www.nature.com/scientificreports OPEN The possible occurrence of iron‑dependent anaerobic methane oxidation in an Archean Ocean analogue Fleur A. E. Roland1*, Alberto V. Borges1, François Darchambeau1, Marc Llirós2,4, Jean‑Pierre Descy1 & Cédric Morana3 In the ferruginous and anoxic early Earth oceans, photoferrotrophy drove most of the biological production before the advent of oxygenic photosynthesis, but its association with ferric iron ­(Fe3+) dependent anaerobic methane ­(CH4) oxidation (AOM) has been poorly investigated. We studied AOM in Kabuno Bay, a modern analogue to the Archean Ocean (anoxic bottom waters and dissolved Fe concentrations > 600 µmol L−1). Aerobic and anaerobic ­CH4 oxidation rates up to 0.12 ± 0.03 and 51 ± 1 µmol L−1 d−1, respectively, were put in evidence. In the Fe oxidation–reduction zone, we observed high concentration of Bacteriochlorophyll e (biomarker of the anoxygenic photoautotrophs), which co-occurred with the maximum ­CH4 oxidation peaks, and a high abundance of Candidatus Methanoperedens, which can couple AOM to ­Fe3+ reduction. In addition, comparison of measured ­CH4 oxidation rates with electron acceptor fluxes suggest that AOM could mainly rely on ­Fe3+ produced by photoferrotrophs. Further experiments specifically targeted to investigate the interactions between photoferrotrophs and AOM would be of considerable interest. Indeed, ferric ­Fe3+-driven AOM has been poorly envisaged as a possible metabolic process in the Archean ocean, but this can potentially change the conceptualization and modelling of metabolic and geochemical processes controlling climate conditions in the Early Earth. Tropical inland waters and wetlands have been recognized as major sources of methane ­(CH4) to the a­ tmosphere1. While progress has been made in refining the evaluation of the C ­ H4 emission rates, less attention has been given to evaluate the underlying production and loss terms, i.e. methanogenesis and methane oxidation. In modern marine sediments where sulfate (­ SO42−) is more abundant by several orders of magnitude than any other electron acceptor, most of the ­CH4 removal is due to anaerobic ­CH4 oxidation (AOM) coupled to ­SO42− ­reduction2–5. However, ­SO42− abundance is typically much lower in freshwaters compared to marine ecosystems, so that ­CH4 oxidation in anoxic hypolimnion or sediments of lakes might be linked to the reduction of thermodynamically more favorable electron acceptors such as nitrite ­(NO2−)6, nitrate ­(NO3−)7, manganese IV ­(Mn4+) and ferric iron ­(Fe3+)8. Kabuno Bay is a ferruginous, nearly isolated, sub-basin of Lake Kivu (RD Congo) with a marked and distinct physico-chemistry. Primarily due to high hydrothermal activity, a strong and stable stratification is established within Kabuno bay water column throughout the year, with waters being anoxic below ~ 11 m d ­ epth9,10. A con- sequence of this strong stratification is the occurrence of a particularly steep gradient in C ­ H4 and iron (­ Fe2+/ Fe3+) concentrations in the chemocline. Also, anoxic waters of Kabuno Bay are characterized by low sulfide ­(HS−) ­concentrations11. These combined features are rarely encountered in modern environments, Lake Matano (Indonesia) and Lake La Cruz (Spain) being one of the few o ­ thers12, while they were widespread in the Archean ­ocean13. Llirós et al.11 reported the occurrence of a particularly active pelagic Fe cycle driven by photoferrotrophy in Kabuno Bay, with little net Fe oxidation, meaning that Fe reduction processes are tightly coupled to photofer- rotrophic Fe oxidation. In the present study, we measured ­CH4 oxidation rates in the water column of Kabuno Bay, and investigated the potential importance of ­Fe3+ as a terminal electron acceptor for AOM. We hypothesized 1 Chemical Oceanography Unit, Université de Liège, Liège, Belgium. 2Department of Genetics and Microbiology, Universitat Autònoma de Barcelona, Barcelona, Spain. 3Department of Earth and Environmental Sciences, Katholieke Universiteit Leuven (KU Leuven), Leuven, Belgium. 4Present address: Girona Biomedical Research Institute, Salt, Catalunya, Spain. *email: froland@uliege.be Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 1 Vol.:(0123456789) www.nature.com/scientificreports/ that ­Fe3+ could be the main electron acceptor for AOM given the high abundance of Fe species in the water ­ ay11,14. column and the high in situ photoferrotrophic rates previously reported in Kabuno B Material and methods Description of the study site and the sampling device. Kabuno Bay (− 1.6216°N, 29.0497°E; Fig- ure S1) was sampled in May 2013 (late rainy season), September 2013 (dry season) and August 2014 (dry sea- son)15. Vertical profiles of temperature, conductivity, pH and oxygen were obtained with a Yellow Springs Instru- ment (YSI) 6600 V2 multiparameter probe, with a detection limit for dissolved oxygen of 0.01 mg L−1. High amounts of dissolved gases (in particular ­CO2) were present in superficial and deep waters of Kabuno Bay, causing losses of C ­ H4 when samples were brought to the surface. To avoid that, a home-made sampler (Fig- ure S2) was used; sealed ­N2-flushed 60 mL glass serum bottles (SUPELCO, Sigma Aldrich, 33109-U) were fixed on a two-meter high plate, every 0.25 m. Thin needles (0.6 × 25 mm) equipped with non-return valves (valves allowing the water to fill in the bottles but preventing gases to escape from the bottles) penetrated the grey butyl stoppers (WHEATON, USA). The non-return valves were sealed by a butyl stopper. A string was connected to stoppers in series (all stoppers were connected to the same string). The device was immersed at the sampling depth, and the stoppers were removed from the non-return valves by pulling the string, allowing water to enter the bottles through the needle. The system was left under water 10 min to fill the serum bottles. Once the sam- pling device was brought back to the surface, the needles were removed from the butyl stoppers and further processed as described below. Serum bottles were half-filled with water, and the other half was a N ­ 2 headspace. The five main rivers of Kabuno Bay (Figure S1) were sampled every month from November 2013 to June 2014, by the mean of a Niskin bottle. Samples for total Fe and Mn concentrations determination were taken in plastic vials, stored at 4 °C and analyzed as described hereafter. Chemical analyses. Samples for C ­ H4 concentrations were collected in sealed (with butyl stoppers previ- ously boiled in milli-Q water in the laboratory, and aluminium caps) ­N2-flushed 60 mL glass serum bottles, as described above. Two bottles were directly poisoned with 100 µL of H ­ gCl2. ­CH4 concentrations were determined via the headspace equilibration technique and measured by gas chromatography (GC)16, as described by Borges et al.1. The precision of measurements was ± 3.9% and the detection limit of the method is 0.5 nmol ­L−1. Samples for nutrient analyses were collected into 250 mL borosilicate bottles, using the same sampling device as for the gas sampling. Water was then collected from the bottles with a 50 mL-syringe, filtered through a 0.22 µm syringe filter (polyethylsulfone), preserved with 200 µL of H ­ 2SO4 5 N, and stored frozen. Nitrite (­ NO2−) and ­NO3− concentrations were measured by spectrophotometry, by the sulfanilamide ­method17 and the vanadium reduction to N ­ O2− ­method18, respectively, while ammonia ­(NH4+) was determined with the dichloroisocyanu- rate–salicylate–nitroprussiate colorimetric ­method19. ­NO2− and ­NH4+ were quantified on a Thermo Spectronic Genesys 10vis spectrophotometer using a 5-cm light path, and N ­ O3– was determined with a Multiskan Ascent Thermo Scientific multi-well plate reader. The detection limits for these methods were 0.03, 0.15 and 0.3 µmol L−1 for ­NO2−, ­NO3− and ­NH4+, respectively. The concentrations for N ­ O3− and ­NO2− are reported here as ­NOx con- centrations ­(NO3− + NO2−). Nutrients concentrations are not available in May 2013, due to a problem during samples preservation. Samples for ­SO42− and sulfide ­(HS−) concentrations were collected in ­N2-flushed 60 mL serum bottles, by the same sampling method as described above. Water was rapidly filtered after collection through a 0.22 µm syringe filter, and collected in 5 mL Cryotube vials and 50 mL plastic vials for ­SO42− and ­HS−, respectively. Samples were preserved with 20 µL of 20% zinc acetate (ZnAc), for ­SO42− and 200 µL of ZnAc for ­HS−; both samples were then stored frozen. ­SO42− concentrations were quantified by ion chromatography (Dionex ICS-1500, with an autosampler Dionex AS50, a guard column Dionex AG22 and an analytical column Dionex IonPac AS22) and ­HS− concentrations were determined with a Thermo Spectronic Genesys 10vis spectrophotometer, using a 5-cm light path, according to the method described by C ­ line20. The detection limits were 0.5 and 0.25 µmol L−1 for ­SO42− and ­HS−, respectively. Samples for Fe and Mn measurements were collected into sealed ­N2-flushed 60 mL glass serum bottles, with the sampler described above. Water was rapidly transferred from the bottles to the filtration set with a syringe equipped with a tube, and was passed through 25 mm glass fiber ­filters15. Filters were collected in 2 mL Eppendorf vials and preserved with 1 mL of a ­HNO3− 2% solution, while filtrates were collected into four 2 mL Eppendorf vials and preserved with 20 µL of a H ­ NO3 65% solution. Particulate Fe and Mn concentrations were determined from the filters, which were digested with nitric acid in Teflon bombs in a microwave digestion apparatus (Ethos D, Milestone Inc.) and diluted with milli-Q water to a final volume of 50 mL. Dissolved Mn and Fe concentra- tions were determined from the filtrates, which were diluted with milli-Q water to a final volume of 50 mL. Fe and Mn concentrations were determined by inductively coupled plasma mass spectrometry (ICP-MS) using dynamic reaction cell (DRC) technology (ICP-MS SCIEX ELAN DRC II, PerkinElmer inc.). Analytical accuracy was verified by a certified reference material (BCR 715, Industrial Effluent Wastewater). CH4 oxidation rate measurements. Samples for C ­ H4 oxidation incubations were collected in N ­ 2-flushed 60 mL glass serum bottles sealed with butyl stoppers previously boiled in milli-Q water in the laboratory, and aluminum caps, using the sampling device described above. C ­ H4 oxidation was determined following the meth- odology described by Roland et al.21. Briefly, two bottles were immediately poisoned with 100 µL of ­HgCl2 after collection ­(T0), five bottles received an inhibitor of sulfate-reducing bacteria (sodium molybdate, + Mo) and five other did not receive any amendment (− Mo). In May 2013, the molybdate (Mo) solution was prepared directly on the field with milli-Q water stored at ambient temperature and was not flushed, while it was prepared with fresh milli-Q water and was flushed before the transport in September 2013 and August 2014. The bottles of both Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 2 Vol:.(1234567890) www.nature.com/scientificreports/ treatments were incubated in the dark and at constant temperature close to in situ temperature (~ 23 °C). The biological activity in + Mo and – Mo bottles was stopped at ~ 12, 24, 48, 72 and 96 h by the addition of 100 µL of ­HgCl2. ­CH4 concentrations were determined via the headspace equilibration technique and measured by gas chromatography (GC)16, as described by Borges et al.1. The precision of measurements was ± 3.9% and the detec- tion limit of the method is 0.5 nmol L−1. The precision was calculated based on the analysis of the two T ­ 0 bottles sampled in duplicate for each depth and then accounted for the variability induced by the handling of samples (samples collection, storage) and our analytical method. CH4 oxidation rates were calculated as a linear regression of C ­ H4 concentrations over time during the course of the incubation. Table S1 shows standard deviations, initial C ­ H4 concentrations, percentage of C ­ H4 consumed and the time lapse during which the ­CH4 oxidation rates were calculated for each ­depth15. A correction of the C­ H4 oxidation rates has been applied taking into account the potential oxygen supply through the injection of the Mo solution. We considered that a maximum of 2.5 µmol L−1 of O ­ 2 were added to each bottle (250 µL of the solution were added to 30 mL of water). The calculations were made according to Roland et al.21. Only the time change in dissolved C ­ H4 concentration and not the concomitant decrease in the concentration of the electron acceptors potentially involved in ­CH4 oxidation processes were monitored during the incubation. This is due to the interference caused by the ­HgCl2 poison addition with the analytical methods used to determine the electron acceptors concentrations. Vertical flux calculations. The vertical fluxes (­ Fvertical) of ­NH4+, ­SO42−, ­HS−, ­Mn2+ and ­Fe2+ were calculated as described by Pasche et al.22 (Eq. 1): Fvertical = − Dturbulent ∗ Grad + C ∗ Adv (1) where ­Dturbulent is the turbulent diffusion coefficient, Grad is the vertical concentration gradient of each element, C is the concentration of the element at a given depth, and Adv is the upwelling velocity. Vertical fluxes were computed by using a range of turbulent diffusion coefficient and of upwelling velocity of 1.4 × 10–7–1.0 × 10–6 ­m2 s−1 and 6.3 × 10–9–6.3 × 10–8 m s−1, ­respectively14. Contribution to ­CH4 oxidation. Based on these vertical fluxes, the fraction of the integrated AOM rates potentially sustained by Fe reduction, ­NO3− reduction and S­ O42− reduction rates were calculated considering stoichiometry equivalences of 1:1 ­(SO42−:CH4), 8:5 (­NO3−:CH4), 8:1 (Fe(OH)3:CH4) and 4:1 (­MnO2:CH4)8,23, according to the following equations: %SO2− 2− 2− 4 = vertical SO4 flux observed/vertical SO4 flux needed ∗ 100 (2) = vertical SO2− 4 flux observed/integrated AOM rates ∗ 100 %NO− + + 3 = vertical NH4 flux observed/vertical NH4 flux needed ∗ 100 (3) = vertical NH+   4 flux observed/ integrated AOM rates/(5 ∗ 8) ∗ 100 %Fe(OH)3 = vertical Fe2+ flux observed/vertical Fe2+ flux needed ∗ 100 (4) = vertical Fe2+ flux observed/ integrated AOM rates ∗ 8 ∗ 100   %MnO2 = vertical Mn2+ flux observed/vertical Mn2+ flux needed ∗ 100 (5) = vertical Mn2+ flux observed/ integrated AOM rates ∗ 4 ∗ 100.   Bacteriochlorophyll pigments analyses. Samples for pigments analyses were collected every 0.25 m, from 9 to 13 m depth in September 2013, and from 8 to 12 m depth in August 2014. Water was collected with the sampler described above, and filtered through Whatman GF/F 47 mm diameter filters. The filtration volume depended on the depth sampled, but was on average 0.3 L. Filters were preserved in 5 mL Cryotube vials and stored frozen. The pigment extraction was made in 4 mL of 90% HPLC grade acetone. Two 15-min sonication steps separated by an overnight period at 4 °C in dark were applied, and extracts were stored in 2 mL-amber borosilicate vials. HPLC analyses were carried out as described by Sarmento et al.24. Archaeal diversity. Samples for DNA analyses were collected as detailed by Inceoğlu et al.25. Genomic DNA was extracted as previously ­described26 and further subjected to FLX–titanium amplicon ­pyrosequencing27 from collected filters using ARCH 349F (5′-GYGCASCAGKCGMGAAW-3′) and ARCH 806R (5′-GGA​CTA​ CVSGGG​TAT​CTAAT-3′) as sequencing primers targeting the 16S rRNA V3–V4 r­egion27. Reads used in the present study can be accessed through sequencing read archive (SRX349388). Archaeal 454-pyrosequencing sequences from Kabuno Bay water samples tentatively belonging to the Methanosarcinales order were subse- quently analysed for further taxonomic refinement. All sequences were aligned using the SINA a­ ligner28 and then imported into the latest SILVA 16S rRNA-ARB-compatible database (SSURef-132_NR_99_13_12_17_opt. arb; http://www.arb-silva​.de) in ­ARB29. Two base frequency filters (“termini” and “ssuref:archaea”; positional variability by parsimony) were applied to exclude highly variable positions before adding sequences to the origi- nal database using the “parsimony quick add marked” tool from ARB. Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 3 Vol.:(0123456789) www.nature.com/scientificreports/ Figure 1.  Physico-chemical conditions in Kabuno Bay are analogous to the Archean Ocean (a,b: May 2013; c,d: September 2013; e,f: August 2014). (a,c,e): bacteriochlorophyll contents (Bchle, µg ­L−1), dissolved oxygen (DO, µmol ­L−1) and ­CH4 concentrations (µmol L ­ −1), specific conductivity (SPC, µS ­cm−1). (b,d,f): methane oxidation rates (µmol ­L−1 ­d−1) without molybdate added (− Mo) and with molybdate added (+ Mo). Results and discussion Environmental settings in Kabuno Bay. The water column of Kabuno Bay was sharply stratified and anoxic from 11.0 to 11.3 m depth during the three field campaigns (2013–2014; Fig. 1, Figure S3). Chemocline co-occurred with the oxycline. Methane was abundant in anoxic waters (up to ~ 200 µmol L−1 at 13 m) but its concentration decreased abruptly at the bottom of the chemocline to relatively modest values (0.1–1.1 µmol L−1), indicative of vigorous microbial C ­ H4 oxidation. Ferruginous Kabuno Bay hypolimnion was characterized by high ­Mn2+ and ­Fe2+ concentrations (up to 55 and 600 µmol L−1, respectively; Figs. 1, 2). Dissolved Mn and Fe concentrations declined in the C ­ H4 gradient, and were mirrored by an accumulation of particulate Mn and Fe species. Sulfate concentrations were relatively high in the chemocline and did not change substantially within the ­CH4 gradient, while H ­ S− concentrations were always two orders of magnitude lower than S­ O42− (i.e., lower than 1.0 µmol ­L ), with the exception of a maximum peak (10 µmol ­L−1) detected at 9.5 m depth in September 2013 −1 (Fig. 2). The vertical fluxes of the potential electron acceptors for AOM and their reduced forms are shown in Table S2. Five main rivers enter Kabuno Bay and are sources of Fe and Mn to the lake. Based on data gathered during a monthly monitoring of these rivers, we estimated that they supplied the lake with 3.3 mmol m−2 d−1 of F ­ e3+ oxide and 0.1 mmol m−2 d−1 of M ­ n4+ oxide. Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 4 Vol:.(1234567890) www.nature.com/scientificreports/ Figure 2.  Vertical profiles of electron acceptors potentially involved in AOM (a–c: May 2013; d–g: September 2013; h–k: August 2014). (d,h): NOx and ­NH4+ concentrations (µmol ­L−1). (a,e,i): ­SO42− and ­HS− concentrations (µmol ­L−1). (b,f,j(: particulate ­(MnO2) and dissolved (­ Mn2+) Mn concentrations (µmol L ­ −1). (c,g,k(: particulate ­(Fe3+) and dissolved (­ Fe2+) Fe concentrations (µmol L­ −1). Electron acceptors sustaining AOM in Kabuno Bay. Methane oxidation rates in oxic waters (maxi- ­ −1 ­d−1 observed in May 2013) were one order of magnitude lower than those in anoxic mum of 0.12 ± 0.03 µmol L waters with maximum rates of 51 ± 1 (at 11.5 m depth), 21 ± 4 (at 11.5 m) and 48 ± 7 (at 12.0 m) µmol L−1 d−1 in May 2013, September 2013 and August 2014, respectively (Fig. 1). Methane removal in anoxic waters by aerobic organisms has been found to be supported by oxygenic photosynthesis in the well-illuminated (10% of incident PAR) chemocline of Lake ­Cadagno30. Kabuno Bay chemocline is located below the photic zone so that light conditions (0.1–1% PAR) do not appear suitable to support significant phytoplankton activity. Pigments analysis Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 5 Vol.:(0123456789) www.nature.com/scientificreports/ Figure 3.  Presence of Candidatus Methanoperedens, capable of Fe-related AOM. 16S rRNA gene phylogenetic tree of the Candidatus Methanoperedens representative related OTUs (0.03 cut-off; only those OTUs containing more than 10 reads are shown) retrieved by pyrosequencing from Kabuno Bay water samples, the scale bar indicates 0.10 fixed point mutation per nucleotide position. carried out during our study revealed that the abundance of bacteriochlorophyll e (Bchl e), a pigment distinctive of low light adapted anoxygenic photoautotrophs Green Sulfur Bacteria (GSB)31,32, was at least one order of mag- nitude higher than chlorophyll a in the chemocline (Figs. 1 and S4). Also, Morana et al.14 showed that 74 ± 13% of particulate biomass in the chemocline derive from anoxygenic ­CO2 fixation by GSB. These multiple lines of evidence indicate that biological primary production in the chemocline is largely dominated by anoxygenic photoautotrophs so that a cryptic oxygen cycle sustained by oxygenic photosynthesis in Kabuno Bay anaerobic waters can be ruled out. Nevertheless, we cannot rule out the possibility of punctual and/or episodic oxygen incursions in the anoxic waters, which could explain the presence of ­NOx below the oxycline in September 2013. This oxygen could be rapidly used by aerobic ­CH4 oxidation, and the part of aerobic ­CH4 oxidation in the water column of Kabuno Bay might be more significant than reflected by the results of our in vitro incubations. However, in the particular conditions of our in vitro incubations, we could estimate that 89–98% of the C ­ H4 was oxidized under anoxic conditions, raising the question which electron acceptors supported AOM. The water column was particularly rich in ­SO42−, but ­SO42− concentrations did not decrease substantially with depth in the chemocline (Fig. 2), neither in anoxic waters. Indeed, S­ O42− reduction rates reported by Llirós et al.11 were relatively low compared to S­ O42− concentrations and were ca. 10 times lower than the AOM rates. Furthermore, except in May 2013 where AOM rates were lower with Mo added (what can be linked to the slightly different methodology used), our in situ incubation experiments revealed that AOM rates were up to 6 times higher (Sep- tember 2013 and August 2014) in presence of Mo, an inhibitor of ­SO42− reduction (Fig. 1), contrary to what would have been expected if ­CH4 oxidation depended on S­ O42− reduction. All these multiple lines of evidence suggest that ­SO42− reduction did not sustain a significant part of the C ­ H4 oxidation in the chemocline of Kabuno Bay. Similarly, it seems unlikely that Mn oxides and N­ O3− would fuel a substantial part of AOM. Their concentrations were always low, and the upward fluxes of ­Mn2+ and ­NH4+ could only have sustained at most 4% and 25% of the AOM rates, considering an extreme scenario where the totality of M ­ n2+ and N ­ H4+ fluxes, once oxidized, would be exclusively involved in Mn oxides or ­NO3–dependent AOM, which is unlikely. Instead, it has been showed that denitrification and N­ O3− reduction to ­NH4+ (DNRA) linked to Fe oxidation occur in the water column of Kabuno ­Bay33. As both these processes are thermodynamically more favorable than N ­ O3– driven AOM, we hypothesized − that the N­ O3 formed in the water column of Kabuno Bay is rapidly consumed by DNRA and denitrification coupled to Fe oxidation rather than by N ­ O3–driven AOM, which can also explain the low N ­ O3− concentrations. − Therefore, it is likely that AOM coupled to ­NO3 reduction did not occur at a significant extent in Kabuno Bay. On the other hand, Llirós et al.11 showed that F ­ e3+ reduction in Kabuno Bay was ca. 24 times higher than 2− ­SO4 reduction. This study also reported the existence of an important Fe-related bacterial community in the water column of Kabuno Bay, among which Chlorobium phaeoferrooxidans, a GSB capable of Fe o­ xidation34 was the dominant member. Here, we showed that Bchl e, a specific biomarker of the GSB, was mainly located in the Fe oxidation–reduction zone, which co-occurred with the maximum C ­ H4 oxidation peaks (Fig. 1). 16S-RNA gene based pyrosequencing data from February 2012 showed the presence of an archaeal community related to Candidatus Methanoperedens nitroreducens (the most abundant retrieved OTUs showed 94.6 and 93.7% sequence similarity, respectively, against Candidatus Methanoperedens nitroreducens (JMIY01000002); Fig. 3 and Table S3). The peaks of abundance of these archaea co-occurred within the Fe oxidation/reduction zone and the maximum occurrence of photoferrotrophy previously reported by Llirós et al.11 (Fig. 4). Overall, putative AOM-related archaea in Kabuno bay represented ca. 16% of the whole community in February 2012. Recent studies have Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 6 Vol:.(1234567890) www.nature.com/scientificreports/ Figure 4.  Co-occurence of Candidatus methanoperedens and ferrophototrophs in the chemocline of Kabuno Bay. (a) Vertical distribution of Candidatus methanoperedens and (b), Vertical profiles of particulate Fe concentrations (µmol L−1) and Bacteriochlorophyll e (Bchle) content (µg L−1) in February 2012. While this profile was not contemporary to the measurements of AOM (Fig. 1) the particulate Fe and Bacteriochlorophyll e peaks show that AOM and Archaea abundance coincided. shown that microbes belonging to the Candidatus Methanoperedens archaeal group (Order Methanosarcinales) are particularly versatile, and can couple AOM with different electron acceptors, among which Fe, depending on environmental c­ onditions35,36. Cai et al. recently demonstrated that these archaea were capable to catalyze Fe-linked AOM alone, without a bacterial partner, via the “reverse methanogenesis” pathway and possibly using a extracellular electron transport ­pathway37. Despite that these prokaryotes diversity data were acquired during a different sampling c­ ampaign25 than the AOM measurement reported here, the good agreement between (1) high Candidatus methanoperedens abundance and high Bchl e concentrations in the Fe oxidation–reduction zone in 2012, and (2) high AOM rates and high Bchl e concentrations in the Fe oxidation–reduction zone dur- ing this study, allow to hypothesize that Candidatus methanoperedens could represent the dominant microbes thriving AOM during the present study. Accordingly, these AOM-associated archaea (AAA​5) could therefore be responsible for the Fe-related AOM measured in Kabuno bay, taking into account that AOM coupled to Fe reduction is thermodynamically more favorable than coupling with other electron a­ cceptors38. Iron-driven AOM has already been suggested as a domi- nant ­CH4 removal pathway in other ferruginous environments (i.e.38–40). Bacterial data reported from samples collected in 2012 evidenced that photoferrotrophs were responsible for the oxidation of 37 mmol Fe m−2 d−1 11. Comparison of this Fe oxidation rate with AOM showed that F ­ e3+ released via photoferrotrophy could potentially fuel an important fraction of the AOM (up to 31% in September 2013), in contrast to N ­ O3− and S­ O42− reduction ­rates11,33, which could only fuel up to 5% of the AOM observed (Fig. 5). Furthermore, the observation of higher AOM rates when Mo was added may result from the higher availability of Fe oxides when sulfate-reducing bacteria (SRB) activity was inhibited. Indeed, ­SO42− reduction produces ­HS− that can rapidly reduce Fe oxides to form iron sulfides, which could precipitate and then be unavailable for Fe-dependent C ­ H4 oxidizers. Fe is known to be efficiently recycled in the chemocline of ferruginous l­ akes38 or bioturbated marine ­sediments41. Overall, process rate measurements and metagenomics data suggest that an intense biotic regeneration of ­Fe3+ mediated by photoferrotrophs could provide an important fraction of the electron acceptors required to oxidize ­CH4 anaerobically in Kabuno Bay. Following the same approach as Jones et al.42 and assuming steady state conditions, the rate of Fe or Mn leaving the water column via sedimentation must equals the rate of Fe or Mn input in Kabuno bay’s water column via the rivers. Assuming that Mn and Fe leave the water column as a ­Mn2+ or F ­ e2+ mineral, all the oxidized Mn or Fe must ultimately be reduced, and the downward flux of par- ticulate ­Fe3+ should be equivalent to the input of Fe via the rivers (3 mmol m−2 d−1) and the upward flux of ­Fe2+ (4–33 mmol m−2 ­d−1). If we consider that the totality of this downward flux of particulate F ­ e3+ is reduced within Kabuno bay’s chemocline, but that only 3 mmol Fe m−2 ­d−1 finally leave the mixolimnion, we estimated that Fe would be recycled up to 11 times before removal by sedimentation. Consequences on representation of the Archean ocean metabolism. A strong interaction between photoferrotrophs and ­CH4 oxidizers has been hypothesized in several other modern Archean ocean analogues, such as Lake ­Matano38 and Lake La ­Cruz43. Under the ferruginous conditions of Archean oceans, photoferrotrophs would have been responsible for most of the primary production of the primitive ­Earth12. It is also generally assumed that a much larger fraction of the organic matter generated by primary producers would have been processed by methanogens than nowadays, given the absence of oxic and S­ O42− driven mineralization of organic matter in the ­O2 and ­SO42− depleted waters of the early Earth ­Ocean44,45. Pavlov et al.46 estimated that up to 250 Tmol year−1 (1.9 mmol m−2 d−1, assuming an ocean area of 3.6 × 1014 ­m2) of C ­ H4 would have been emitted during the Archean, hence C ­ H4 would have been a key component of the Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 7 Vol.:(0123456789) www.nature.com/scientificreports/ Figure 5.  Chemical evidence of ­Fe3+ as an important electron acceptor of AOM. Fraction (%) of the integrated AOM rates potentially sustained by Fe reduction, ­NO3− reduction and S­ O42− reduction rates measured by Llirós et al.11 and Michiels et al.33. Error bars are calculated as the standard deviation of the mean of the three sampling campaigns. ancient C cycle, with important consequences on the early Earth climate, as the higher ­CH4 concentrations (~ 100 ppmv) in the atmosphere are thought to have provided enough greenhouse warming to compensate for a 5–17% fainter Sun. The photochemical decomposition of C ­ H4 in the atmosphere and the resulting escape of hydrogen to space may also have participated to the oxidation of the Earth surface e­ nvironment47. However, geological archives do not provide constraints on the magnitude of the ­CH4 concentrations, and large ­CH4 fluxes are calculated with quantitative models that limit the existence of Fe-dependent ­CH4 oxidation and assume a negligible role of S­ O42− driven C­ H4 oxidizers. This paradigm has recently been challenged by Olson et al.48 and Sauterey et al.49 who showed that the combined effects of competition between methanogens and S­ O42− reducers and occurrence of S­ O42− driven ­CH4 oxidation would have effectively reduced the ­CH4 fluxes from the ocean even at modest S­ O42− concentrations, and regardless of O ­ 2 concentrations. Similarly, we propose that strong interac- tions between photoferrotrophs and Fe-dependent C ­ H4 oxidizers might have exerted an important control on the Archean–Proterozoic ­CH4 cycling. For instance, modelled photoferrotrophic primary production in early Earth ferruginous ocean (3.8 mmol m−2 d−1 50) would have produced Fe oxides at a rate of 15.3 mmol m−2 ­d−1, assuming a 4:1 ratio between Fe oxidation and C fixation by photoferrotrophs. Although simplistic given the complexity of the C and Fe biogeochemical cycle, comparison of this rate of Fe oxides production with the sea- to-air ­CH4 flux (1.9 mmol m−2 d−1) proposed by Pavlov et al.46 suggests that photoferrotrophy would have been high enough to potentially support the oxidation of 100% of the ­CH4 flux to the early atmosphere. In Kabuno Bay, a modern analog to early Earth ocean, measured photoferrotrophy rates would have been sufficient to sustain a smaller (31 ± 18%, n = 3), but still important, part of the oxidation of the ­CH4 flux measured during this study (19 ± 11 mmol m−2 d−1, n = 3). It has been hypothesized that the rise of atmospheric oxygen about 2.4 Gyr ago (Great Oxidation Event) was triggered by a decrease of atmospheric ­CH4 ­levels51. This has been attributed to an increased importance of ­SO42 reduction in the oceans that outcompeted the methanogenic organisms, although this explanation is not consistent with geological ­records52. It has also been hypothesized that the production of methane decreased in response to the decrease of the nickel inputs to oceans, as this is a key metal for methanogen ­enzymes53. Alternatively, it was showed that supplying a culture media with nickel does not stimulate m ­ ethanogenesis54. A widespread occurrence of AOM coupled to Fe oxidation offers an alternative explanation that would have led to the decrease of dissolved C ­ H4 in the ocean and consequently the emission of C ­ H4 to the atmosphere, thus going in the direction of the study of Riedinger et al.39. This is consistent with the revision of the putative composition of the Archean a­ tmosphere55 that suggests that the amount of greenhouse warming by C ­ H4 was more limited than previously ­thought49,56. While we can hypothesize that Fe(OH)3 sustaining AOM was initially provided by photoferrotrophy, the onset of oxygenic photosynthesis would also have been an ample supply of Fe(OH)3, available to sustain AOM, from the oxidation of F ­ e2+ with dissolved O­ 2 released by oxygenic photoautotrophs (Fig. 6). This might also provide an explanation to the modest but significant increase in Fe-using genes from the Archean to the Proterozoic given by the phylogenomic ­analyses57. A decrease of dissolved ­CH4 concentrations due to Fe-dependent AOM could have had several other consequences on the timing and sequence of Archean and Proterozoic events. The decrease of atmospheric C ­ H4 would have led to a decrease of H ­ 2 and CO generation by photolysis, which in turn would have led to a decrease of supply of H ­ 2 and CO to surface oceans, contributing to the demise of pelagic ­H2-methanogens and CO-acetogens (Fig. 6), that is usually attributed exclusively to the inhibition of these anaerobic organisms by increasing O ­ 2 level. Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 8 Vol:.(1234567890) www.nature.com/scientificreports/ CO Methane photolysis CH4 H2 Atmosphere Ocean Fe2+ x H2-methanogenesis x x hν hν CO-acetogenesis CO2 CH2O + O2 Fe2+ CH2O + Fe(OH)3 CH2O + CH4 H2 CO CO 2 + CH3OOH Oxygenic photosynthesis CO2 CO2 H2O Photoferrotrophy Fe2+ + CO2 CH4 Iron-oxide AMO Acetate-methanogenesis Figure 6.  Potential role of iron-oxide AOM in Archean Ocean metabolism. In the Archean Ocean, anaerobic metabolism (photoferrotrophy, methanogenesis and CO-acetogenesis in dark blue) dominated before the advent of oxygenic photosynthesis (in light blue). In red, we propose anaerobic methane oxidation (AOM) using Fe oxides as electron acceptor as additional metabolic process. Before the advent of oxygenic photosynthesis, F ­ e3+ dependent AOM linked photoferrotrophy and H ­ 2-methanogenesis that so far have been seen as two parallel and unconnected processes. After the advent of oxygenic photosynthesis, Fe oxides-dependent AOM might have used the abundantly produced Fe(OH)3 from the oxidation of F ­ e2+ by ­O2 to further remove ­CH4 from the water column, facilitating the increase of O ­ 2 in the atmosphere and the great oxidation event. Finally, the great oxygenation event was shortly afterwards followed by a low latitude glaciation that would be associated to lower atmospheric ­CH4 concentrations. 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Scientific Reports | (2021) 11:1597 | https://doi.org/10.1038/s41598-021-81210-x 10 Vol:.(1234567890) www.nature.com/scientificreports/ Acknowledgements We thank the team of the Observatoire volcanologique de Goma (OVG) for their involvement in sampling, Bo Thamdrup (University of Southern Denmark) for the access to his laboratory, Bruno Leporcq (University of Namur), Renzo Biondo (University of Liège), Dina Holmgaard Skov and Heidi Grøn Jensen (University of Southern Denmark) for help in measurements, Jack Middelburg and Steven Bouillon for comments on the draft and the three anonymous reviewers and associated editor for their valuable contribution. We also thank Thibault Lambert (University of Liège) for the elaboration of the map (Figure S1). This study was funded by the Belgian Federal Science Policy Office (BELSPO, Belgium) under the EAGLES (East African Great lake Ecosystem Sensitivity to Changes, SD/AR/02A) project, by the Fonds National de la Recherche Scientifique (FNRS) under the MICKI (Microbial diversity and processes in Lake Kivu, 1715859) project, and contributes to the European Research Council (ERC) starting grant project AFRIVAL (African river basins: Catchment-scale carbon fluxes and transformations, 240002). GC apparatus was acquired with funds from the FNRS (Contract No. 2.4.598.07). AVB is a senior research associate at the FNRS. FAER had a PhD grant from FNRS (« Fonds pour la formation à la Recherche dans l’Industrie et dans l’Agriculture »—FRIA) and is now post-doctoral researcher at the FNRS (Project No. X.3007.17 funded by the Walloon Institute of Sustainable Development). This study shows results mainly obtained during FAER’s Ph.D., and the “Material and methods” section has been mostly described in the resulting unpublished thesis. Author contributions F.A.E.R., A.V.B and F.D designed the study, and F.A.E.R and F.D. carried out the field data collection. J.-P.D. car- ried out the HPLC measurements, M.Ll. carried out the archaeal diversity analyses. F.A.E.R. and C.M. drafted the manuscript, which was substantially commented upon and amended by A.V.B. All co-authors approved the manuscript. Competing interests The authors declare no competing interests. Additional information Supplementary Information The online version contains supplementary material available at https​://doi. org/10.1038/s4159​8-021-81210​-x. Correspondence and requests for materials should be addressed to F.A.E.R. Reprints and permissions information is available at www.nature.com/reprints. 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