Ocean margin sediments have been considered as important sources of dissolved organic carbon (DOC) to the deep ocean, yet the contribution from advective settings has just started to be acknowledged. Here we present evidence showing that near-surface heating of sediment in the Guaymas Basin, a young extensional depression, causes mass production and discharge of reactive dissolved organic matter (DOM). In the sediment heated up to ~100 °C, we found unexpectedly low DOC concentrations in the pore waters, reflecting the combined effect of thermal desorption and advective fluid flow. Heating experiments suggested DOC production to be a rapid, abiotic process with the DOC concentration increasing exponentially with temperature. The high proportions of total hydrolyzable amino acids and presence of chemical species affiliated with activated hydrocarbons, carbohydrates and peptides indicate high reactivity of the DOM. Model simulation suggests that at the local scale, near-surface heating of sediment creates short and massive DOC discharge events that elevate the bottom-water DOC concentration. Because of the heterogeneous distribution of high heat flow areas, the expulsion of reactive DOM is spotty at any given time. We conclude that hydrothermal heating of young rift sediments alter deep-ocean budgets of bioavailable DOM, creating organic-rich habitats for benthic life.
The vast pool of marine DOC represents an important growth substrate for heterotrophic microorganisms1. In the deep ocean, DOC is considered to be refractory2, yet recent carbon budgets in the bathypelagic zone suggested that ‘dark ocean respiration’, driven mainly by prokaryotic activities3 below the euphotic zone, frequently exceeds the total influx of organic carbon (including particulate organic carbon and DOC) from the upper ocean4. One of the explanations for this imbalance is the existence of unaccounted sources introducing biodegradable organic matter into the deep ocean4. Although it has been argued that ocean margin sediments are quantitatively important sources of DOC to the deep ocean5,6, the contribution from advective settings, such as cold seeps7, has just started to be acknowledged.
Thermally altered sediments have not been accounted for as benthic DOC sources. Laboratory experiments and field studies have demonstrated marked accumulation of bulk DOC and acetate, a common substrate for prokaryotic life, in diagenetically heated marine sediment8,9,10. Although the geothermal gradients of 30–80 °C km–1 (ref. 11) in most sedimentary basins require great subseafloor depths to trigger this process, near-seafloor heating of sediment also takes place in spreading centers. To examine the flux of DOC and biodegradability of DOM from such environments, we measured the DOC concentration in the bottom water and sediment from the Guaymas Basin (Table 1 and Fig. S1 of Supplementary Information), an extensional depression representing the transition from continental rifting to seafloor spreading12. In addition, batch experiments simulating low-temperature heating were carried out to study the formation and composition of heat-mobilized DOM. These experimental data were finally used to estimate the DOC efflux from the young rift sediment at different spatiotemporal scales. Our multiple lines of evidence indicate that near-surface heating of young rift sediment creates mass production and release of reactive DOM, a process that has not been reported in other seafloor environments.
Results and Discussion
Sediment geochemistry and water-extractable DOC (DOCWE)
In the hydrothermally altered sediment, the temperature increased from 3 °C to over 100 °C within less than 40 cm (Fig. 1a). Using Fourier’s law and thermal conductivity of 0.9 W m−1 K−1 for the bulk sediment, we obtained an average heat flow of 207 W m−2. Neither did the hydrothermal sites show elevated levels of DOC relative to the reference site (Fig. 1a; see Fig. S2 of Supplementary Information for the profiles from other hydrothermal sites; the reference site is published in McKay et al.13), nor did DOC concentration profiles increase exponentially with depth as typically observed in anoxic, organic-rich sediment in ocean margins6. The seawater-level content of Mg2+ in pore waters of the hydrothermally impacted sediment and the presence of ample sulfate (22‒26 mmol L−1 pore water) despite the high sedimentary sulfur content (3‒6.5% of dry weight (% dw); Fig. S3 of Supplementary Information) imply advective pore fluid flow, possibly driven by hydrothermal fluid circulation between shallow sediment and seawater14. Similar to previously published push cores from the Guaymas Basin hydrothermal field15, sediment from the heated site was heavily impregnated with petroleum and exhibited total organic carbon contents as high as 5‒8% dw (Fig. S3 of Supplementary Information). When the bituminous material was removed via solvent extraction, the heated site, especially in sediment deeper than 5 cm, possessed only half of the kerogen carbon content observed at the reference site. This data set indicates that thermally induced loss of organic matter from the solid phase and the subsequent migration of heat-mobilized products have occurred. With rising temperature, kerogen rearranges its structure and releases mobile organic compounds16. A fraction of these compounds is oily, condenses on cold particle surfaces when migrating upward, and forms the oil-impregnated sediment that is characteristic for Guaymas Basin17,18,19.
In order to test whether such a “mobilization and expulsion” mechanism also applies to water-soluble compounds, we measured water-extractable DOC (DOCWE), the organic carbon pool that could be readily mobilized from the solid phase by short-term aqueous extraction. We employed two methods, batch extraction with artificial seawater and Soxhlet extraction with Milli-Q water, to constrain the range of DOCWE contents. Both methods generated the same pattern of much lower DOCWE contents by one to two orders of magnitude in the heated site compared to the reference site (Fig. 1a), consistent with the prediction of thermal mobilization and expulsion of DOC from the sediment under in situ conditions. In addition, we did not see indications of DOC condensation in the sediment of the heated site, suggesting that expulsion into the water column or degradation represent the major fates of mobilized DOC. Taken together, the geochemical data suggest that DOC distribution was not controlled by diffusion but by hydrothermal mobilization and circulation. The heat-driven fluid flows through the sediment flushes away solutes released from the organic-rich sediments, gradually depletes the mobilizable fraction of organic matter on the particle surface over time, and finally decouples the extant pore-water DOC distribution from the temperature regime.
Formation and composition of heat-mobilized DOM
Since extant pore-water profiles of DOC are impacted and altered by advective fluid flow, they cannot be used to assess the efflux and degradability of sedimentary DOC upon heating. We instead studied the formation and composition of heat-mobilized DOC by means of long-term (191 days) heating experiments using the reference site sediment. Both non-sterilized and sterilized sediments showed an exponential increase in DOC with temperature (Fig. 1b), confirming the predominantly abiotic nature of heat-induced DOC release. The marked difference in DOC between the non-sterilized and sterilized sediment incubated at 50 °C reflected the activity of heterotrophs, which also resulted in a substantial decrease of sulfate and accumulation of dissolved inorganic carbon (see Fig. S4 of Supplementary Information). Accumulation of DOC over time in the heating experiments can be broadly fitted with first-order kinetics (Fig. 1c). In the heated sediment (50 and 90 °C), the maximum DOC concentrations were reached within only dozens of days, suggesting thermal mobilization of DOC from sediment to be an exceptionally rapid process compared to diagenetic alteration and remineralization.
The degradability of heat-mobilized DOM was assessed with total hydrolyzable dissolved amino acids (THDAA), which also increased exponentially from 0.7 to ~4300 μmol L−1 fluid with elevated temperature (Table 2 and Fig. 2). The observed increase of THDAA-based N to total dissolved nitrogen during heating of sterilized samples, from 5.9% at 12 °C to 20% at 90 °C (Table 2), provides a first indication of enhanced reactivity. The degradation index (DI; ref. 20) was calculated using the concentration data of 14 amino acids (see Table 2). More positive values indicate greater reactivity of organic matter. For the sterilized sediment, which showed a fairly linear trend on a double logarithmic scale, the elevated DI at 50 and 90 °C was mainly ascribed to the selective enrichment of leucine and isoleucine, which together contributed to a positive shift of 0.8‒1.2 along the DI scale. The heat-mobilized THDAAs were biodegradable, as manifested by a decrease of 87% in THDAA concentration in the non-sterilized sediment at 50 °C compared to the sterilized control. This biodegraded, residual DOM, enriched in aspartic acid and depleted in leucine, isoleucine and methionine, exhibited the lowest DI and hence the highest degree of recalcitrance.
Non-targeted molecular characterization of heat-mobilized DOM using Fourier transform-ion cyclotron resonance-mass spectrometry (FT-ICR-MS) further revealed the presence of molecular formulas that can be affiliated with reactive compound classes (Fig. 3; see also Table S1 and Fig. S5 of Supplementary Information). Compared to low-temperature samples, the 90 °C sample exhibits selective enrichment of CHO and CHN3–4O species with high H/C and low O/C ratios (see Table S1 of Supplementary Information). Two groups of CHO species became detectable only after heating of the sediment (Fig. 3a). The formulas of the first group (O/C > 0.6, H/C > 1.3) resembled the elemental composition of carbohydrates21, whereas the other group was less oxidized but more aliphatic (O/C < 0.6, H/C > 1.7, double bond equivalent ≤4)22. About 30% of the heat-activated aliphatic compounds shared the same molecular composition as the metabolites recently found in oil-entrapped water droplets23, suggesting their possible identity as activated hydrocarbons24. The most striking feature of heat-mobilized DOM is the elevated proportion of CHN3‒4O formulas, 34% of which matching the composition of tri- and tetrapeptides (Fig. 3b and Fig. S6 of Supplementary Information). These lines of evidence agree well with the THDAA data (Fig. 2) and reinforce the argument of reactive heat-mobilized DOM.
The compositional data also suggest that multiple mechanisms besides desorption, which is known to be highly temperature-dependent25, are shaping the molecular composition of DOM. For example, the detection of molecules affiliated with activated hydrocarbons suggests that hydrophobic compounds become more accessible to microorganisms at elevated temperature, possibly via their enhanced solubility in hot water26. The presence of the identified oligosaccharide- and oligopeptide-like components would require hydrolysis of biomacromolecules to smaller fragments in the heated sediment27. An in-depth examination of the molecular composition and mobilization mechanism of DOM is beyond the scope of this study and will be presented elsewhere.
Assessing the DOC efflux
To estimate the contribution to deep-sea DOC from near-surface heating of young rift sediment, the heat-induced sedimentary DOC efflux needs to be constrained. We first employed a simple reaction-transport model to obtain insights into the magnitude and evolution of transient DOC efflux upon a heating event. Three parameters that have been experimentally determined in the present work were incorporated into the model. First, the temperature dependence of maximum DOC yield can be derived from the results of the non-sterilized incubations (Fig. 1b):
where ΔDOCmax (μmol g−1 dry sediment) is the difference between maximum and initial DOC concentrations, T is the experimental temperature in °C, and m and b are coefficients determined by linear regression.
The DOC evolution records at three incubation temperatures (Fig. 1c) enabled us to mathematically describe the second parameter, the kinetics of DOC production:
where P is the concentration of product as a function of time, A0 the initial concentration of reactant, k the rate constant, and t the reaction time. In our case, we set A0 as ΔDOCmax and P as ΔDOCt, which is the concentration difference in DOC (in μmol g−1 dry sediment) between a specific time point and experimental start. k can be further fitted by the Arrhenius equation:
where A is a prefactor, Ea is the activation energy, and R is the universal gas constant.
The advection of warm fluids creates temperature anomalies (Fig. 1a), which in turn provide information on the third parameter, the advection rate of pore water. Assuming steady flow with a constant source temperature, the resulting temperature profile is described by the following analytical solution to the heat transfer equation (modified from Henry et al.28):
where z is the subseafloor depth (positive downward), dz the depth offset to compensate for inaccurate estimates of penetration depth, Ts the source temperature, Tbw the bottom water temperature, v the Darcy velocity (upward is negative because z is positive downward), ρw the density of pore water, cw the specific heat capacity of pore water, and κ the thermal conductivity of the bulk sediment.
The values of parameters, coefficients and constants are listed in Table S2 of Supplementary Information. Equations (1) to (4) and the diffusion coefficient of DOC29 were used in the reaction-transport model Explicite30 to simulate the temporal evolution of DOC efflux. In the case of the hydrothermal site visited in Dive 4568, the modeled DOC efflux from the upper 33 cm of heated sediment was 30 to 78 mol C m–2 yr–1 (Fig. 4). The production of DOC was temporally heterogeneous; more than 70% of the heat-mobilized DOC would be flushed out to the bottom water in the first 30 days after heating, leading to instantaneous efflux as high as 4.5 mol C m–2 d–1. The bottom-water DOC concentrations reflected the impact of the short and massive DOC discharge events: despite the presence of strong bottom currents with velocities up to 12 cm s–1 (ref. 31), the seawater sampled 2 m above the seafloor (Table 1) had DOC concentrations 3 to 50 times higher than the typical concentration (~40 μmol L−1; ref. 2) in the bathypelagic zone. The effects of near-surface heating on mobilization of sedimentary organic matter and the consequential massive discharge of reactive DOM and concurrent impregnation of the sediment with oil-like components are schematically summarized in Fig. 5. The DOC efflux from a heated, 30-cm thick sediment column exceeds the particulate organic carbon burial flux from the overlying water column32 by two orders of magnitude. This imbalance occurs because the heat-mobilizable fraction of sedimentary organic matter that has accumulated over hundreds of years is released during comparatively short periods of heating.
For longer time scales, in the presence of a temporally stable heat source, the availability of heat-mobilizable organic matter is the main controlling factor of DOC efflux. To assess the long-term average DOC efflux for the basin, we adopted an approach following Lizarralde et al.12, who based their estimation of carbon release, irrespective of the form of carbon, on the sedimentation rates and efficiency of magmatism-induced alteration processes. Our long-term heating experiment showed that at 90 °C, the efficiency of DOC production was equivalent to up to 0.56% dw (or ~19% of the initial total organic carbon content of 3% dw; Figs 1a and S3), which translates to 28% of the maximum total carbon loss induced by magmatism12. After correcting for carbon loss due to background remineralization represented by the decline of DOCWE contents with depth at the reference site (~6% of the initial total organic carbon content based on the average of the two DOCWE data sets; Fig. 1a), we obtained a maximum DOC flux of 27 Gg C yr–1 based on a sedimentation rate of 0.18 cm yr–1 (ref. 33) and an area of ~4950 km2 of active sill intrusion12. This maximum flux needs to be revised based on the spatial heterogeneity of near-surface heating13, temporal fluctuation in fluid temperature34, and consumption of DOM by benthic organisms. Assuming that <1% of the sediment undergoes near-surface heating at the current stage, we estimated the DOC efflux averaged over the whole area of magmatism to be <5 mmol C m−2 yr−1, equivalent to <0.8% of the particulate organic carbon burial flux in the overlying water column32. For the majority of the sediment that has heat flow barely exceeding 10 W m−2 (ref. 35), the mobilized DOC at deeper depths will accumulate in the pore fluid36 due to the sluggish pore fluid flow37 and long transport distance to the seafloor. Therefore, the massive DOC discharge during spotty near-surface heating contributes little in counteracting the natural carbon sequestration in this highly productive coastal ocean, an implication highlighted by Lizarralde et al.12 for the shallow magmatism in young sedimented rift. However, if the young rift system of the Guaymas Basin continues to spread in a manner similar to nascent mid-ocean ridges, the extensional force would allow magma intrusion to occur at increasingly shallower depths38 in a widening basin, elevating the proportion of DOM released to seawater. Such a massive release of bioavailable DOM could stimulate respiration in the deep water at a basin-wide scale, thereby altering the bottom water oxygen content34,39, carbon chemistry, and even pH. Most importantly, this process creates unprecedented DOM-rich oases at the seafloor, making the young rift sediment a natural incubator of rich benthic life34,40.
Material and Methods
Bottom-water samples in the Southern Trough of the Guaymas Basin were retrieved from ~2 m above the seafloor by 5-L Niskin bottles mounted on the Human Occupied Vehicle (HOV) Alvin during the expedition AT15–56 (November-December, 2009) of the RV Atlantis (Table 1 and Fig. S1 of Supplementary Information; see McKay et al.13 for detailed description). Push core sampling and heat probe measurements were also carried out by the HOV Alvin. Seawater samples were filtered through pre-combusted (450 °C, 8 hrs) glass fiber filters (0.7 μm) for DOC analysis. Pore-water samples for geochemical analyses were extracted by the Rhizon suction samplers41 (pore size 0.2 μm). Sediment samples were cut into 3- to 4-cm thick slices for solid phase analysis and aqueous extraction. Except for the supplementary pore-water DOC profiles (Fig. S2 of Supplementary Information), all of the analyses and experiments were based on materials from microbial mat-free sediment from Dives 4567 (reference site) and 4568 (hydrothermally impacted site). The distance between these two sites was about 200 m.
The downcore DOCWE distribution was determined via both batch extraction with artificial seawater and Soxhlet extraction with Milli-Q water. For batch extraction, about 10 to 30 g of frozen, wet sediment from each depth were mixed with artificial seawater at a ratio of 1:2.4 (w/w) to make bulk slurry. The slurries were purged with argon, dispensed into 20 mL glass ampoules, flame sealed, and incubated in the dark at 90 °C for up to 30 days. To harvest the aqueous phase for analysis, all slurry samples were allowed to cool down to room temperature before phase separation. Slurries in the ampoules were centrifuged and the supernatant filtered with Rotilabo polytetrafluoroethylene syringe filters (pore size 0.45 μm; Carl Roth GmbH, Karlsruhe, Germany). The fluid samples were stored at −20 °C until DOC analysis.
The Soxhlet extraction was carried out broadly following the procedure described in Schmidt et al.27 The Soxhlet extractors were cleaned by alkaline detergent and thoroughly rinsed with Milli-Q water prior to use. To reduce the blank DOC level, the assembled extractors containing empty Whatman glass microfiber thimbles (30 × 100 mm; precombusted at 450 °C for 8 hrs) were flushed with heated Milli-Q water for 24 hrs. After the cleaning step, 10 to 20 g of frozen, wet sediment were weighed into the thimbles and extracted with 200 mL of fresh Milli-Q in the dark for 48 hrs. The extracts were filtered through pre-combusted Whatman GF/F filters, weighed, and stored at −20 °C until DOC analysis. For the reference site sediment, Soxhlet extraction yielded lower DOCWE than batch extraction by a factor of 2.5 to 3.9 (Fig. 1a), possibly due to the shorter extraction time, the lower reaction temperature (ca. 80 °C; ref. 27), the lack of ionic strength in the solvent, or the combination of these factors.
The measured DOCWE values were normalized to the initial total organic carbon content (TOCinit) of 3% dw, which was the measured value of the top 5 cm sediment from the reference site (Fig. S3 of Supplementary Information). This TOCinit value is in the range (2.3‒3.5% dw) reported for the surface sediments in the central Gulf of California42. Given the proximity of the reference and heated sites, we used the same TOCinit for samples from both sites.
Near-surface sediment (0–10 cm) and overlying water in the core taken from the reference site were pooled to make slurries for the heating experiment. These materials differed from those for DOCWE analysis in that they were kept cold (4 °C) instead of frozen after the cruise. The sediment slurries were dispensed into customized 40 mL glass ampoules in an anaerobic chamber, flushed with argon, flame sealed, and incubated in the dark at 12, 50, and 90 °C for up to 191 days. Sterilized controls were prepared by adding zinc chloride into the slurries to a final concentration of 5% (w/v). To monitor the progress of reactions, a suite of small-volume (4 mL) slurries in small glass vials were incubated at each of the temperatures and were sacrificed sequentially for interim geochemical analyses. Because of material limitation, we had only duplicates for the large-volume incubations. To harvest the aqueous phase for analysis, all slurry samples were allowed to cool down to room temperature before phase separation. Slurries in the glass vials were centrifuged and the supernatant was filtered with syringe filters as described above. Slurries in the ampoules were extracted in an anoxic chamber with Rhizon suction samplers. The fluid samples for biogeochemical analysis were stored at −20 °C. The samples for non-targeted DOM analysis were immediately extracted (see below).
DOC and total dissolved nitrogen were measured with high-temperature catalytic oxidation-infrared detection. Solid-phase carbon contents were determined by an elemental analyzer. Sediment samples were first decalcified for measurements of total organic carbon content, and then treated by a mixture of dichloromethane and methanol (volume ratio = 9:1 v/v) for determination of kerogen carbon in the non-extractable residue. Sulfate concentration was determined by ion chromatography. DIC was determined as carbon dioxide liberated from acidified samples by infrared spectroscopy. Dissolved Mg2+ was determined by inductively-coupled plasma-optical emission spectroscopy. Total sulfur contents of the sediment samples were determined by an elemental analyzer. Fluid samples for THDAA analysis were acid hydrolyzed, pre-column derivatized with o-phthaldialdehyde and N-isobutyryl-L/D-cysteine, and analyzed with high-performance liquid chromatography-fluorescence detection43.
DOM for non-targeted mass spectrometric analysis was extracted using solid-phase extraction cartridges following the procedure described in Dittmar et al.44 Samples were ionized by an Apollo II electrospray source (Bruker Daltonik GmbH, Bremen, Germany) in negative ion mode and measured on a SolariX (FT-ICR-MS; Bruker Daltonik GmbH) equipped with a 12 T refrigerated actively shielded superconducting magnet (Bruker Biospin, Wissembourg, France). Data evaluation started with internal calibration of the mass spectra with a suite of compounds repeatedly identified in marine DOM samples22,45. The root mean square error of the internal calibration was below 0.100 ppm. Data evaluation was performed in the range m/z 200 to 600. For peaks with a signal to noise ratio higher than 3, molecular formulas were calculated in the mass accuracy range of ±0.5 ppm by considering the following elements: 1H (0 to 90), 12C (0 to 60), 13C (0 to 1), 16O (0 to 35), 14N (0 to 4), 32S (0 to 2), 34S (0 to 1). The criteria summarized in Koch et al.46 were applied for formula assignment. For the final dataset we focused on ions with a relative intensity (normalized to the highest peak in each spectra) of ≥3%, corresponding to a signal to noise ratio of ≥6.
How to cite this article: Lin, Y.-S. et al. Near-surface Heating of Young Rift Sediment Causes Mass Production and Discharge of Reactive Dissolved Organic Matter. Sci. Rep. 7, 44864; doi: 10.1038/srep44864 (2017).
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Kujawinski, E. B. The impact of microbial metabolism on marine dissolved organic matter. Annu. Rev. Mar. Sci. 3, 567–599 (2011).
Hansell, D. A. Recalcitrant dissolved organic carbon fractions. Annu. Rev. Mar. Sci. 5, 421–445 (2013).
Reinthaler, T. et al. Prokaryotic respiration and production in the meso- and bathypelagic realm of the eastern and western North Atlantic basin. Limnol. Oceanogr. 51, 1262–1273 (2006).
Burd, A. B. et al. Assessing the apparent imbalance between geochemical and biochemical indicators of meso- and bathypelagic biological activity: What the @$#! is wrong with present calculations of carbon budgets? Deep-Sea Res. II 57, 1557–1571 (2010).
Bauer, J. E. & Druffel, E. Ocean margins as a significant source of organic matter to the deep open ocean. Nature 392, 482–485 (1998).
Burdige, D. J. Sediment pore waters. In: Hansell, D. A. & Carlson, C. A. (Eds) Biogeochemistry of Marine Dissolved Organic Matter (Academic Press, London, 2002).
Pohlman, J. W. et al. Methane hydrate-bearing seeps as a source of aged dissolved organic carbon to the oceans. Nat. Geosci. 4, 37–41 (2011).
Wellsbury, P. et al. Deep marine biosphere fueled by increasing organic matter availability during burial and heating. Nature 388, 573–576 (1997).
Parkes, R. J. et al. Temperature activation of organic matter and minerals during burial has the potential to sustain the deep biosphere over geological timescales. Org. Geochem. 38, 845–852 (2007).
Egeberg, P. K. & Barth, T. Contribution of dissolved organic species to the carbon and energy budgets of hydrate bearing deep sea sediments (Ocean Drilling Program Site 997 Blake Ridge). Chem. Geol. 149, 25–35 (1998).
Wright, J. A. & Louden, K. E. CRC Handbook of Seafloor Heat Flow (CRC Press, Boca Raton, FL, 1989).
Lizarralde, D., Soule, S. A., Seewald, J. S. & Proskurowski, G. Carbon release by off-axis magmatism in a young sedimented spreading center. Nature Geosci. 4, 50–54 (2010).
McKay, L. J. et al. Spatial heterogeneity and underlying geochemistry of phylogenetically diverse orange and white Beggiatoa mats in Guaymas Basin hydrothermal sediments. Deep-Sea Res. I 67, 21–31 (2012).
Gundersen, J. K., Jørgensen, B. B., Larsen, E. & Jannasch, H. W. Mats of giant sulphur bacteria on deep-sea sediments due to fluctuating hydrothermal flow. Nature 360, 454–456 (1992).
Magenheim, A. J. & Gieskes, J. M. Hydrothermal discharge and alteration in near-surface sediments from the Guaymas Basin, Gulf of California. Geochim. Cosmochim. Acta 56, 2329–2338 (1992).
Killops, S. D. & Killops, V. J. Introduction to Organic Geochemistry (Wiley, Oxford, 2005).
Simoneit, B. R. T. & Lonsdale, P. F. Hydrothermal petroleum in mineralized mounds at the seabed of Guaymas Basin. Nature 295, 198–202 (1982).
Didyk, B. M. & Simoneit, B. R. T. Hydrothermal oil of Guaymas Basin and implications for petroleum formation mechanisms. Nature 342, 65–69 (1989).
Peter, J. M. et al. 14C ages of hydrothermal petroleum and carbonate in Guaymas Basin, Gulf of California: Implications for oil generation, expulsion, and migration. Geology 19, 253–256 (1991).
Dauwe, B., Middelburg, J. J., Herman, P. M. J. & Heip, C. H. R. Linking diagenetic alteration of amino acids and bulk organic matter reactivity. Limnol. Oceanogr. 44, 1809–1814 (1999).
Sleighter, R. L. & Hatcher, P. G. Molecular characterization of dissolved organic matter (DOM) along a river to ocean transect of the lower Chesapeake Bay by ultrahigh resolution electrospray ionization Fourier transform ion cyclotron resonance mass spectrometry. Mar. Chem. 110, 140–152 (2008).
Schmidt, F., Elvert, M., Koch, B. P., Witt, M. & Hinrichs, K. U. Molecular characterization of dissolved organic matter in pore water of continental shelf sediments. Geochim. Cosmochim. Acta 73, 3337–3358 (2009).
Meckenstock, R. U. et al. Water droplets in oil are microhabitats for microbial life. Science 345, 673–676 (2014).
Widdel, F., Boetius, A. & Rabus, R. Anaerobic biodegradation of hydrocarbons including methane. Prokaryotes 2, 1028–1049 (2006).
Cornelissen, G., van Noort, P. C. M., Rarsons, J. R. & Govers, H. A. J. Temperature dependence of slow adsorption and desorption kinetics of organic compounds in sediments. Environ. Sci. Technol. 31, 454–460 (1997).
Marche, C., Ferronato, C. & Jose, J. Solubilities of n-alkanes (C6 to C8) in water from 30 °C to 180 °C. J. Chem. Eng. Data 48, 967–971 (2003).
Schmidt, F., Koch, B. P., Witt, M. & Hinrichs, K. U. Extending the analytical window for water-soluble organic matter in sediments by aqueous Soxhlet extraction. Geochim. Cosmochim. Acta 141, 83–96 (2014).
Henry, P. et al. Fluid flow in and around a mud volcano field seaward of the Barbados accretionary wedge: results from the Manon cruise. J. Geophys. Res. 101 (B9), 20323–20797 (1996).
Alperin, M. J., Albert, D. B. & Martens, C. S. Seasonal variations in production and consumption rates of dissolved organic carbon in an organic-rich coastal sediment. Geochim. Cosmochim. Acta 58, 4909–4930 (1994).
Zabel, M. & Schulz, H. D. Importance of submarine landslides for non-steady state conditions in pore water systems – lower Zaire (Congo) deep-sea fan. Mar. Geol. 176, 87–99 (2001).
Lonsdale, P. & Becker, K. Hydrothermal plumes, hot springs, and conductive heat flow in the Southern Trough of Guaymas Basin. Earth Planet. Sci. Lett. 73, 211–225 (1985).
Thunell, R. C. Seasonal and annual variability in particle fluxes in the Gulf of California: A response to climate forcing. Deep-Sea Res. I 45, 2059–2083 (1998).
Thunell, R. C., Pride, C. J., Tappa, E. & Muller-Karger, F. E. Biogenic silica fluxes and accumulation rates in the Gulf of California. Geology 22, 303–306 (1994).
Teske, A. D. et al. The Guaymas Basin hiking guide to hydrothermal mounds, chimneys and microbial mats: complex seafloor expressions of subsurface hydrothermal circulation. Frontiers in Microbiology 7, 75, doi: 10.3389/fmicb.2016.00075 (2016).
Fisher, A. T. & Becker, K. Heat flow, hydrothermal circulation and basalt intrusions in the Guaymas Basin, Gulf of California. Earth Planet. Sci. Lett. 103, 84–89 (1991).
Chen, R. F., Bada, J. L. & Suzuki, Y. The relationship between dissolved organic carbon (DOC) and fluorescence in anoxic marine porewaters: Implications for estimating benthic DOC fluxes. Geochim. Cosmochim. Acta 57, 2149–2153 (1993).
Fisher, A. T. & Narasimhan, T. N. Numerical simulations of hydrothermal circulation resulting from basalt intrusions in a buried spreading center. Earth Planet. Sci. Lett. 103, 100–115 (1991).
Svensen, H. et al. Release of methane from a volcanic basin as a mechanism for initial Eocene global warming, Nature 429, 542–545 (2004).
Calvert, S. E. Factors affecting distribution of laminated diatomaceous sediments in Gulf of California. In: van Andel, T. J., & Short, G. G. (Eds), Marine Geology of Gulf of California. Am. Assoc. Petrol. Geol. Mem. 3, 311–330 (1964).
McKay, L. et al. Thermal and geochemical influences on microbial biogeography in the hydrothermal sediments of Guaymas Basin, Gulf of California. Environ. Microbiol. Rep. 8, 150–161 (2016).
Seeberg-Elverfeldt, J. et al. Rhizon sampling of porewaters near the sediment-water interface of aquatic systems. Limnol. Oceanogr.: Methods 3, 361–371 (2005).
Calvert, S. E. Accumulation of diatomaceous silica in the sediments of the Gulf of California. Geol. Soc. Am. Bull. 77, 569–596 (1966).
Fitznar, H. P., Lobbes, J. M. & Kattner, G. Determination of enantiomeric amino acids with high-performance liquid chromatography and pre-column derivatisation with o-phthaldialdehyde and N-isobutyrylcysteine in seawater and fossil samples (mollusks). J. Chromatogr. A 832, 123–132 (1999).
Dittmar T. et al. A simple and efficient method for the solid-phase extraction of dissolved organic matter (SPE-DOM) from seawater. Limnol. Oceanogr.: Methods 6, 230–235 (2008).
Flerus, R. et al. Molecular level investigation of reactions between dissolved organic matter and extraction solvents using FT-ICR MS. Mar. Chem. 124, 100–107 (2011).
Koch, B. P. et al. Fundamentals of molecular formula assignment to ultrahigh resolution mass data of natural organic matter. Anal. Chem. 79, 1758–1763 (2007).
We thank the captain and crew of RV Atlantis, and the Alvin team for expert support above and below sea level during cruise AT15–56 to Guaymas Basin in November/December 2009; the cruise was supported by NSF Biological Oceanography grant OCE-0647633 to Andreas Teske. We thank Jenny Wendt, Xavier Prieto Mollar, Heidi Taubner, Shu-Han Chang, Yu-Min Liao and Hsuan-Min Bao for their support in lab work, Oliver Lechtenfeld and Bing-Rong Jiang for helping with DOC measurements, Kai-Uwe Ludwichowski for amino acid analysis, and Jay Li for providing the Matlab code. YSL was funded through the DFG-Research Center/Excellence Cluster ‘The Ocean in the Earth System’ (MARUM). Additional funding for analytical infrastructure was provided by the European Research Council project DARCLIFE to KUH [Grant # 247153].
The authors declare no competing financial interests.
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Lin, YS., Koch, B., Feseker, T. et al. Near-surface Heating of Young Rift Sediment Causes Mass Production and Discharge of Reactive Dissolved Organic Matter. Sci Rep 7, 44864 (2017). https://doi.org/10.1038/srep44864
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