; Quigley et al., 1999].
Table 3. Mass Fluxes Over the Survey Area Using Different Interpolation Gridding Methodsa
Survey Area (km2)
Area With Fluxes ≥8 μmol m−2 d−1 (km2)
Inverse Distance Weighted
Area Weighted Mean Flux (μmol m−2 d−1)
Mass Flux (mol d−1)
Area Weighted Mean Flux (μmol m−2 d−1)
Mass Flux (mol d−1)
Area Weighted Mean Flux (μmol m−2 d−1)
Mass Flux (mol d−1)
The boundaries for the gridded fluxes are shown in Figure 6.
 The daily methane mass flux distribution for each survey area was determined by interpolation using natural neighbor, inverse distance weighted interpolation, and krigging (Table 3). The three different interpolation methods do not produce significantly different fluxes. Since the natural neighbor method produced a smoother shape, we chose this algorithm as our main interpolation method for plotting the mass flux distribution over the seep sites. Due to the high temporal and spatial variability of the methane fluxes within and between sites, it is difficult to extrapolate the observed net sea-to-air fluxes to other periods or to other hydrocarbon seeps (Figures 5 and 6). However, we can approximate the upper limit of the diffusive net sea-to-air flux of methane from the deepwater hydrocarbon seeps in the northern Gulf of Mexico under normal conditions (i.e., no mud volcanoes or submarine earthquake) by assigning the highest daily flux determined in this study, 300 mol d−1 (per seep site), to other deepwater hydrocarbon seeps in this region. Large uncertainty exists in the number of active seeps in the northern Gulf of Mexico. Geophysical anomalies generated by seeps in the geologic past exceed 5000 possible sites [Frye, 2008] whereas preliminary results for seeps detected by remote sensing (see the detailed method by Garcia-Pineda et al. ) suggest a maximum number of active vents about 1500. Assuming that each of the 1500–5000 seeps in the northern Gulf of Mexico has daily net sea-to-air flux of 300 mol d−1and they persistently emit methane to the atmosphere at the same rate over a one-year period, the total diffusive net sea-to-air flux from deepwater hydrocarbon seeps in the northern Gulf of Mexico is about 3–9 Gg yr−1. Compared with the total annual emission of methane to the atmosphere, 5.8 × 105 Gg yr−1 [Denman et al., 2007], the contribution of the net diffusive sea-to-air flux from deepwater hydrocarbon seeps in the northern Gulf of Mexico is insignificant to the atmospheric methane budget.
4.3. Explanation for Flux Discrepancy
 The three orders of magnitude methane flux discrepancy between this study and that reported by Solomon et al.  is mainly attributable to the surface seawater methane values used in the flux equation (equation (9)). The “surface” seawater methane concentrations reported by Solomon et al.  were in the range of 57.1–1609 nmol L−1 while the methane concentrations in this study ranged from 1.72 to 23.5 nmol L−1. Although we cannot exclude the possibility of temporal variability, we can evaluate the methodological differences between these two studies. How each study defines a surface sampling depth is a key factor that bears consideration. In the present study, seawater was continuously sampled from ∼4 m water depth within the mixed layer as the ship was moving. Mean mixed layer depths were 4.8 m (0–28.8 m; median: 3.5 m; 32 CTD casts) at MC118, 4.9 m (4.2–5.5 m; 2 CTD casts) at GC 600, and 2.1 m (1.4–2.6 m; 3 CTD casts) at GC185 (Figure 4). When determining the air-sea flux using the air-sea concentration gradient, the dissolved concentrations must be measured as close to the surface as possible. By contrast, the shallowest sample collected bySolomon et al.  was around 20 m. Their temperature and salinity profiles (see supplementary materials of Solomon et al. ) do not display a mixed layer depth below 20 m. Therefore, the surface water value they used to calculate methane fluxes were not diagnostic of true surface water values.
 A contributing but minor factor to the differences in net sea-to-air fluxes reported in the two studies involves the atmospheric methane concentrations used in the flux calculation.Solomon et al.  used an averaged atmospheric methane concentration for their flux calculations, while the atmospheric mixing ratios were measured once every 12 min locally during the current study. Atmospheric methane ranged from 1.70 to 4.01 ppm over the seep sites during the current study. At times, the atmospheric methane concentrations were over twice the average background concentration. In some places during the occupation of GC600, the surface ocean acted as a sink for atmospheric methane and would have been misinterpreted as a source to the atmosphere if average atmospheric methane concentrations were used in the flux calculations. Fluxes of methane from the ocean to the atmosphere or other incidental hydrocarbon emissions could result in perturbations to the local atmospheric methane concentrations, and these perturbations should be accounted for in the calculation of the flux.
4.4. Impact of Small Area High Concentration Hotspots on the Regional Air-Sea Flux
 To determine if the regional air-sea flux results from continuous air-sea measurements are more representative than discrete measurements, we investigate whether the technique used in this study could have missed a high methane concentration hotspot that is large enough to impact the overall flux from the plume area. To address this possibility, the sensitivity of the corrected seawater concentration (Cw) to the size and concentration of a potential hotspot is determined using equation (7). We assumed (1) that any corrected seawater concentration ≥4 nmol L−1 (twice the background concentration) indicated an observable hotspot and (2) that the ship left a background concentration of 2 nmol L−1 and immediately crossed a methane hotspot with a concentration ranging from 4 to 1609 nmol L−1 (the highest 20 m value reported by Solomon et al. ). Under these conditions, a surface hotspot with a concentration of 1609 nmol L−1 is observable for a hotspot with a diameter ≥2 m when the ship speed is 4 knots (e.g., when the ship is conducting coarse surveys) (Figures 7a and 7c), and a diameter ≥5 cm when the ship speed is 0.1 knots (e.g., when the ship was holding a station) (Figures 7b and 7d). As the concentration of the hotspot decreases, the hotspot size required for unequivocal detection would exponentially increase (Figure 7).
 Since the corrected seawater concentration (Cw) is close to an average concentration over 12 min (see equation (7)), it averages out the high and low seawater concentrations. Here, we will assess the possible impact of missed hotspots along the survey track. Assuming the three seep sites only contain hotspots with methane concentrations of 1609 nmol L−1 and waters with background concentrations of 2 nmol L−1, the possible sizes of the missed hotspots can be determined by equation (7) using the actual ship speeds and the observed concentrations. The area of each possible missed hotspot ranges from 5.2 × 10−4 m2 to 77 m2 and the total area of missed hotpots in each of the three plume areas is 181–930 m2 (MC118), 51 m2 (GC600) and 20 m2 (GC185), corresponding to fluxes of 0.80–5.16 mol d−1 (MC118), 0.24 mol d−1 (GC600) and 0.05 mol d−1 (GC185) (Table 4). The mean flux over each plume area resulting from hotspots that might have been missed using the current survey technique accounts for only 1.7% (MC118), 0.5% (GC600) and 0.7% (GC185) of the integrated regional flux (Table 4).
Table 4. The Integrated Net Mass Flux of Methane From Each Survey Area Each Day and the Total Potential Mass Flux From Hotspots at Those Sites
The total methane flux from hotspots assuming relatively small areas of hotspots exist on the survey tracks.
0.930 × 10−3
0.238 × 10−3
0.444 × 10−3
0.181 × 10−3
0.597 × 10−3
0.181 × 10−3
0.051 × 10−3
0.020 × 10−3
 Another potential limitation of the survey technique used in this study is the possibility that hotspots between the survey tracks were never sampled. Since the extremely high surface water methane concentrations reported by Solomon et al.  were from GC185, we use this site to investigate the impact of missed hotspots between the survey tracks. Assuming that either the missed hotspots or our sampling pattern were randomly distributed throughout the survey area, we estimate the probability that a hotspot was completely missed. For each surface water measurement, the probability (P) that a hotspot was missed is calculated as a function of the total integrated hotspot area (Ah) and the total survey area (A; 6.686 km2) of GC185
Since we sampled 71 times, the probability that the hotspot was completely missed on all 71 measurements is P71. This calculation clearly shows that as the area of the hotspot increases, the probability that it was missed rapidly decreases (Figure 8). While there is an increased probability that a relatively small total integrated hotspot area was missed, this relatively small area leads to a relatively small flux from hotspots. Interestingly, even if we assume a background flux of 50 times the observed value for GC185, a total integrated hotspot area of only 1.92% of the survey area is necessary to produce a daily flux similar to our “background” observations. And for a hotspot area of 1.92%, there is only a 25% chance that hotspots covering this total integrated area were missed during our sampling campaign.
 Elevated methane concentrations in surface seawater were observed, and elevated net sea-to-air methane fluxes were determined at three seep sites (MC118, GC 600 and GC185) in the northern Gulf of Mexico. The net sea-to-air methane fluxes ranged from −4.19 to 86.1μmol m−2 d−1over the deepwater hydrocarbon plume areas, agreeing with most previous studies. Variations in the atmospheric methane concentrations suggest the need for measuring atmospheric methane concentration when assessing the net sea-to-air fluxes. High temporal and spatial variability in the methane fluxes was observed over the three seep areas. Extrapolating the highest flux from this study to other deepwater hydrocarbon seeps in the northern Gulf of Mexico suggests that diffusive net sea-to-air fluxes from deepwater hydrocarbon seeps in the northern Gulf of Mexico is an insignificant source to atmospheric methane. However, the elevated air concentrations on GC600 require about 3 × 105 mol d−1 of methane released in this area. This tremendous methane source could not be characterized during this study.
 Three orders of magnitude of discrepancy exist between the results from this study and those reported by Solomon et al. for the estimation of the diffusive net sea-to-air flux of methane from deepwater hydrocarbon seeps in the northern Gulf of Mexico. The large discrepancy between these two studies is mainly attributed to the different concentrations observed and the depths of those concentrations. The concentrations reported here are all from within or close to the surface mixed layer and appropriate for use in air-sea flux calculations. However, assuming that extremely high methane concentrations existed as relatively small hotspots in the surface seawater over deepwater hydrocarbon seep area, the impact of those hotspots on the regional diffusive air-sea flux would be small.
 The data reported here are available from the authors and will be submitted to the Marine Methane and Nitrous Oxide (MEMENTO) database. Information on accessing this database can be found at http://www.bodc.ac.uk/solas_integration/implementation_products/group3/. This work was supported by the Department of Energy (National Nuclear Security Administration) National Energy Technology Laboratory under Award Number DE-NT0005638. We thank TDI Brooks, the crew of R/VBrooks McCall and our colleagues in the HYFLUX project for all of their help. We are grateful for the constructive and helpful comments from two reviewers, especially from the reviewer one. This report was prepared as an account of work sponsored by an agency of the United States Government. Neither the United States Government nor any agency thereof, nor any of their employees, makes any warranty, express or implied, or assumes any legal liability or responsibility for the accuracy, completeness, or usefulness of any information, apparatus, product, or process disclosed, or represents that its use would not infringe privately owned rights. Reference herein to any specific commercial product, process, or service by trade name, trademark, manufacturer, or otherwise does not necessarily constitute or imply endorsement, recommendation, or favoring by the United States Government or any agency thereof. The views and opinions of authors herein do not necessarily state or reflect those of the United States Government or any agency thereof.