Methane cold seep systems typically exhibit extensive buildups of authigenic carbonate minerals, resulting from local increases in alkalinity driven by methane oxidation. Here, we demonstrate that modern seep authigenic carbonates exhibit anomalously low clumped isotope values (Δ47), as much as ∼0.2‰ lower than expected values. In modern seeps, this range of disequilibrium translates into apparent temperatures that are always warmer than ambient temperatures, by up to 50 °C. We examine various mechanisms that may induce disequilibrium behaviour in modern seep carbonates, and suggest that the observed values result from several factors including kinetic isotopic effects during methane oxidation, mixing of inorganic carbon pools, pH effects and rapid precipitation. Ancient seep carbonates studied here also exhibit potential disequilibrium signals. Ultimately, these findings indicate the predominance of disequilibrium clumped isotope behaviour in modern cold seep carbonates that must be considered when characterizing environmental conditions in both modern and ancient cold seep settings.
Methane cold seeps host diverse macro and microbiological communities1,2,3,4,5. These ecosystems are driven by microbially mediated reactions involving methane-containing fluids advecting from depth6. As methane ascends it is primarily oxidized anaerobically by sulfate (termed the anaerobic oxidation of methane (AOM)), or aerobically in the presence of oxic seawater, as follows:
Both reactions produce bicarbonate, but only methane oxidation coupled with sulfate reduction increases alkalinity. The alkalinity production fostered by eq. 1 sustained by the relatively high concentration of sulfate in seawater promotes extensive carbonate (and sulfide) mineral production near methane seeps7. Complex microbial consortia facilitate sulfate reduction-coupled methane oxidation8 yielding extensive and generally rapid authigenic carbonate production in cold seep environments.
In an attempt to characterize the interactions in cold seep systems, both modern4,9,10,11,12 and ancient10,11,13,14,15 cold seep deposits have been studied extensively. Of particular importance is the characterization of ancient cold seep environmental conditions and their relationship to modern seep systems. However, due to the inherent issues associated with studies of past environments, characterization of ancient seeps hinges on the reliability of paleoproxies. A particularly useful parameter to quantify is precipitation temperature, as it dictates thermodynamic considerations such as abiotic versus biotic reaction times, and gas hydrate dynamics16. The newly emerging clumped isotope proxy has shown promise as a powerful geothermometer in the geosciences17,18,19,20,21,22, yet the utility of clumped isotopes as an accurate geothermometer in cold seep carbonates has yet to be demonstrated.
Here, we demonstrate the occurrence of non-temperature dependent carbonate clumped isotope signatures in cold seep carbonates through analyses of modern precipitates forming under well-constrained conditions (that is, temperatures, pH, salinities and fluid δ18O values). We compare modern systems with clumped isotope signatures in ancient seep carbonates, and discuss potential mechanisms to explain the observed disequilibrium values.
Both modern and ancient cold seep carbonates are explored here. Modern samples originate from Hydrate Ridge, offshore Costa Rica, the Eel River Basin and the Norwegian Sea. Ancient samples originate from the Tepee Buttes Colorado (Cretaceous), the Panoche Hills California (Paleocene), the Quinault Formation (Mio-Pliocene), the Pysht Formation (Eocene) and the Lincoln Creek Formation (Oligocene; Fig. 1).
Modern cold seeps occur along continental margins and within large inland seas (for example, the Black and Mediterranean Seas)23,24. These sites exhibit spatially and temporally variable delivery of subsurface methane, derived from sedimentary production (microbial or thermogenic), to relatively oxic marine waters25. This methane is oxidized microbially either by reaction with dissolved oxygen or sulfate26, as explained above. Photographs, photomicrographs and previously reported and new δ13C and δ18O values are provided in Figs 2, 3, 4, respectively.
Cold seep systems of Hydrate Ridge exhibit authigenic carbonate buildups in the form of chimneys, crusts, slabs, cements and concretions12,27,28,29,30. These carbonate buildups are actively forming, and carbon-14 ages indicate that authigenesis has occurred within the last∼40 ka (ref. 30). Carbonate δ13C (δ13Ccarb) values are extremely negative and commonly extend to lesser than –30‰ (VPDB), indicative of a significant methane carbon source (Fig. 4). Carbonates consist of aragonite, calcite, high-magnesium calcite and dolomite primarily as micritic and acicular cements31,32,33 (Figs 2 and 3). Bottom water temperatures of Hydrate Ridge are ∼4–5 °C (ref. 12).
Authigenic carbonates (Figs 2 and 3) associated with cold seeps of the Eel River Basin occur primarily as irregular carbonate slabs, cements and concretions4. Erosion has exposed ancient carbonates, such that slabs commonly crop out on the seafloor despite formation in shallow sediments4. Authigenic carbonates are composed of magnesium calcite, aragonite and dolomite4. Aragonite and calcite δ13C and δ18O values do not overlap with dolomites but instead exhibit δ13C and δ18O values (Fig. 4) that range from –40 to –3.2‰ and +3.2 and +5.8‰, respectively. In contrast, dolomites express significantly 13C-enriched values with δ13C and δ18O values ranging from +5.0 to +15‰ and +6.1 to +8.9‰, respectively4. The bottom water temperatures of Eel River Basin are ∼5 °C (ref. 4).
Cold seep sites off the coast of Costa Rica exhibit similar authigenic carbonate precipitates (Figs 2 and 3). These precipitates include concretions, carbonate ‘clasts’ and carbonate cemented muds34. Larger buildups are oftentimes referred to as chemoherm carbonates due to the direct association with characteristic cold seep fossil assemblages9,32. These chemoherm carbonates appear morphologically similar to slabs identified at the Hydrate Ridge and Eel River Basin localities. In addition, bottom water temperatures are ∼5 °C, similar to Hydrate Ridge and Eel River Basin9.
The Norwegian Sea hosts cold seep systems yielding primarily aragonitic and calcitic carbonate buildups exposed in seafloor ‘pockmarks’35. These buildups exhibit variable morphologies including crusts, ridges and blocky, tubular or irregular structures33,36. Carbonate carbon and oxygen (δ18Ocarb) isotope values are ∼−50 to −48‰ and ∼+5 to +6‰, respectively36,37 (Fig. 4), similar to values recognized at other modern cold seep sites. The bottom water temperatures are significantly colder than the other sites, ranging from ∼−1 to 1 °C (ref. 35).
In addition to modern seep carbonates, samples of Cretaceous to Oligocene seep carbonates from the western USA are explored here. These carbonates are inferred to have cold seep affinity due to depleted δ13C values (below −30‰) and/or the presence of diagnostic cold seep fossils. The ancient seep carbonates from these localities exhibit similar fabrics to modern seeps including fibrous and finely crystalline micrites4. In addition to these, coarser-crystalline phases including sparry vug filling cements and various sparites occur. Typically, these spars express 18O-depleted and less 13C-depleted compositions, respectively, potentially indicative of formation during later diagenesis (Fig. 4). Ultimately, ancient seeps record a more complex paragenetic evolution than modern seep carbonates10,11,14,15,38.
Modern cold seep carbonates
Carbonate carbon isotope compositions are generally very low, whereas oxygen isotope values are elevated (Fig. 4). Specifically, δ13Ccarb values range from −54.64 to −3.02‰, −49.86 to −39.00‰, +13.97 to +15.95‰, –52.01 to –50.82‰ for carbonates from Hydrate Ridge, Costa Rica, the Eel River Basin and the Norwegian Sea, respectively. Respective δ18Ocarb values range from +3.11 to +7.76‰, +3.76 to +4.10‰, +7.26 to +7.34‰ and +4.72 to +5.42‰ for carbonates from Hydrate Ridge, Costa Rica, the Eel River Basin and the Norwegian Sea. These isotope compositions are consistent with values observed in these and similar cold seep carbonates reported elsewhere4,11,12,27,37,39.
Clumped isotope compositions (Fig. 5, Tables 1 and 2) overlap among all of the modern sample sites. In addition, clumped isotope compositions of fibrous and micritic carbonates (the two most abundant phases recognized) do not exhibit crystal habit-related differences in Δ47. The Δ47 values range from 0.620–0.679‰, 0.639–0.677‰, 0.706–0.740‰ and 0.705–0.783‰ for carbonates from Hydrate Ridge, Costa Rica, the Eel River Basin and the Norwegian Sea, respectively. Equilibrium values calculated for 1 and 5 °C bottom waters are 0.790 and 0.771‰, respectively, using a steep slope calibration40, and 0.768 and 0.753‰, respectively, using a shallow slope calibration41. These calibrations were selected because both were generated partially or fully on the same instrument used for measuring the samples analysed for this study. The extent of disequilibrium (offset from expected equilibrium values) is ∼+0.014 to –0.134‰ in the most conservative scenario, and up to –0.008 to –0.152‰ (Table 3), yielding temperatures that are always warmer than ambient temperatures. These clumped isotope compositions translate to reconstructed temperatures ranging from 3–44°C when a steep slope calibration is used40. If a shallow slope calibration41 is used, the reconstructed temperatures range from −3 to 52 °C.
Ancient cold seep carbonates
Traditional δ13C and δ18O values show a wider range in ancient seep carbonates (Fig. 4). Carbon isotope values range from −45.21 to −14.31‰, −30.08 to −6.05‰, −19.33 to −4.03‰ and −34.99 to −0.92‰ in cold seep carbonates of the Tepee Buttes, Quinault Formation, Pysht Formation and Panoche Hills, respectively (Table 2). Oxygen isotope compositions range from –12.09 to –0.30‰, −8.32 to +0.91‰, −1.00 to +1.53‰ and −0.71 to +2.25‰ in cold seep carbonates of the Tepee Buttes, Quinault Formation, Pysht Formation and Panoche Hills, respectively (Table 2). The Lincoln Creek Formation carbonate exhibits δ13Ccarb and δ18Ocarb values of −15.16 and +1.25‰, respectively (Table 2). These δ13Ccarb and δ18Ocarb values broadly overlap with those reported previously11,13,14,38,42,43 although some of the Tepee Buttes values are lower (Fig. 4).
Ancient cold seep carbonates exhibit clumped isotope compositions that range from those expressed by modern precipitates to significantly lower Δ47 values (Fig. 5; Table 2). Clumped isotope signatures from micritic, fibrous and sparry phases of the Tepee Buttes show no obvious crystallographic-specific distributions (that is, values generally overlap among phases). Tepee Buttes, Quinault Formation, Pysht Formation and Panoche Hills Δ47 values range from 0.377–0.521‰, 0.558–0.644‰, 0.611–0.631‰ and 0.649–0.705‰, respectively. A single sample form the Lincoln Creek Formation yielded a value of 0.623‰. Using the calibration by Tang et al.41, these clumped isotope values translate to temperatures ranging from 107–286 °C, 42–83 °C, 47–56 °C, 19–40 °C and 46 °C, respectively (Supplementary Table 1). The calibration by Tripati et al.40, calibration yields temperatures ranging from 81–169 °C, 37–66 °C, 41–47 °C, 20–35 °C and 40 °C, respectively (Supplementary Table 1).
The δ13Ccarb values reported here from Hydrate Ridge, Costa Rica and the Norwegian Sea are consistent with carbonate formation from dissolved inorganic carbon generated via methane oxidation4. In contrast, the positive δ13Ccarb values of the Eel River Basin carbonates indicate formation in sediments experiencing microbial methane production44. The δ18Ocarb values of cold seep carbonates are ∼+3 to +5‰ higher than those expected for carbonates precipitated in normal seawater with a δ18O of ∼0‰ (Fig. 4). These enriched oxygen isotope values may reflect gas hydrate (clathrate) dissolution at depth, the presence of which has been established at most of the study sites4,9,12,37.
The clumped isotope values presented in this study are not in isotopic equilibrium with ambient temperatures of precipitation. The sediment-water interface temperature at each site is ∼0–5°C (refs 4, 12, 34, 37). The Δ47 values are on the order of ∼0.1‰ lower than expected for an equilibrium precipitate (Fig. 5, Table 3). This translates to significantly elevated carbonate formation temperatures (up to 52 °C) compared with the ambient conditions and well beyond reasonable annual temperature variations of bottom waters. In some cases, authigenic carbonates associated with cold seeps have been postulated to grow after burial and then be exhumed by later sediment winnowing. Whereas this process may account for re-exposure after shallow (<<50 m) burial, it seems very unlikely that winnowing would remove the 100s of metres of the sediment required to reach depths heated to ∼25 °C via burial. Of course, deep burial would be unnecessary if warm fluids were advecting from depth. Modern seep fluids are not hot enough to perturb the ambient bottom water temperatures, however, one could argue that fluid temperatures differed in the recent past. Ultimately, carbonate precipitation at elevated temperature is unlikely given the δ18Ocarb data, which are enriched compared with modern seawater and furthermore exhibit bulk isotope absolute values consistent with equilibrium precipitation from ambient fluids. Therefore, we reject the possibility that the majority of these carbonates formed at temperatures consistent with the predictions based on the clumped isotope data.
Several factors are likely to be important in contributing to the observed clumped isotope disequilibrium signatures at methane seeps. We hypothesize that the AOM reaction (eqs. 1 and 2) produces a kinetic isotope signal in the clumped isotope composition of the generated DIC species (Fig. 6). Kinetic effects have been shown to result from CO2 hydration and hydroxylation reactions (Fig. 6)17,45,46,47, and dehydration/dehydroxylation reactions45. Similar effects also occur in association with oxygen and carbon isotope partitioning among the gaseous and dissolved inorganic carbon phases48. It is highly likely that rate-limiting steps may occur during the methane oxidation process, which may be complex as AOM involves multiple intermediate reaction steps25. We predict these rate-limiting steps may induce a large disequilibrium composition in product HCO3− or CO32−, as with these other systems. Modern cold seep carbonate Δ47 values suggest that AOM leads to decreased Δ47 values. If the reactant methane results from gas hydrate dissolution, the AOM kinetic effects may be accompanied by δ18O enrichment (Fig. 6b). Future work is needed to better constrain the magnitude and direction of offset in Δ47 of these effects on the composition of product DIC species.
The equilibrium clumped isotope composition of HCO3− and CO32− are thought to differ from each other, and from carbonate minerals40,49. Given that both pH and salinity affect DIC speciation, they can impart small but significant deviations in clumped isotope signatures of minerals (Fig. 6a)49. Some cold seep carbonates may have formed in environments experiencing enhanced alkalinity production within relatively saline marine waters and/or fluids influenced by clathrate formation or dissociation50. Theoretical modelling indicates that although the combined effects of salinity and pH affect clumped isotope values, the maximum expected differences in Δ47 are on the order of 0.035‰ over pH and salinity ranges of 5–14 and 0–50 parts per thousand, respectively49. These ranges are beyond those observed in cold seep environments. Experimental data support a somewhat larger effect with maximum offsets of ∼0.060‰ (ref. 40). We suggest that the effects of pH and salinity, although not sufficient enough to produce the full extent of clumped isotope anomalies observed here, may be a contributing factor given the range of fluid compositions at cold seeps.
Mixing of HCO3− or CO32− from two different sources with distinct bulk (δ13C and δ18O) and clumped isotope compositions does not necessarily yield a product reflecting simple linear mixing between end-members17,51,52. Therefore it is feasible that mixing between DIC from seawater and DIC generated from AOM could induce anomalous clumped isotope signatures in the product carbonate minerals.
In addition, geochemically heterogeneous carbonates may yield clumped isotope compositions that do not reflect true precipitation temperatures of the mixture and/or individual end-members. Defliese et al.19 have demonstrated that mixing among carbonate phases with differing isotope compositions can produce inaccurate clumped isotope signatures and therefore have the potential to produce anomalous temperatures, such as those observed in cold seep carbonates. The degree to which the clumped isotope temperatures differ from linear mixing in a two-component system depends on the differing isotope compositions expressed by the two end-members. The offset is greatest when phases are most dissimilar, and mixing occurs in equal proportions (that is, a 50:50 mixture). Such mixing can produce clumped isotope compositions offset in either the positive or negative direction, yielding apparent low or high temperatures, respectively19. Modern and ancient cold seep carbonates commonly exhibit phase heterogeneity on 10–100 μm scales4,11,13,14,15 (Fig. 3). Current clumped isotope analytical protocols preclude sampling at this resolution, therefore cold seep carbonates may yield inaccurate temperatures as a result of phase mixing.
We address the possibility of mixing-related temperature anomalies by considering bulk isotope compositions and initial formation conditions of chemical species that contribute to modern cold seep carbonates. Cold seep carbonates commonly exhibit δ13Ccarb values that extend down to ∼–40 to –60‰ (Fig. 4), including those analysed here at the relatively large sample sizes required for clumped isotope quantification. We recognize the complexity of carbon cycling at the sulfate methane transition zone53, however, as a first-order approximation, here we assume that the δ13C values represent near equal mixtures of DIC produced from AOM (δ13C ranges from –60 to –100‰; in agreement with reported methane values34,37,54,55,56) and the bulk seawater DIC pool (∼0‰). Some cold seep carbonates tend to exhibit δ18Ocarb values above normal marine precipitates (δ18Ocarb of ∼+5‰), consistent with precipitation from fluids associated with clathrate dissociation32. Maximum clumped isotope offsets are achieved when the end-members are most dissimilar19. In Fig. 7a we illustrate how cold seep δ13Ccarb values may relate to potential fractional contributions of methane-derived carbon (fmethane), by assuming a range of potential carbon isotope compositions of this methane (δmeth) and a purely marine DIC end-member (with δ13C=0‰). Many modern and ancient cold seep carbonates exhibit δ13Ccarb values that could reflect equal mixtures between these two end-members (fmethane=0.5) and therefore have the potential to express maximum mixing-related clumped isotope composition offsets.
Two mixing models are explored here to potentially reconcile the Δ47 anomalies (Fig. 7). The first is relevant to a marine bottom water with a temperature of ∼5 °C, consistent with temperatures observed at Hydrate Ridge, Eel River Basin and Costa Rica. This temperature would yield a mineral Δ47 value of ∼0.76. The second simulates Norwegian Sea bottom waters, which exhibit temperatures of ∼–1 °C from which an equilibrium-precipitated carbonate would exhibit a Δ47 value of ∼0.77. Mixing between more dissimilar end-members produces larger possible anomalies19. Here, the isotope compositions of the cold seep end-member include δ13C values of −60, −80 and −100‰, a δ18O value of +5‰ and Δ47 values of 0.71 and 0.72. The isotope compositions of the marine end-member include a δ13C value of 0‰, a δ18O value of 0‰ and Δ47 values of ∼0.76 and 0.77. Mixing models between the end-members described above generally do not produce the magnitude of observed temperature disequilibrium between cold seep carbonates and modern bottom waters (Fig. 7), even though mixing yields the maximum possible offset as constrained by environmental parameters.
AOM rates are variable in modern cold seep systems (Supplementary Fig. 1). Rates commonly correspond to the flux of methane from the deeper subsurface to sulfate-containing fluids. Vent-proximal, advection-dominated methane delivery is generally associated with higher AOM rates, whereas more peripheral, diffusive seepage is generally associated with lower AOM rates57. As this reaction (eq. 1) produces alkalinity in equal molar proportions to the methane reactant, AOM is likely a first-order control on carbonate mineral authigenesis.
The anomalously low Δ47 values exhibited by modern seep carbonates may arise from rapid mineralization, which may allow them to retain an isotopic fingerprint of processes controlling solution disequilibrium, as well as surface kinetic processes. Quantitative models have shown that minerals forming rapidly will have a higher propensity to exhibit geochemical signatures out of equilibrium with the ambient environment58, and recent observations have shown this can apply to clumped isotope signatures40, although recent laboratory-based rapid precipitation experiments can yield equilibrium clumped isotope signatures59. In cold seep settings, mineral precipitation rates are difficult to quantify, so that although there are many reports of AOM rates, authigenic carbonate precipitation rates are rarely available. Where carbonate precipitation and AOM rates have been quantified in the Nile Delta60,61 and Mediterranean Sea62,63 precipitation rates broadly overlap with AOM rates (see Supplementary Fig. 1). Therefore environments exhibiting more rapid AOM rates may also exhibit more rapid carbonate precipitation rates and carbonates expressing more severe disequilibrium behaviour.
The above combination of factors likely explains the large disequilibrium signatures observed in modern seep carbonates. These same processes would be relevant in ancient seeps, and therefore it is reasonable to assume that ancient seeps also exhibit disequilibrium. The ancient seep carbonates measured here all show evidence for apparent temperatures that are too warm to reflect bottom waters. On the one hand, this is consistent with our explanation for modern seep disequilibrium, however, on the other hand, ancient deposits are generally composed of many distinct phases, some perhaps precipitated from warm, later diagenetic fluids11,13.
We suggest that although modern samples record disequilibrium (that is, non-temperature dependent) Δ47 values, ancient samples may have experienced subsequent heating, solid-state re-ordering (Fig. 6) or both that may overprint the signal and randomize 13C–18O bonds from an initial ordering. Complex parageneses have been interpreted for ancient cold seep carbonate cement relationships11,14,15,38. Thus in an ancient seep setting, extremely low Δ47 values could be recorded. In fact, it has been argued that Neoproterozoic Doushantuo carbonates exhibit low Δ47 values consistent with hydrothermal conditions51. However, based on our modern and ancient seep data, an alternative possibility is that the Doushantuo carbonates exhibited substantial disequilibrium Δ47 signatures on initial formation, and that subsequent processes (for example, solid-state re-ordering22) have randomized the signatures from original values. Evidence to support this interpretation stems from our fossil seep carbonates of the Tepee Buttes, which show clumped isotope and δ18Ocarb values more similar to those of Doushantuo carbonates51 than modern seep carbonates.
In conclusion, modern cold seep carbonates exhibit Δ47 values ranging from 0.609 to 0.783‰, significantly lower than equilibrium precipitation would yield. This disequilibrium translates into apparent formation temperatures of −3 up to 52 °C, while modern, seep-proximal bottom waters are all <5 °C. We hypothesize kinetic effects likely arise from a combination of processes, including AOM, DIC speciation effects and mixing, with the rapid precipitation rates in such settings leading to the high potential for incorporation of such kinetic isotope signals into carbonate minerals. In ancient cold seeps these same factors, in combination with burial diagenesis and/or solid-state reordering, can result in extremely low Δ47 values. Ultimately, our findings indicate that cold seep carbonates formed by AOM are susceptible to disequilibrium behaviour and therefore clumped isotopes cannot be used as a strict temperature proxy for the primary formation environment in modern or ancient seeps.
Carbonate samples were collected from modern cold seeps of Hydrate Ridge, off the western coast of Costa Rica, Eel River Basin and the Norwegian Sea (Fig. 1). Micritic and fibrous carbonate phases were mirodrilled from these modern cold seep carbonates. Ancient cold seep carbonates were collected from outcrops of the Quinault, Pysht and Lincoln Creek Formations, the Tepee Buttes and the Panoche Hills (Fig. 1). In addition to micritic and fibrous phases, ancient carbonates also exhibit sparry phases11,14,15,38.
Sample preparation and analyses
Between 8 and 14 mg of powdered sample was used for each measurement. The powders were pretreated in 30%, cold (∼10 °C) hydrogen peroxide to mitigate potential contamination by organic compounds. Some samples were measured in duplicate to evaluate reproducibility. Sample powders were digested in phosphoric acid at 25 or 90 °C (Table 1) and analysed following published protocols64. The resulting CO2 was analysed on a customized Thermo MAT 253 gas source mass spectrometer at UCLA dedicated to measuring clumped isotopes in CO2. A custom-built, automated, online device64 is used to introduce samples to the mass spectrometer.
Values of Δ47 are reported as the per mil (‰) difference relative to what would be predicted given a stochastic distribution of isotopes among all possible isotopologues. Values of Δ47 are determined by calculating δ18O, δ13C, and the abundance of mass-47 isotopologues52. This spectrum of masses along with known fractionation factors for 18O/16O and 13C/12C allows for quantification of carbonate δ18O, δ13C and Δ47 values20. Data are shown in Tables 1 and 2. All Δ47 values are reported on the absolute reference frame (ARF), which is calculated using 25 and 1,000 °C equilibrated gases. These measurements were made before the implementation of a baseline correction scheme.
These Δ47 values were converted to temperature using various calibrations20,40,41,65,66,67,68. Figures and discussion are based on the calibrations by Tang et al.41 and Tripati et al.40 and acid fractionation factor of 0.092‰ (ref. 69), which is within error of the value reported by Defliese et al.65. The acid digestion temperatures, calibrations and fractionation factors yield comparable temperatures (aside from the Dennis and Schrag66 calibration, which significantly lower and produces some impossible temperatures). Carbonate δ13C and δ18O values are reported in ‰ relative to the VPDB standard. The average Δ47 precision based on measurements of carbonate standards and samples during the runs for this study was 0.012‰ (1 s.e.), and select replicate analyses yield an average standard deviation of 0.033‰ (1 s.d.). The average reproducibility of carbonate δ13C and δ18O are 0.006 and 0.011‰, respectively (Tables 1 and 2).
All data pertinent to this manuscript and its reported findings can be found in the manuscript itself or the associated Supplementary Information file.
How to cite this article: Loyd, S. J. et al. Methane seep carbonates yield clumped isotope signatures out of equilibrium with formation temperatures. Nat. Commun. 7:12274 doi: 10.1038/ncomms12274 (2016).
Preliminary discussion and access to some cold seep carbonates provided by Victoria Orphan. Funding for the study was provided to S.L. by the Agouron Geobiology Postdoctoral Fellowship. A.K.T. acknowledges support from the Department of Energy through BES grant DE-FG02-13ER16402.
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