High speeds have been measured at seep and mud-volcano sites expelling methane-rich fluids from the seabed. Thermal or solute-driven convection alone cannot explain such high velocities in low-permeability sediments. Here we demonstrate that in addition to buoyancy, osmotic effects generated by the adsorption of methane onto the sediments can create large overpressures, capable of recirculating seawater from the seafloor to depth in the sediment layer, then expelling it upwards at rates of up to a few hundreds of metres per year. In the presence of global warming, such deep recirculation of seawater can accelerate the melting of methane hydrates at depth from timescales of millennia to just decades, and can drastically increase the rate of release of methane into the hydrosphere and perhaps the atmosphere.
Methane is of great environmental importance as a greenhouse gas, and marine seeps are estimated to contribute some 37% of the geological sources; likewise mud volcanism provides another 11–17% (ref. 1). Methane hydrates are often found in the vicinity of submarine seeps and mud volcanoes2, and the project of commercializing this energy source is under way. Concomitantly, there is concern that anthropogenic climate change could destabilize hydrates, thereby potentially releasing large quantities of methane into the ocean and atmosphere3,4,5. Thus there are both environmental and economic reasons to be interested in methane associated with seeps and mud volcanism.
A mud volcano is a geological structure on land or in the oceans in which water plus fine particulates—‘mud’—issues from a conduit typically topped by a conical hill with a crater. The emerging mud is generally accompanied by methane, both dissolved and, if the concentration exceeds the saturation concentration, as bubbles6. A submarine seep, on the other hand, has similar fluid flow through the porous sediment constituting the seabed without the conical structure or open conduit. What physical forces drive such fluid flows?
We find that both buoyancy and osmotic effects are present in cold seeps and mud volcanism in which, rather than being a passive element, methane is its driving force. Some researchers have suggested the importance of considering osmosis in seeps and mud volcanism7,8. Clays and shales are known to possess the semipermeability necessary for osmosis, associated with charge and pore-size effects9,10. Moreover, methane hydrates frequently exist in the sediments around a cold seep or mud volcano2,6. As hydrate forms, the sediment plus hydrate becomes progressively less permeable11,12. However, other mechanisms involving adsorption and chemical reaction can also produce significant osmotic pressures13,14,15,16,17,18,19,20. Methane is shown to adsorb onto sediments21,22,23,24. Hydrates form in pores under a wider range of conditions than in the bulk25 and methane molecules adsorb onto the cages of methane hydrate during the hydrate growth process26,27. Thus, we propose below that given a supply of methane, a submarine cold seep or mud volcano can function as a geological instance of an osmotic pump9,28,29. We find cause for concern that this convective pump mechanism facilitates methane hydrate destabilization under anthropogenic climate change.
Liquid flow mechanisms in seeps and mud volcanoes
Consider the possible physical driving forces for a submarine seep in which salty water and methane are driven out of the seabed (Fig. 1). The origin for this water can be either a reservoir beneath the seabed or seawater itself, recirculated within the porous seabed.
One commonly discussed flow mechanism is the expulsion of pore water from sediments under compression, which can yield a speed of some vsc=1.8 × 10−3 m yr−1 (ref. 30). This estimate provides a baseline with which to compare mechanisms. Buoyancy and osmotic forces are other possible driving mechanisms. Let us consider quantitatively the processes for fluid transport in a cold seep in which the sea bed consists of a homogeneous porous medium, within which, at a given depth beneath the seafloor, we position (Fig. 1a) an extended source of buoyancy, caused by either a thermal or a compositional difference, or (Fig. 1b) a two-dimensional source of buoyancy, such as that at a continental margin. Much previous work has explored the occurrence of flow focussing in overpressured heterogeneous sediments31,32. We further consider the case (Fig. 1c) in which the sediment is heterogeneous, so that focussed flow may occur above a source of buoyancy or osmotic effects; for example, methane dissolved in warm water, the porous medium being semipermeable to this methane. We estimate the rate of flow of water induced in each case. We should mention that there exists a further buoyancy-driven flow mechanism, that of liquid flow driven by buoyant bubbles33, but this becomes dominant only with very large gas fluxes; that is, during the eruptive phase of mud volcanism, while here we concentrate on flows during the quiescent phase that subsists ∼95% of the time6.
The effectiveness of each mechanism of pumping fluid depends of course on the permeability of the sediment. Measurements at seeps indicate values for inter-granular permeability in the range 10−18–10−14 m2 (ref. 34). However, it has been suggested34,35,36 that bulk permeabilities are much higher, of the order of 10−12 m2, owing to channelling of fluid through the sediment. Below we assume a bulk permeability k=10−12 m2 and later extend our results to the range of permeabilities 10−13–10−11 m2.
Positive buoyancy forces can arise from a temperature gradient that heats the water, or from solutal sources. For example, heat is released when methane hydrates form and lower-density fresh water is generated when hydrates dissociate (Fig. 1a). When buoyancy from a geological process is released over a large area at depth in an otherwise quiescent, saturated porous medium, the less-dense fluid rises above the source (Fig. 1a). In a homogeneous sediment, the upward flow is essentially one-dimensional and we estimate (Methods) flow speeds vest∼0.15 m yr−1 and vess∼0.75 m yr−1 for thermal and solutal convection, respectively.
Consider now the release of heat over a long, thin area such as a continental margin. The rise of the warm fluid is now more localized, forming a line or two-dimensional plume (transverse view in Fig. 1b). The plume increases in width as it rises, owing to viscous drag and to transverse heat conduction. The rise velocity of the warm fluid decreases with height as a consequence of cooling and the consequent reduction of buoyancy, while the volumetric flow rate increases on account of the increase in plume width. We consider a heat source of strength Ft=25 J m−1 s−1 at a depth H=100 m to be consistent with observations of surface heat fluxes of the order of 0.12 J m−2 s−1 measured at the northern Cascadia accretionary sedimentary prism37. The upward liquid speed at the seafloor is then estimated (Methods) as vlst=0.25 m yr−1, the half-width of the plume is blst=87 m and the total flow rate per unit length is Qlst=43 m2 yr−1.
A similar plume flow develops when less dense fluid is released in a localized region at depth, for example water liberated through methane hydrate dissociation38 or during the smectite-illite transformation39. In a given case, the chlorinity of interstitial pore water sampled at a seep site is about 0.95 times that of seawater34, suggesting dilution of low salinity water from depth with seawater by a factor of the order of 20. Also, heat balances over active seep areas taking into account measured background thermal gradients have suggested dilution of the original water from depth with seawater by a factor of 6 to 30 (ref. 39). Constraining the plume flow here to a dilution factor of 20 allows us to estimate (Methods) the original source fluid flow rate Q0=0.16 m2 yr−1, so that the the total flow rate per unit length at the seafloor is Qlss=3.1 m2 yr−1. We estimate the plume speed vlss=0.13 m yr−1 and half-width blss=12 m. This source flow rate is consistent with values quoted for the release of water by the smectite-illite transformation and the hydrate layer39.
For comparison, consider now a buoyant flow in a heterogeneous porous medium under a seep (Fig. 1c). We assume focussed flow directly under the seep area has increased the local permeability so that the main resistance to flow arises in the drawing of seawater from the surroundings into the rising seep plume. For an array of seeps spaced at ∼50 m and radius bs=2 m (refs 2, 40), we predict (Methods) a vertical velocity of vss∼59 m yr−1, for a solutal source of buoyancy at depth H=100 m and a dilution ratio of 20. The total flow rate in the convective cell is Qss=7.4 × 102 m3 yr−1. The effluent flux of methane averaged over the inflow area is ∼0.0031, mol m−2 yr−1.
Osmotic forces arise from a compositional gradient of fluid within a medium possessing a degree of semipermeability. Let us consider the flow induced by the osmotic pressure gradient associated with a release of fresh water saturated with methane at depth in the same heterogeneous porous medium under a seep (Fig. 1c). The water at the seafloor, above and beyond the seep region, is free from methane owing to continuous motion of ocean currents. We expect seawater to flow downward from the seafloor into the porous sediment and towards the region with high concentration of methane. The methane in solution may diffuse into and through the surrounding seawater-saturated porous sediment. A mixture of the source freshwater with methane and seawater will eventually rise in the form of an osmotic plume, exiting at the seafloor as a seep flow. We predict (Methods) a vertical velocity of vso∼5.7 × 102 m yr−1 for an osmotic source at depth H=100 m and a dilution ratio of 20. The total flow rate in the convective cell is Qso=5.9 × 103 m3 yr−1. The effluent flux of methane averaged over the inflow area is ∼0.025 mol m−2 yr−1.
These scaling and numerical results suggest that liquid efflux from the seabed in seep regions driven by osmotic pumping can be at least 10 times larger than in seeps with convection induced by salinity and thermal differences. It is also far larger than reported velocities for water expulsion resulting from sediment compression.
Lastly, let us consider both buoyant and osmotic circulation in the vicinity of a fully developed mud volcano with a fractal network of smaller channels at depth leading to the main central conduit, like a tree roots and trunk, above a source of solute or/and heat. Consider an idealized version of the geometry of the conduits: a vertical main channel, through which water with dissolved methane flows upwards from side feeder channels at depth and exits at the seafloor (Fig. 1d). Here we consider the drawdown of water from the seabed caused by buoyant or osmotic pressure associated with a solute in solution in these conduits. Each conduit thus behaves like a buoyant or osmotic source considered above. Such network flows have been considered for many systems, from rivers in geology to the vascular system and the lungs in biology; our case corresponds to a directed spanning tree, the most efficient class of networks41. We find that the speed of the flow in the main conduit is proportional to the total lateral area of all the feeder conduits (Methods). The combination of a buoyant or osmotic pump and a very small volume fraction of conduits within the sediment produces flow rates orders of magnitude larger than that in a homogeneous porous medium alone.
Comparison with field measurements
The convective pump mechanism that we have demonstrated here functions as an amplifier of a small external source of buoyancy or dissolved methane into a large quantity of water that cycles through the seep or volcano. The question of the provenance of the water is a telling datum. The dominant contribution to the water issuing from submarine seeps and mud volcanoes is not water from reservoirs under the seafloor, but seawater42,43,44,45.
In Fig. 2, we present a comparison of in-situ measurements of liquid and methane fluxes from cold seeps30,46 and mud volcanoes47,48 with our theoretical predictions. It is clear that thermal and solutal convection alone cannot explain the very high velocities measured at methane-rich sites with low permeability sediments. Contrariwise, osmosis induced by methane is likely to be the physical mechanism responsible for some of these high velocities, as revealed by the orange shaded ellipse. Indeed, even with a conservative estimate of the osmotic effect, osmotic pressure gradients are capable of producing very fast flows. The fluids vented at these seep sites had concentrations of dissolved methane in the range 0.6–126 μM. Osmosis is an efficient mechanism for producing fast localized flows, owing to the relatively large pressure differences it generates. While for the buoyant seep considered above the pressure driving the convective cell is of the order of 4.4 × 103 Pa, in the osmotic seep a pressure of 19 × 103 Pa is achieved.
Fluid flow into the seabed in the vicinity of a seep has been observed; this flow pattern is difficult to understand from non-convective mechanisms. Measurements of downward speeds have been reported of 0.02–1.6 m yr−1 in the vicinity of methane vents in the Gulf of Mexico49 and of 0.1–0.5 m yr−1 in Hydrate Ridge, Cascadia40,50. These measurements may be compared with a predicted downward velocity at the seafloor surrounding the seep of ∼3.1 m yr−1 for the osmotic flow, but only 0.38 m yr−1 for the buoyant case, so the faster downward flows, at least, should be owing to osmosis.
Our prediction of localized venting driven by osmosis is consistent with observations of seep regions in the Gulf of Mexico involving cold and dense saline effluent, where buoyancy cannot drive the flow51,52,53.
There is at present just one measurement of flow rates in a mud volcano conduit, of 400 km yr−1 at a conduit of the Håkon Mosby mud volcano with radius 0.2 m (Mud volcano II (ref. 47); the other mud volcano measurement we plot, Mud volcano I (ref. 48), corresponds not to a conduit, but to flow through a porous medium, as at a seep). This conduit flow measurement is compatible with our theoretical estimate for a mud volcano that predicts that the exit speed in a main conduit will be increased in proportion to the total lateral area of the network of conduits. Given a tiny volume fraction of 0.00001% of the porous medium forming feeder conduits for a main conduit, we predict such high-speed flows can be driven by either buoyancy or osmosis. This is a measure of how much more efficient than a seep a mud volcano is at pumping seawater.
Our model shows that recirculation of seawater within the seabed is rather greater and deeper than previously understood. While earlier models have considered convection of seawater in shallow layers of sediment of only a few metres depth34,38,39, here we have deduced that convection can extend to the depth of the source of buoyancy or dissolved methane. Such flow can cool the sediment column by up to 1.3 × 107 J m−2 yr−1 per unit temperature difference between the seawater and the seep effluent. Measurements of outflow temperatures at seeps indicate a temperature elevated by 0–5 K relative to seawater2. So we predict a maximum heat flux of ∼6 × 107 J m−2 yr−1 associated with convection in the sediment. We, therefore, envisage that recirculation of seawater to hundreds of metres depth will be problematic under conditions of climatic warming, as buried methane hydrates below seep and mud-volcano sites will be much more susceptible to destabilization than has been recognized up to now.
Previous studies have estimated a timescale of millennia for conduction of heat from warmer seawater at the seafloor to affect the base of a hydrate layer at a few hundred metres depth and promote melting3,4,5. However, under enhanced heat transport by both buoyant and osmotic convection, we predict that the melting of hydrates could begin within timescales as short as 30 years. Such accelerated heat transport by convection will also increase the rate of melting of some hydrates by a factor of up to 100 compared with the heat conduction scenario previously studied (see Methods). The release of methane to the hydrosphere may thus occur much sooner and faster than previously thought. Such a continuous intense release of methane at the seabed will form a plume of rising methane bubbles that may reach the upper water column47,54,55.
It is challenging to assess what portion of the global inventory of methane hydrate, estimated as 1.8 × 103 Gt C (ref. 56), might be susceptible to warming by the mechanism described here. For this, we need to combine oceanographic predictions for the warming of the upper few hundred metres of the ocean with hydrate stability studies. It is thought57 that marine deepwaters on upper continental slopes (up to a few hundred metres depth), at the edge of the gas hydrate stability zone, encompass some 3.5% of the global hydrate inventory. It is also known4 that shallow waters down to a few hundreds of metres respond to climate change in roughly 10 years, while deep waters at 1–3 km take longer, 100–1000 years. Based on these estimates, a maximum of about 3.5% of the global hydrate inventory (∼60 Gt C) might be susceptible to warming by the mechanism proposed here within a timescale of a few decades.
The subscripts es, lst, lss, so and ss denote an extended source of buoyancy, a thermal margin plume, a solutal margin plume, a seep driven by osmosis and a seep driven by buoyancy, respectively. The subscripts ‘single’ and ‘network’ refer to a single conduit and a network of conduits in a mud volcano.
Uniform flow above an extended buoyancy source
A buoyancy-viscosity balance suggests a velocity driven by the density difference between the surroundings and the less dense liquid Δρ. For a thermally driven flow Δρ=ρβtΔT=2 kg m−3 for a temperature difference ΔT=10 K (ref. 37) and ρ=103 kg m−3. For a solutal source of buoyancy, the maximum density difference driving the flow can be estimated to be smaller than Δρ=10 kg m−3 taking into account salinity differences34 and heat absorbed during methane hydrate dissociation. For the properties of water, we take the thermal expansion coefficient βt=2 × 10−4 K−1 and the viscosity μ=1.8 × 10−3 kg m−1 s−1.
Thermal margin plume
The vertical velocity at the centreline of a plume at a distance H above the source is vlst≈(kβtgFt/(μCp))2/3(3/(32κmH))1/3 and the plume half-width is blst≈(48μCpH2/(kβtgFt))1/3 (ref. 58). The thermal diffusion coefficient of the saturated sediment is κm=10−7 m2 s−1; g is the acceleration of gravity. The specific heat capacity of water is Cp=4.2 × 103 J kg−1 K−1.
Solutal margin plume
The plume velocity is vlss≈(kΔρgQ0/μ)2/3(3/(32DsH))1/3 and the plume half-width is blss≈(48μH2/(kΔρgQ0))1/3. We take the effective diffusivity of the solute causing the density difference, for example, salt, in the porous medium as Ds=10−9 m2 s−1, and Δρ=10 kg m−3 as before.
Pumping in a seep
For pumping driven by osmosis, the porous medium behaves as only partially permeable to methane because a fraction of methane molecules of up to 0.6 are adsorbed22,30 and later released by the sediment. This adsorption creates a change of momentum in the methane molecules that leads to a reflection coefficient of σ0<0.6 (refs 17, 19, 22, 59). For the pressure and temperature conditions in the seep data in Fig. 2, the solubility of methane in water is in the range c0∼0.10–0.23 M (ref. 60); we consider an intermediate value c0=0.156 M. A conservative estimate for the contribution of methane to osmosis is, therefore, σ0c0=0.008 M, assuming that ∼5% of methane-molecule collisions with the sediment result in adsorption and later desorption21,23,24. Seawater of course contains another solute, sodium chloride (other solutes found in seep water have much lower concentrations44,45); we may neglect the osmotic effect of sodium and chloride ions because size-restriction effects in the sediment are very small for the permeabilities considered here9,28. The semipermeability of the sediment to methane creates an osmotic pressure difference between the seawater and the methane-rich fluid released at depth of p0=σ0c0RT; here, R is the universal gas constant and T∼283 K is the temperature. A balance of osmotic and viscous forces gives the scale for the flow rate of seawater drawn into the osmotic plume . This flow will be channelled upwards towards the seafloor in a plume within the high permeability sediment column below the seep. Consistent with seafloor observations, we assume a radius of a=2 m for this column2,40. The vertical velocity in the plume is . Numerical simulations neglecting the resistance in the upward flow compared with the downward and radial flow confirm this scaling, with a coefficient of 1.4 for seeps spaced at 50 m and a dilution ratio of the original source fluid of 20. We estimate a vertical effluent speed vso∼4.7 × 102 m yr−1. The vertical downward speed at the seafloor surrounding the seep is of the order of uso=3.1 m yr−1.
For pumping driven by buoyancy, the pressure difference between the seawater and the hot or fresh fluid released at depth is p0=ΔρgH. A balance of buoyancy and viscous forces gives the scale for the flow rate of seawater drawn into the buoyant plume . Numerical simulations neglecting the resistance in the upward flow compared with the downward and radial flow confirm this scaling, with a coefficient of 0.35 for seeps spaced at 50 m and a dilution ratio of the original source fluid of 20. We estimate a vertical effluent speed vss∼59 m yr−1. The vertical downward speed at the seafloor surrounding the seep is of the order of uss=0.38 m yr−1.
Pumping in a mud volcano
A similar balance of buoyant/osmotic and viscous forces applies as for a seep, with the plume radius a replaced by the conduit radius, Rc. Thus, for a single vertical conduit, the effluent speed is to leading order independent of the conduit length. For a network of conduits, with the simplifying assumptions that one conduit domain has no impact on the others and the viscous resistance to flow in the network is small compared with that in the porous medium, the flow rate is proportional to the sum of the lateral surface areas Ai of all the individual conduits; the exit velocity in the main conduit is then vnetwork=vsingle Ai/Asingle. The exit speed thus depends on lengths and radii of the feeder conduits extending about the main conduit. For a single vertical conduit of radius Rc=0.2 m, we predict a maximum speed of vsingle∼3 × 103 m yr−1. vnetwork can be several orders of magnitude larger than this: to achieve a hundredfold increase to vnetwork∼3 × 105 m yr−1, for example, the lateral surface area of conduits needed is m2, for H=103 m and Rc=0.2 m. Assuming feeder-conduit radii rc∼0.01 m, the corresponding volume of these conduits is ∼100 m3. The recirculation volume of the porous medium is ∼103 × (103)2=109 m3. So, a hundredfold increase in the exit speed requires just a fraction of 10−7 of the recirculation volume of the porous medium to be conduits.
Propagation of a thermal signal from the seafloor
The time of travel of a thermal signal from the seafloor to the base of the hydrate layer (where melting occurs) is approximately given by H/u, where H is the distance from the seafloor to the base of the hydrate layer and u is the superficial or Darcy vertical speed of the seawater moving downward in the sediment surrounding the seep or mud volcano. u was estimated from the scaling expressions above and confirmed by numerical simulation.
The ratio of the heat flux associated with convection of seawater downward into the sediment and that associated with conduction is the Péclet number Pe=uH/κ. We find Pe∼100 for the osmotic seep.
Data availability statement
The authors declare that the data supporting the findings of this study are available within the article.
How to cite this article: Cardoso, S. S. S. & Cartwright, J. H. E. Increased methane emissions from deep osmotic and buoyant convection beneath submarine seeps as climate warms. Nat. Commun. 7, 13266 doi: 10.1038/ncomms13266 (2016).
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Ciais, P. et al. in Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change (eds Stocker T. F.et al. Cambridge University Press (2013).
Judd, A. & Hovland, M. Seabed Fluid Flow Cambridge University Press (2007).
Buffett, B. Clathrate hydrates. Annu. Rev. Earth Planet. Sci. 28, 477–507 (2000).
Archer, D. Methane hydrate stability and anthropogenic climate change. Biogeosciences 4, 521–544 (2007).
Archer, D., Buffett, B. & Brovkinc, V. Ocean methane hydrates as a slow tipping point in the global carbon cycle. Proc. Natl Acad. Sci. USA 106, 20596–20601 (2009).
Kopf, A. J. Significance of mud volcanism. Rev. Geophys. 40, 1005 (2002).
Soloviev, V. A. & Ginsburg, G. D. Water segregation in the course of gas hydrate formation and accumulation in submarine gas-seepage fields. Marine Geol. 137, 59–68 (1997).
Ginsburg, G. D. & Soloviev, V. A. Methane migration within the submarine gas-hydrate stability zone under deep-water conditions. Marine Geol. 137, 49–57 (1997).
Neuzil, C. E. Osmotic generation of ‘anomalous’ fluid pressures in geological environments. Nature 403, 182–184 (2000).
Malusis, M. A., Shackelford, C. D. & Olsen, H. W. Flow and transport through clay membrane barriers. Eng. Geol. 70, 235–248 (2003).
Seol, Y. & Kneafsey, T. J. Methane hydrate induced permeability modification for multiphase flow in unsaturated porous media. J. Geophys. Res. Solid Earth 116, B08102 (2011).
Konno, Y. et al. Permeability of sediment cores from methane hydrate deposit in the Eastern Nankai Trough. Mar. Petrol. Geol. 66, 487–495 (2015).
Lee, C. et al. Osmotic flow through fully permeable nanochannels. Phys. Rev. Lett. 112, 244501 (2014).
Derjaguin, B. V., Dukhin, S. S. & Koptelova, M. M. Capillary osmosis through porous partitions and properties of boundary layers of solutions. J. Colloid Interface Sci. 38, 584–595 (1972).
Derjaguin, B. V., Dzyaloshinskij, J. E., Koptelova, M. M. & Pitaevsky, L. P. Molecular-surface forces in binary solutions. Disc. Farad. Soc. 40, 246–252 (1965).
Manassero, M. & Dominijanni, A. Modelling the osmosis effect on solute migration through porous media. Geotechnique 53, 481–492 (2003).
Biesheuvel, P. M. Statistical-mechanical theory of membranes transport. J. Colloid Interface Sci. 355, 389 (2011).
Malusis, M. A., Shackelford, C. D. & Manevalc, J. E. Critical review of coupled flux formulations for clay membranes based on nonequilibrium thermodynamics. J. Contam. Hydrol. 138–139, 40–59 (2012).
Cardoso, S. S. S. & Cartwright, J. H. E. Dynamics of osmosis in a porous medium. Roy. Soc. Open Sci. 1, 140352 (2014).
Córdova-Figueroa, U. M. & Brady, J. F. Osmotic propulsion: The osmotic motor. Phys. Rev. Lett. 100, 158303 (2008).
Sugimoto, A., Dan, J., Kumai, T. & Murase, J. Adsorption as a methane storage process in natural lake sediment. Geophys. Res. Lett. 30, 2080 (2003).
Ertefai, T. F. et al. The biogeochemistry of sorbed methane in marine sediments. Geochim. Cosmochim. Acta 74, 6033–6048 (2010).
Ji, L., Zhang, T., Milliken, K. L., Qu, J. & Zhang, X. Experimental investigation of main controls to methane adsorption in clay-rich rocks. Appl. Geochem. 27, 2533–2545 (2012).
Rexer, T. F., Benham, M. J., Aplin, A. C. & Thomas, K. M. Methane adsorption on shale under simulated geological temperature and pressure conditions. Energy Fuels 27, 3099–3109 (2013).
Casco, M. E. et al. Methane hydrate formation in confined nanospace can surpass nature. Nat. Commun. 6, 6432 (2015).
Guo, G.-J., Li, M., Zhang, Y.-G. & Wu, C.-H. Why can water cages adsorb aqueous methane? a potential of mean force calculation on hydrate nucleation mechanisms. Phys. Chem. Chem. Phys. 11, 10427–10437 (2009).
Zhong, D.-L., Sun, D.-J., Lu, Y.-Y., Yan, J. & Wang, J.-L. Adsorption-hydrate hybrid process for methane separation from a CH4/N2/O2 gas mixture using pulverized coal particles. Indust. Eng. Chem. Res. 53, 15738–15746 (2014).
Noy, D., Horseman, S., Harrington, J., Bossart, P. & Fisch, H. in Mont Terri Project—Hydrogeological Synthesis, Osmotic Flow. Reports of the Federal Office for Water and Geology, Geology Series (6) (ed. Heitzmann P. 95–126Federal Office for the Environment (2004).
Barge, L. M. et al. From chemical gardens to chemobrionics. Chem. Rev. 115, 8652–8703 (2015).
Linke, P. et al. In situ measurement of fluid flow from cold seeps at active continental margins. Deep-Sea Res. 41, 721–739 (1994).
Flemings, P. B., Stump, B. B. & Zoback, T. F. M. Flow focussing in overpressured sandstones: theory, observations and applications. Amer. J. Sci. 399, 827–855 (2002).
Reilly, M. J. & Flemings, P. B. Deep pore pressures and seafloor venting in the Auger Basin, Gulf of Mexico. Basin Res. 22, 380–397 (2010).
O’Hara, S. C. M. et al. Gas seep induced interstitial water circulation: observations and environmental implications. Continental Shelf Res. 15, 931–948 (1995).
Henry, P. et al. Interpretation of temperature measurements from the Kaiko-Nankai cruise: Modeling of fluid flow in clam colonies. Earth Planet. Sci. Lett. 109, 355–371 (1992).
Giambalvo, E. R., Fisher, A. T., Martin, J. T., Darty, L. & Lowell, R. P. Origin of elevated sediment permeability in a hydrothermal seepage zone, eastern flank of the Juan de Fuca ridge, and implications for transport of fluid and heat. J. Geophys. Res. Solid Earth 105, 913–928 (2000).
Saffer, D. M. The permeability of active subduction plate boundary faults. Geofluids 15, 193–215 (2015).
Davis, E. E. & Hyndman, R. D. Rates of fluid expulsion across the northern Cascadia accretionary prism: Constraints from new heat flow and multichannel seismic reflection data. J. Geophys. Res. 95, 8869–8889 (1990).
Henry, P. et al. Fluid flow in and around a mud volcano field seaward of the Barbados accretionary wedge: results from Manon cruise. J. Geophys. Res. 101, 20297–20323 (1996).
Pichon, X. L. & Henry, P. The Kaiko-Nankai Scientific Crew. Water budgets in accretionary wedges: a comparison. Phil. Trans. R. Soc. Lond. A 335, 315–330 (1991).
Tryon, M. D. et al. Measurements of transience and downward fluid flow near episodic methane gas vents, Hydrate Ridge, Cascadia. Geology 27, 1075–1078 (1999).
Banavar, J. R., Maritan, A. & Rinaldo, A. Size and form in efficient transportation networks. Nature 399, 130–132 (1999).
Paull, C. K. et al. Seawater circulation through the flank of the Florida platform: evidence and implications. Marine Geol. 102, 265–279 (1991).
Tryon, M. D. & Brown, K. M. Complex flow patterns through Hydrate Ridge and their impact on seep biota. Geophys. Res. Lett. 28, 2863–2866 (2001).
Mastalerz, V., de Lange, G. J., Dählmann, A. & Feseker, T. Active venting at the Isis mud volcano, offshore Egypt: origin and migration of hydrocarbons. Chem. Geol. 246, 87–106 (2007).
Nakayama, N., Ashi, J., Tsunogai, U., Gamo, T. & Tanahashi, M. Sources of pore water in a Tanegashima mud volcano inferred from chemical and stable isotopic studies. Geochem. J. 44, 561–569 (2010).
Torres, M. E. et al. Fluid and chemical fluxes in and out of sediments hosting methane hydrate deposits on Hydrate Ridge, OR, I: Hydrological provinces. Earth Planet. Sci. Lett. 201, 525–540 (2002).
Sauter, E. J. et al. Methane discharge from a deep-sea submarine mud volcano into the upper water column by gas hydrate-coated methane bubbles. Earth Planet. Sci. Lett. 243, 354–365 (2006).
Felden, J., Wenzhöfer, F., Feseker, T. & Boetius, A. Transport and consumption of oxygen and methane in different habitats of the Håkon Mosby mud volcano (HMMV). Limnol. Oceanogr. 55, 2366–2380 (2010).
Solomon, E. A., Kastner, M., Jannasch, H., Robertson, G. & Weinstein, Y. Dynamic fluid flow and chemical fluxes associated with a seafloor gas hydrate deposit on the northern Gulf of Mexico slope. Earth Planet. Sci. Lett. 270, 95–105 (2008).
Tryon, M. D., Brown, K. M. & Torres, M. E. Fluid and chemical flux in and out of sediments hosting methane hydrate deposits on Hydrate Ridge, OR, II: Hydrological processes. Earth Planet. Sci. Lett. 201, 541–557 (2002).
Coffin, R. et al. Analysis of methane and sulfate flux in methane-charged sediments from the Mississippi Canyon, Gulf of Mexico. Mar. Petrol. Geol. 25, 977–987 (2008).
Ruppel, C., Dickens, G. R., Castellini, D. G., Gilhooly, W. & Lizarralde, D. Heat and salt inhibition of gas hydrate formation in the northern Gulf of Mexico. Geophys. Res. Lett. 32, L04605 (2005).
Ruppel, C., Boswell, R. & Jones, E. Scientific results from Gulf of Mexico Gas Hydrates Joint Industry Project Leg 1 drilling: introduction and overview. Mar. Petrol. Geol. 25, 819–829 (2008).
Cardoso, S. S. S. & McHugh, S. T. Turbulent plumes with heterogeneous chemical reaction on the surface of small buoyant droplets. J. Fluid Mech. 642, 49–77 (2010).
Domingos, M. G. & Cardoso, S. S. S. Turbulent two-phase plumes with bubble-size reduction owing to dissolution or chemical reaction. J. Fluid Mech. 716, 120–136 (2013).
Boswell, R. & Collett, T. S. Current perspectives on gas hydrate resources. Energy Environ. Sci. 4, 1206–1215 (2011).
Ruppel, C. D. Methane hydrates and contemporary climate change. Nat. Educ. Knowledge 3, 29 (2011).
Turcotte, D. L. & Schubert, G. Geodynamics Cambridge University Press (2002).
Chapman, S. & Cowling, T. G. in The Mathematical Theory of Non-Uniform Gases 3rd edn Cambridge University Press (1970).
Duan, Z. & Mao, S. A thermodynamic model for calculating methane solubility, density and gas phase composition of methane-bearing aqueous fluids from 273 to 523 K and from 1 to 2000 bar. Geochim. Cosmochim. Acta 70, 3369–3386 (2006).
We thank Francesca Alvisi, Bruno Escribano, Diego González, Ignacio Sainz-Díaz and Micol Todesco for useful discussions. S.S.S.C. acknowledges the financial support of the UK Leverhulme Trust project RPG-2015-002. J.H.E.C. acknowledges the financial support of the Spanish MINCINN project FIS2013-48444-C2-2-P.
The authors declare no competing financial interests.
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Cardoso, S., Cartwright, J. Increased methane emissions from deep osmotic and buoyant convection beneath submarine seeps as climate warms. Nat Commun 7, 13266 (2016). https://doi.org/10.1038/ncomms13266