Microbial activity, methane production, and carbon storage in Early Holocene North Sea peats
- 1Department of Earth Sciences, Vrije Universiteit Amsterdam, De Boelelaan 1085, 1081 HV Amsterdam, the Netherlands
- 2Department of Microbiology, Institute for Water and Wetland Research, Radboud University, Heyendaalseweg 135, 6525 AJ Nijmegen, the Netherlands
- 3Netherlands Earth System Science Center, Utrecht University, Heidelberglaan 2, 3584 CS Utrecht, the Netherlands
- 4TNO – Geological Survey of the Netherlands, Princetonlaan 6, 3508 TA Utrecht, the Netherlands
- 5Department of Applied Geology and Geophysics, Deltares Research Institute, Daltonlaan 600, 3584 BK Utrecht, the Netherlands
- 6Department of Microbiology & Biogeochemistry, Royal Netherlands Institute for Sea Research, Landsdiep 4, 1797 SZ 't Horntje, the Netherlands
- 7Department of Earth Sciences, Faculty of Geosciences, Utrecht University, Princetonlaan 8a, 3584 CB Utrecht, the Netherlands
- 8Centre for Arctic Gas Hydrate (CAGE), Environment and Climate, Department of Geosciences, UiT The Arctic University of Norway in Tromsø, Tromsø, Norway
- 9Soehngen Institute of Anaerobic Microbiology, Radboud University, Heyendaalseweg 135, 6525 AJ Nijmegen, the Netherlands
- These authors contributed equally to this work.
Correspondence: Tanya J. R. Lippmann (email@example.com)
Northern latitude peatlands act as important carbon sources and sinks, but little is known about the greenhouse gas (GHG) budgets of peatlands that were submerged beneath the North Sea during the last glacial–interglacial transition.
We found that whilst peat formation was diachronous, commencing between 13 680 and 8360 calibrated years before the present, stratigraphic layering and local vegetation succession were consistent across a large study area. Large carbon stores were measured. In situ methane (CH4) concentrations of sediment pore waters were widespread but low at most sites, with the exception of two locations.
Incubation experiments in the laboratory revealed molecular signatures of methanogenic archaea, with strong increases in rates of activity upon methylated substrate amendment. Remarkably, methanotrophic activity and the respective diagnostic molecular signatures could not be detected. Heterotrophic Bathyarchaeota dominated the archaeal communities, and bacterial populations were dominated by candidate phylum JS1 bacteria.
In the absence of active methanogenic microorganisms, we conclude that these sediment harbour low concentrations of widespread millennia-old CH4. The presence of large widespread stores of carbon and in situ methanogenic microorganisms, in the absence of methanotrophic microorganisms, holds the potential for microbial CH4 production if catalysed by a change in environmental conditions.
The expansion and submersion of northern latitude peatlands play a key role in global methane (CH4) and carbon (C) cycles (e.g. Charman et al., 2013; Morris et al., 2018). Globally, peatlands serve as long-term carbon sinks (Clymo et al., 1998; Gorham, 1991) that store more carbon than the world's forests combined despite covering only 3 % of the world's surface land area (Xu et al., 2018). At the time of the Last Glacial Maximum (LGM), peatlands stored 600 000 Tg C worldwide (Yu et al., 2010). This estimate is calculated using ocean-basin-scale peat layer thickness and depth. Few in situ observations of peat deposit properties are available to quantify uncertainty.
Methane is globally the second most prevalent greenhouse gas (GHG), with emissions to the atmosphere amounting to 550–594 Tg CH4 each year (Saunois et al., 2020). Continental shelves and deltas are important sinks within the global carbon cycle (Oppo et al., 2020; Saunois et al., 2020) and are responsible for 80 %–85 % of oceanic carbon sequestration (Muller-Karger et al., 2005). Shelf regions contribute ∼ 75 % of global ocean CH4 flux to the atmosphere, with estimates of seepage from oceanic shelves into bottom waters ranging between 6–12 Tg CH4 yr−1 (Weber et al., 2019) or 16–48 Tg CH4 yr−1 (Judd et al., 2002). Reducing the uncertainties in these estimates requires further work at both regional and global scales (Oppo et al., 2020; Saunois et al., 2020). High CH4 concentrations in surface waters of continental shelves are due to CH4 inputs from estuaries and seafloor sediments, where methanogenesis is fuelled by high organic matter (OM) sedimentation (Carr et al., 2018; Zhuang et al., 2018). Methane entering the water column from the seafloor arrives by ebullition and pore water diffusion and is of either biogenic or thermogenic origin.
Variations in atmospheric CH4 are due, in part, to the changing extent of peatlands over glacial–interglacial periods (Frolking and Roulet, 2007). Triggered by postglacial sea level rise and, consequently, rising groundwater, peatlands (now basal peats) in the area between the Netherlands, the United Kingdom, and Denmark (now the North Sea) developed by the process of paludification in the Late Pleistocene and Early Holocene (Fig. 1a). During the Late Pleistocene and Early Holocene, strong glacio-isostatic adjustments (GIAs) resulted in the isostatic subsidence of the North Sea basin (Hijma et al., 2012; Vink et al., 2007), and, combined with rapid melting of polar ice sheets, high rates of sea level rise, up to 1–2 cm yr−1 (Hijma and Cohen, 2019), gave rise to paludification, peatland development, and later peatland submersion (now basal peats).
Until now, only one vegetation record has documented the Late Pleistocene peatland ecosystem submerged beneath the North Sea basin (Wolters et al., 2010). The record began with an open birch (Betula) woodland, impacted by a carr vegetation, consisting mostly of Willow (Salix) due to early influences of paludification 10 700 calibrated years (cal yr) before the present (BP). Subsequently, brackish reed (Phragmites), salt marsh vegetation with Chenopodiaceae, developed due to marine inundation ca. 9350 cal yr BP. The period of succession spanned 1300 years (Wolters et al., 2010). A high degree of peatland plant community variability results from the highly heterogeneous, irregular, and micro-ecosystem nature of peatlands (Clymo et al., 1998). It is likely that concurrent sea-level-independent terrestrialization occurred in isolated topographic features (e.g. local pools, valleys, streams), impacting local vegetation succession.
Microbial surveys of phylogenetic or functional gene markers have shown that bacterial community composition is generally distinct between different types of ecosystems, e.g. peatlands (Cadillo-Quiroz et al., 2006), estuarine and marine sediments (Purdy et al., 2002), tundra, and permafrost (Ganzert et al., 2007). Marine microbial communities are highly diverse and include many uncultured phylotypes (Fry et al., 2008). Community composition is often similar between ecosystems with common environmental parameters (Kim et al., 2018), but there is a lack of knowledge of the microbial processes contributing to the production of CH4 in submerged peat deposits globally and in the North Sea in particular.
Microbial activity plays a large role in the biological CH4 cycle and is estimated to be responsible for reducing annual seabed CH4 emissions to the atmosphere by 1–35 Tg CH4 (Saunois et al., 2020) or 8–65 Tg CH4 (Reeburgh, 2007). In other words, 50 %–90 % of CH4 produced below ground is estimated to have been oxidized before reaching the atmosphere (Frenzell and Karofeld, 2000). Numerous studies have measured CH4 fluxes from present-day peatlands (e.g. Hendriks et al., 2007; Tiemeyer et al., 2016). Microbial CH4 production is performed by methanogens that carry out the final steps in the anaerobic degradation of OM. Methanogenesis is countered by the activity of methanotrophic microorganisms that oxidize CH4 to carbon dioxide (CO2) using a variety of electron acceptors (in 't Zandt et al., 2018). The relative activity of methanotrophic vs. methanogenic microorganisms plays a determining role in CH4 emissions to the earth's atmosphere (Frenzell and Karofeld, 2000).
In most North Sea surface waters, CH4 concentrations are typically < 0.005 µM L−1 (Borges et al., 2016; Niemann et al., 2005). However, much higher CH4 concentrations (1.1 µM L−1), among the highest in the world, are observed in the southern North Sea water column off the coast of Belgium (Borges et al., 2016). The release of CH4 from blowout craters linked to gas exploration could contribute to the high CH4 concentrations in the water column in the North Sea (Schneider von Deimling et al., 2015; Steinle et al., 2016), but the basin-scale impacts are uncertain (Rehder et al., 1998).
Despite extensive efforts to map these submerged peatland ecosystems (Treat et al., 2019; Xu et al., 2018), basal peats remain hard to reach, meaning accessing and measuring CH4 stores remain challenging, limiting in situ measurements (Dean et al., 2018). Consequently, these deposits are omitted from the global accounting of C and CH4 budgets of marine sediments (Saunois et al., 2020). Whilst the results of seismic surveys indicate large stores of naturally occurring biogenic CH4 within the North Sea basal peat deposits (Missiaen et al., 2002), the presence of CH4 has not been confirmed or quantified by in situ observations.
We derive the following hypotheses to describe the palaeo-peat ecosystem submerged beneath the North Sea. Firstly, we hypothesize that CH4 is present within basal peat deposits beneath the North Sea. This is based on seismic signatures indicating large pockets of an unconfirmed gas in the submerged peat layer off the coast of Belgium. Secondly, considering that seismic surveys indicate that these gas pockets are without cracks and sealed off from underlying geological CH4 stores, we hypothesize that CH4 present in the basal peats is produced in the present day by methanogenic microorganisms. Thirdly, because the peatland ecosystem went through distinct changes from establishment to cessation influenced by groundwater paludification due to sea level rise during the Late Pleistocene and Early Holocene, we expect similar plant macrofossil sequences across the North Sea basin, according to the influence of sea level rise on local groundwater. Finally, we hypothesize that microbial populations will be influenced by carbon, mineral, and nutrient availability, depending on the plant macrofossil sequence, and we tentatively expect microbial populations to vary according to the plant macrofossil sequence.
To provide a better understanding of submerged basal peats and their role in the global C, CO2, and CH4 cycles, we present in situ CH4 concentrations and OM content of North Sea basal peat deposits. Plant macrofossil analysis was performed to determine plant community composition and describe the habitat available to microorganisms. Radiocarbon dating was carried out to determine the timing of peatland initiation and cessation. The 16S rRNA gene amplicon sequencing was performed to determine microbial diversity, and batch incubation experiments were conducted to investigate actual and potential microbial CH4 cycle activity in the submerged peat deposits. We compare the results across sites.
2.1 Study area
The study region (Fig. 1b) spans 150 km east to west, bordering the United Kingdom (3∘ E) and the barrier islands of the Netherlands (5∘ E), and 371 km north to south, extending from the latitude of 52 to 56∘ N. This region includes the Dogger Bank, Frisian Front, and the Brown Bank, with ocean depths ranging from 19 to 60 m. A total of 34 cores were collected across 22 sites (see Supplement Table S1 for the location and analysis details of all cores and sites). To carry out multiple sampling procedures, we used more than one core per site with the aim of comparing results across sites, not within sites. Each sampling method uses one core per site. Cores, sites, and sampling are documented in Table S1. In this paper, we refer to the site names except in places where the specific core number is relevant. The sites were named according to nearby shipwrecks using EMODnet (EMODnet, 2018) with the exception of the Darci site.
Methane measurements were performed at all sites. Four sites in the Vlieland (Vittorio, Max Gundelach, Senator Westphal SW, Westland) and Dogger Bank (Dorthea Shallow SW, Dorthea SSW, Dorthea NW, Fredricksborg NE) regions were chosen for microbial sequencing analysis and microbial activity studies, respectively. Loss on ignition (LOI) was performed on these eight sites. These sites are a focus of this paper. Two sites were chosen for plant macrofossil analysis (Vittorio and Fredricksborg NE) and radiocarbon dating. All cores were photographed and texturally described at the facilities of TNO-GDN (Geological Survey of The Netherlands; Bosch, 2000) and are available at https://www.dinoloket.nl.
2.2 Sediment sampling
Short vibrocores (3–4.5 m) were collected during two separate cruises in June 2017 and July 2018 on board the research vessel Pelagia. Before the cruise, digital maps of peat occurrences in the southern North Sea were prepared using the DINO digital database of the TNO-GDN (Van Der Meulen et al., 2013). Based on these maps, areas were selected for geophysical research using sub-bottom profiler and sparker systems. The seismic profiles were directly interpreted on board to identify the presence and depth of basal peat beds. The seismic data were used to select sampling sites from a range of water depths and latitudes and within the maximum penetration depth of the vibrocorer (4.5 m below the seabed). At each site, two or three cores were collected. Before sampling, or after (in the case of CH4 sampling only), the cores were cut into 1 m sections. From one core, CH4 samples were taken as soon as the core was on deck. One of the three recovered cores was cut lengthways following recovery. Sediment for molecular analysis was sampled immediately after opening the core sections and frozen at −80 ∘C until further analysis. Subsequently, pore water samples were collected, and sedimentary samples were taken to determine porosity. All sections were stoppered, sealed at the base and the top, and stored in a refrigerated container (4 ∘C).
2.3 Sediment analysis
Loss on ignition (LOI) analysis was performed at 2 cm resolution within peat layers and 10 cm resolution in non-peat layers at the eight sites corresponding to the sites of the molecular analyses. Organic matter (OM) content (in %) was measured using a Leco® TGA701 thermogravimetric analyser at Vrije Universiteit Amsterdam. Dried samples were crushed and weighed, and the mass loss was measured stepwise during the heating of the samples from room temperature to 1000 ∘C. Here, we present the mass loss at 330 ∘C (LOI330) and 550 ∘C (LOI550). Fixed volume subsamples (42.39 cm3) were used to measure volumetric water content, bulk density, and porosity (cm3 cm−3). These samples were saturated with deionized water, weighed, dried at 60 ∘C for 5 d, and then re-weighed. The bulk density of the sediment was calculated by dividing the volume of the dried sediment by the dry mass. Total pore space (porosity, φ) was calculated by subtracting the measured volumes of water from the original fixed sample volume. The total C pool was estimated using Eq. (1), a general equation used to estimate peatland carbon stocks (Sheng et al., 2004). To estimate the total CH4 pool, Eq. (2) is an adaptation of Eq. (1). The minimum and maximum peat thicknesses provide uncertainty estimates of the total C and CH4 pools, respectively.
where A, D, ρ, and OMC represent the area, peat thickness, bulk density, and OM to C conversion factor (for this peatland type), respectively. CH4 concentration is calculated considering porosity (∅).
2.4 Methane sampling
The sampling and measurement of CH4 concentrations followed standard protocols for headspace sampling and analysis of marine sediments (Egger et al., 2015, 2017; Reeburgh, 2007). Prior to coring, the core liner was pre-drilled with 2 cm diameter holes at 10 cm resolution and taped to be gas-tight. Upon retrieval and working with speed, the top and bottom of the core were sealed immediately, and custom-made metal syringes were inserted into each taped hole. A total of 10 mL of sediment was extracted and deposited into a 65 mL glass bottle filled with a saturated sodium chloride (NaCl) solution. Each bottle was sealed with a butyl rubber stopper and a screw cap and stored upside down at 4 ∘C. In the laboratory of the Vrije Universiteit Amsterdam, the CH4 bottles were prepared for analysis. A total of 10 mL of nitrogen (N2) was injected into each CH4 bottle (with a needle inserted through the septum, allowing excess water to escape) to create a headspace. From this headspace, a subsample was collected with a gas-tight syringe and injected into a Thermo Finnigan TRACE™ gas chromatograph (equipped with a flame ionization detector – FID) at Utrecht University. Methane concentrations were calculated using calibrations from standard gases and measured sediment porosity.
2.5 Pore water analysis
Samples for pore water analysis were extracted using 5 cm long porous polymer soil moisture sampler rhizons (Rhizosphere Research Products B.V., the Netherlands) at 10 cm resolution and stored at 4 ∘C. The samples were acidified with 1 % HNO3 and analysed by inductive coupled plasma optical emission spectrometry (ICP-OES) for Al, Ca, Fe, K, Mg, Mn, Na, P, S, Si, and Zn (iCap 6300, Thermo Scientific, Waltham, MA) and continuous flow analysis (CFA) for NO, NH, PO, Na+, K+, and Cl− (Bran + Luebbe AutoAnalyzer, SPX Flow, Norderstedt, Germany; Seal Analytical AutoAnalyzer 3, Seal Analytical, Southampton, UK; Table S2).
2.6 Molecular analyses
Four cores in the southern North Sea were selected for 16S rRNA amplicon sequencing, and four cores from the Dogger Bank area were selected for microbial activity studies. Unfortunately, the cores from the first sampling expedition did not provide enough material to perform both sequencing and the incubation experiments. Therefore, we chose to divide the microbial experiments over multiple sites in order to obtain the maximum amount of information possible whilst taking the experimental constraints into consideration.
2.6.1 DNA isolation
Samples for DNA isolation were immediately extracted aseptically upon sampling. Samples were stored at −20 ∘C until further analysis. DNA was extracted in duplicate per sample using the Qiagen DNeasy PowerSoil Kit (Qiagen, Venlo, the Netherlands) following the manufacturer's instructions with the following modifications: the initial PowerBead Tube vortex step was carried out using a TissueLyser LT (Qiagen, Venlo, the Netherlands) at 50 Hz for 10 min (min), and the primary centrifugation step was increased to 1 min at 10 000 × g. DNA was eluted with 2×30 µL of sterile Milli-Q incubated for 2 min at room temperature prior to centrifugation. The second elution centrifugation step was carried out for 1 min at 10 000 × g. DNA quality was assessed by agarose gel electrophoresis, spectrophotometrically using a NanoDrop 1000 (Invitrogen, Thermo Fisher, Carlsbad, CA, USA) and fluorometrically using the Qubit™ dsDNA HS Assay Kit (Invitrogen, Thermo Fisher, Carlsbad, CA, USA) according to the manufacturer's instructions. Duplicate samples with the highest yield and quality were selected for downstream application.
2.6.2 Amplicon sequencing and analysis
For DNA purification, the QIAquick PCR Purification Kit was used (Qiagen, Venlo, the Netherlands). For DNA amplification, a two-step amplicon sequencing protocol was used. In the first step, the V3–V4 region of the bacterial 16S rRNA gene was amplified using the universal primers Bac341F (5′-CCTACGGGNGGCWGCAG-3′) (Herlemann et al., 2011) and Bac785R (5′-GACTACHVGGGTATCTAATCC-3′) (Klindworth et al., 2013) for 30 cycles. Archaeal 16S rRNA genes were amplified with the universal archaeal primers Arch349F (5′-GYGCASCAGKCGMGAAW-3′) (Takai and Horikoshi, 2000) and Arch806R (5′-GGACTACVSGGGTATCTAAT-3′) (Takai and Horikoshi, 2000) for 30 cycles. The total PCR reaction volume was 25 µL with 1 µL forward and 1 µL reverse primer (20 µM), 1 µL template, 12.5 µL 2× concentrated SYBR™ Green PCR Master Mix (Thermo Fisher, Carlsbad, CA, USA), and 9.5 µL sterile Milli-Q. All primers were purchased from Biolegio (Biolegio B.V., Nijmegen, the Netherlands).
The following cycling parameters were used for polymerase chain reaction (PCR): initial denaturation for 10 min at 98 ∘C; cycles of denaturation for 1 min at 95 ∘C, annealing for 1 min at 60 ∘C, and elongation for 2 min at 72 ∘C; and a final elongation step for 10 min at 72 ∘C. The primers were tested in an annealing temperature gradient experiment, and 60 ∘C was determined as the optimal temperature for initial amplification. The annealing temperature of 60 ∘C was selected because we observed intense bands of the correct amplicon and no observable primer dimers at this temperature. PCR products were purified using the QIAquick PCR Purification Kit (Qiagen, Venlo, the Netherlands) in two elution steps. A 20 µL aliquot of 55 ∘C Milli-Q water was added to the spin column and incubated for 2 min prior to centrifugation. Next, the eluate was added to the spin column, incubated at 55 ∘C for 2 min, and centrifuged again as described in the manual. The purified PCR products were used in a second 10-cycle nested PCR performed with ion torrent adapters using the PCR protocol described above. After purification with the QIAquick PCR Purification Kit as described earlier, the PCR products were used for library preparation and sequencing steps according to the manufacturer's instructions (Life Technologies, Carlsbad, CA, United States).
Samples were sequenced on an Ion 318 Chip Kit v2 (Thermo Fisher, Waltham, MA, USA). Amplicon sequences were quality checked for chimeras and clustered into operational taxonomic units (OTUs) with a 97 % identity cut-off value using the 454 SOP (http://www.mothur.org/, last access: 18 May 2020) (Schloss et al., 2009) with ion torrent modified protocols in May 2018. Chimeras were checked with the UCHIME algorithm version 4.2.40 (Edgar et al., 2011), and singletons were removed (Fig. S1). Taxonomy was assigned according to the SILVA v132 database using the default, “mothur”, taxonomy assigner (Schloss et al., 2009). Data visualization was performed using the “vegan” package (version 2.5-6) in R (Oksanen et al., 2019). All alpha diversity indices were calculated with the OTU-based alpha diversity analysis tool summary.single of “mothur”. Non-metric dimensional scaling (NMDS) plots were prepared in R using the “vegan” and “MASS” (version 7.3-5.0) packages after pre-filtering of non-abundant OTUs (Venables and Ripley, 2002). OTUs with a sum of ≤ 1 per sequencing dataset were removed from the OTU table. NMDS ordination was performed with the metaMDS function of “vegan”. Data were processed by square root transformation and Wisconsin double standardization. We want to stress that biases associated with PCR-based amplicon studies can result in an observed absence of specific microbial clades and results need to be interpreted with care.
2.6.3 PCR quantification and quantitative polymerase chain reaction
The 16S rRNA gene copy numbers were quantified with the archaeal and bacterial primers described above, except that for bacterial quantification, the primer Bac806R (5′-GGACTACHVGGGTWTCTAAT-3′) (Caporaso et al., 2012) was used. Quality and size checks were performed by agarose gel electrophoresis. All quantitative polymerase chain reaction (qPCR) reactions were performed using PerfeCTa Quanta master mix (Quanta Bio, Beverly, MA) and 96-well optical PCR plates (Bio-Rad Laboratories B.V., Veenendaal, the Netherlands) with optical adhesive covers (Applied Biosystems, Foster City, CA). All reactions were performed on a C1000 Touch™ thermal cycler equipped with a CFX96 Touch™ Real-Time PCR Detection System (Bio-Rad Laboratories B.V., Veenendaal, the Netherlands); a maximum of 1 ng of DNA template was used per reaction. Negative controls were prepared for each run by replacing the template with sterile Milli-Q water. Standard curves were constructed with a 10-fold serial dilution of a quantified copy number of pGEM® T Easy plasmids containing inserted Illumina primer PCR fragments of the archaeal and bacterial 16S rRNA genes (Promega, Madison, WI) (de Jong et al., 2018). All qPCR data were analysed using Bio-Rad CFX Manager version 3.0, using the default settings for defining the detection threshold and efficiencies (Bio-Rad Laboratories B.V., Veenendaal, the Netherlands). All qPCR efficiencies were above 90 %.
2.7 Incubation experiments
Sediment cores for the activity study were drilled on 27 and 28 June 2018 and stored for 10 months at 4 ∘C until further processing. Material was taken aseptically from the carbon-rich (dark black/brown) peat layer and stored in sterile 50 mL falcon tubes kept on ice at 4 ∘C during transport. A total sediment slurry volume of 1.5 L was obtained by mixing 750 g (0.5 L Vol) of peat with artificial seawater (0.546 M Cl−, 0.469 M Na+, 0.0528 M Mg2+, 0.0282 M SO, 0.0103 M Ca2+, 0.0102 M K+, 0.0012 M CO, 0.000844 M Br−, 0.000091 M Sr2+, 0.000416 M B−, 0.00935 M NH, 0.00367 M PO) (Dickson and Goyet, 1994) amended with 1 mL L−1 1000× trace element solution SL-10 with 24 mg L−1 CeCl3 ⋅ 7H2O, 30 mg L−1 Na2SeO3 ⋅ 5H2O, and 40 mg L−1 Na2WO4 ⋅ 2H2O (DSMZ) and adjusted to pH 7.0. Under continuous mixing, 50 mL sludge aliquots were transferred to 120 mL sterile glass serum bottles. The bottles were sealed with airtight butyl rubber stoppers and capped with open top aluminium crimp caps. All incubations were carried out in triplicate per condition.
Methanogenic incubations were carried out anoxically with acetate (20 mM), H2 CO2 (20 mM H2 with 20 % CO2 in headspace), H2 methanol (10 mM H2, 10 mM MeOH), and trimethylamine (20 mM). For methoxydotrophic methanogenesis, incubations were started with methoxyphenol (MPH; 3 mM) and trimethylbenzoate (3 mM). For sulfate-dependent methanotrophy, samples were incubated with 28.2 mM sulfate, the concentration present in the artificial seawater, and 5 % (∼ 2 mM) 13C–CH4. The anoxic control incubations were unamended. Anoxic conditions were created by three 15 min cycles of vacuuming and subsequent gassing for 3 min with 1 bar overpressure. The overpressure was removed before starting the incubations. The gas mixture contained 80 % N2 and 20 % CO2 except for the incubations for hydrogen-dependent methylotrophic methanogenesis, which were gassed with 100 % N2. To remove trace oxygen, 0.5 mL of 150 g L−1 L-cysteine HCl and 0.5 mL of 150 g L−1 Na2S were added. To inhibit excessive growth of sulfate-reducing bacteria, a sterile sodium molybdate solution was added at a final concentration of 1.5 mM to all incubations with H2 (Banat Nedwell and Balba, 1983). A new dose of 10 mM H2 was added to the H2 CO2 incubations at 30 and 49 d of incubation and to the H2 methanol incubations at 35 and 49 d of incubation. A second dose of 10 mM MeOH was added to the H2 methanol incubations at 63 d of incubation.
For aerobic methanotrophic incubations, air was used as the headspace and amended with 10 mM CH4. Oxic control incubations contained only air. All substrate concentrations were calculated based on a liquid volume of 50 mL and assuming that all of the substrate dissolved over time.
For substrate consumption rates, the per cubic centimetre substrate conversions were calculated by dividing the total substrate conversion numbers by 16.67 cm3, which corresponds to the quantity of compacted peat sediment inoculated per batch incubation.
Substrate and product analysis
Gas samples (50 µL) were withdrawn with a gas-tight glass syringe (Hamilton, Reno, NE) and injected into an HP 5890 gas chromatograph (Hewlett Packard, Palo Alto, CA) equipped with a Porapak Q mesh (Sigma Aldrich, Saint Louis, MI) and a flame ionization detector (FID) for CH4 detection and a thermal conductivity detector (TCD) for measuring H2, CH4, and CO2 simultaneously using N2 as the carrier gas. An Agilent 6890 series gas chromatograph coupled to a mass spectrometer (Agilent, Santa Clara, CA) equipped with a Porapak Q column heated at 80 ∘C with He as the carrier gas was used for measurements of 13CO2, 13CH4, and O2.
2.8 Plant macrofossil analysis
Two sites, the Max Gundelach site and the Fredricksborg NE site, were selected for plant macrofossil analysis. The Max Gundelach site is in the southern North Sea near the coast of the Netherlands (53∘20′ N, 4∘51′ E), and the Fredricksborg NE site is in the Dogger Bank region (55∘49′ N, 3∘26′ E).
The Max Gundelach site was analysed with low sample resolution but high taxonomic resolution, showing the main peat components and an overview of the less abundant taxa. As the less abundant taxa were, in this research, not highly relevant, we analysed the Fredricksborg NE site with high sample resolution but low taxonomic resolution, showing only the main peat components. The sites can be compared based on the main peat components.
From the Max Gundelach core, eight samples (slices with a thickness of 1 cm or, in two cases, 2 cm and a volume ranging from 8 to 11 cm3) for plant macrofossils were taken every 10 cm. From the Fredricksborg NE core, 15 subsamples were taken with a resolution ranging from 1 to 4 cm and volumes ranging from 3 to 8 cm3. The samples were heated near the boiling point in 5 % NaOH solution and then gently washed through a 150 µm mesh sieve with tap water. After sieving, the plant macrofossils were stored in a known volume of water. The sample material was systematically examined at 15 to 40× magnification using a stereomicroscope.
The main peat components (monocot epidermis, brown mosses, Sphagnum spp.) of both cores were quantified based on the quadrat and leaf count (QLC) method (Barber et al., 1994, 2003) using 15 averaged quadrat (1×1 cm) counts under low power (10×) magnification using a 10×10 square grid graticule. The main peat components were expressed as percentages (%). The complete samples were scanned for quantification of the less abundant macrofossils, in the case of the Max Gundelach core, and seeds, fruits, leaves, and fragments of mosses were picked out, counted, and expressed as concentrations per unit of volume. Rare taxa are reported as presence. Preservation of the peat deposits was estimated qualitatively during analysis based on the preservation of the macro fossils: poorly preserved (+), intermediately preserved (), and well preserved (). The diagram was constructed with Tilia version 1.7.16 (Grimm, 2004).
2.9 Radiocarbon dating
For radiocarbon dating purposes, the top and bottom 1 cm of the peat layers were sieved and searched for autochthonous terrestrial plant macrofossils or, in the absence of such fossils, charcoal (Hijma and Cohen, 2010). If a 1 cm thick section did not contain enough macrofossils, material from the subsequent centimetre was added. The selected macrofossils were sent to the Centre for Isotope Research (Groningen, the Netherlands) for AMS radiocarbon dating. All radiocarbon ages were calibrated using OxCal 4.3 software (Bronk Ramsey, 2009) with the INTCAL13 curve (Reimer et al., 2013).
3.1 Basal peats vary in thickness, formed on Pleistocene sands, capped by marine clays
The localized nature of this palaeo-landscape is apparent in the lithostratigraphic differences observed between and within sites (Fig. 2). The four sites (Fig. 2a–d) chosen for 16S rRNA gene-based sequencing and the four sites (Fig. 2e–f) used in incubation experiments to investigate the potential role of in situ microbial communities are a focus of the results. Peat was recovered at all sites except Easting Down, Stormvogel, and the Darci site. Whilst seismic signals at the Easting Down and Stormvogel sites indicated the presence of a peat layer, the peat was beyond the range of the vibrocorer at the Easting Down and was a peat-like gyttja (highly organic lacustrine sediment) at the Stormvogel site. At all other sites, peat deposits lie upon Pleistocene sands, capped by marine clays. At some sites, the overlying clay layer was stratified with marine sands (i.e. Dorthea Shallow SW, Dorthea SSW, Dorthea NW, Fredricksborg NE; Fig. 2e–h, respectively). Pleistocene sands lie 2–4 m (m) beneath the seafloor (m b.s.f.) in the southern North Sea and 1–3 m b.s.f. in the Dogger Bank region, capped by basal peat layers 80–120 and 10–30 cm thick in the southern North Sea and Dogger Bank regions, respectively.
Non-erosive contact transitions exist between the peat layer and both the immediate upper and lower sedimentary layers at 17 of the 22 sites. In most cases, the peat was covered by a clay layer that formed under lagoonal, low-energy conditions. However, some cores show erosional contacts at the top of the peat beds – i.e. Fredricksborg NE (Fig. 2h), Fredricksborg NW, and Dorthea NW sites (Fig. 2g) – that may be linked to marine transgressions in the area, likely related to waves or tidal currents. The clay sediment directly above the peat layer at the Vittorio site, approximately 1 m, was the thickest clay deposit retrieved in this study. In comparison, the nearby Max Gundelach site has clay deposits capping the peat that are ∼ 35 cm thick. At the other sites, the clay deposits capping the peat layer range from 5 to 50 cm. Max Gundelach, a southern site in the Vlieland region, and Fredricksborg NE, a northern site in the Dogger Bank region, were determined to be representative of the local onset and termination of peat development, respectively, and were therefore selected for macrofossil analysis.
3.2 Methane concentrations are low, widespread with localized high concentrations
The average CH4 concentration of the sediment pore waters was 2.1 µmol L−1, with a maximum concentration of 32.8 µmol L−1 at the Vittorio site (Fig. 3). A total of 10 sites had CH4 concentrations lower than the study average, i.e. < 2 µmol L−1: TX24, Theodor, Mahren S, Easting Down, Leda, Dorthea Shallow SW, Dorthea NNW, Dorthea NW, Fredricksborg NE, and Easting Down. A total of 10 sites had CH4 concentrations similar to or above the study average, i.e. >2 µmol L−1: Vittorio, Max Gundelach, U21, Senator Westphal, Westland, Fredricksborg NW, Stormvogel, Dorthea Deep SW, Darci site, and Dorthea Shallow SW. One of the two cores retrieved from the Dorthea Shallow SW site had low CH4 concentrations, while the second had high CH4 concentrations. Overall, we found approximately equal numbers of sites with high and low CH4 concentrations, across varying thicknesses of peat layers (Fig. 3), latitudes, and depths beneath the seafloor (Table S1).
3.3 Peatland establishment and cessation
At the Max Gundelach site in the Vlieland region, radiocarbon dating revealed that active peat formation prevailed for approximately 2000–3000 years longer than at the Fredricksborg NE site in the Dogger Bank region (Table 1). The basal peat layer of the Max Gundelach site was approximately 85 cm thick, and radiocarbon dating revealed that an active peatland persisted for 3470 years between 11 760 and 8290 cal yr BP, a far longer period than at the Fredricksborg NE site where the peat layer was only 10 cm thick. At the Fredricksborg NE site, dating indicated that an active peatland persisted during an earlier and shorter 800 year period between 13 680 and 12 880 cal yr BP. Macrofossil analysis denoted that peat accumulation occurred through paludification due to a rising water table at sites.
3.3.1 Local vegetation succession in the southern North Sea
At the Max Gundelach site, wet terrestrial vegetation was present at the start of peat accumulation 11 760 cal yr BP, with the presence of Carex spp. (Fig. 4a). A certain degree of open water was present as remains of invertebrates (Chironomid head capsules, Cladocera) together with Characeae oospores were found. These green algae are characteristic of lake waters in pioneer conditions with inputs of minerogenic material (Mauquoy and Van Geel, 2007) and therefore indicative of eutrophic conditions.
At 180 cm beneath the seabed, Cladocera resting eggs were found, suggesting harsher conditions for these invertebrates. All other open-water taxa disappeared. From a depth of 170 cm onward, the environment became nutrient-poor, as evidenced by the dominance of Sphagnum magellanicum. S. magellanicum is an important contributor to ombrotrophic peat bogs with a constant water table (Siebel and During, 2006). Remains of woody plants, in the form of leaf scars, and charcoal were also present at this depth. This indicates the presence of vascular plants during peatland growth. S. magellanicum declined and the brown moss Tomentypnum nitens, a species no longer occurring in the Netherlands, became the main peat-forming component at 160 cm depth. T. nitens is an indicator species of mineral-rich fens, highlighting a change from nutrient-poor to nutrient-rich conditions. The presence of T. nitens indicates that calcium and nutrient-rich groundwater were seeping into the terrestrial environment (Bohncke et al., 1984; van Geel et al., 2020; Hedenäs and Kooijman, 1996). From 150 cm depth onward, T. nitens was replaced by Warnstorfia sarmentosa and Drepanocladus sp. Both species are brown mosses, further indicating a transition to wet mesotrophic conditions. Carex sp. (sedges) rootlets were found in the top of the peat sequence.
3.3.2 Local vegetation succession at Dogger Bank
In the lower part of the Fredricksborg NE core (Fig. 4b), from 191 cm onward, a change from nearly purely minerogenic substrate (LOI550 is ca. 1 %) to slightly higher LOI550 values (ca. 6 %, Fig. S2) points to the presence of a sparse pioneer vegetation. In the three lower samples, megaspores of Selaginella selaginoides were found. S. selaginoides is a heliophilous (needing/tolerating a high level of direct sunlight) circumpolar boreal-montane species growing in damp neutral to alkaline conditions, including dune-slacks, fens, flushes, mires, and short upland grassland (Tobolski and Ammann, 2000). In northern Scandinavia it occurs in mires, at lake margins, and in damp heath meadows (Bjune et al., 2004). Peat formation by paludification began at 183 cm depth, evidenced by a sudden increase (to 75 %) in OM when incinerated at 550 ∘C.
The plant macrofossil content of the peat deposits in Fredricksborg NE (Fig. 4b) is dominated by bryophytes, Sphagnum, and brown mosses. Peat accumulation began with Sphagnum papillosum, quickly followed by the brown moss Tomentypnum nitens and subsequently by the brown mosses Warnstorfia sp. and Drepanocladus sp. Sphagnum papillosum is a typical moss of an acidic raised bog, but in the Netherlands it also occurs in fenland areas, as well as sand regions, including dune slacks, e.g. on the Wadden Islands (Bryologische en Lichenologische Werkgroep, 2015).
3.4 Estimating CH4 storage, OM, and CO2 equivalents
The study area (116 km by 372 km; Fig 1b) spans a surface area of 43 158 km2, an area larger than the land surface of the Netherlands (41 865 km2). Based on the average peat thickness of 0.29 m (min: 0.07 m; max: 0.88 m), the estimated volume of peat is 12.4 km3 (min: 3.0; max: 38.0 km3). Multiplying this estimated volume by the average observed CH4 concentration (2.14 µmol L−1), we estimate that 0.411 Tg CH4 (min: 0.100; max: 1.256 Tg CH4) is present in the study area.
Carbon storage and its CO2 equivalent were calculated using the estimated peat volume of 12.4 km3 and 103 kg m−3, the average OM density of compressed peat in the Netherlands (Erkens et al., 2016). This volume of peat is estimated to hold 740.8 Tg C (min: 180.4; max: 2270.1), assuming the convention that dry peat biomass has a carbon concentration of 0.5 g C g−1 (Gorham, 1991; Heijmans et al., 2008). This is equivalent to 2716.2 Tg CO2 (min: 661.5; max: 8323.8), if released into the atmosphere, assuming a conversion of soil C to CO2 of 1.00 : 3.67 (Van den Bos, 2003).
3.5 Variations in OM between local environments
Scatter plots show the LOI when incinerated at 330 and 550 ∘C with depth (Fig. S2). OM loss at 330 and 550 ∘C follow comparable trends at all sites. There was a general ceiling of not more than 50 % loss at LOI 330 ∘C. OM loss at 330 ∘C was highest at the Vittorio (core 6.2) and Fredricksborg NE (core 111.0) sites. Large (80 %) OM loss when incinerated at 550 ∘C was observed at all sites, except at the Theodor site. The thickness of the peat layer at the Theodor site was 8 cm, thinner than the mean peat layer thickness (0.29 m). The Fredricksborg NE site was distinct from the other sites because the difference in LOI when incinerated at 330 and 550 ∘C was small, indicating that a higher portion of material was incinerated at a lower temperature.
3.6 Methanogenic archaea actively perform methylotrophic methanogenesis
To investigate the potential of the in situ microbial community for CH4 cycling (schematic of process, Fig. 1a), batch incubations were prepared with an anoxic slurry of artificial seawater and freshly collected peat sediment and amended with a range of methanogenic substrates. Pore water analysis indicated that the peat layers were converted into a marine ecosystem (Table S2). The peat deposits at Dorthea Shallow SW, Dorthea SSW, Dorthea NW, and Fredricksborg NE showed active CH4 production upon incubation, with a strong increase in rates of production upon methylated substrate amendment (Fig. 5). Molecular analysis showed that methanogens were present at all four assessed sites: Westland, Senator Westphal, Max Gundelach, and Vittorio (Fig. 6).
Methane production in the unamended control incubation was very low, indicating that most, if not all, of the labile OM fraction of the peat sediments has already been mineralized. Methane accumulation was observed subsequent to the addition of methylated substrates (Fig. 5) after a lag phase of 2 weeks, indicating that the CH4-producing microbial community could be quickly metabolically revived. In the incubation with H2 and MeOH, CH4 production was solely linked to MeOH, which was confirmed upon amendment with MeOH after depletion of H2.
Amendment with hydrogen and CO2 (H2 CO2) and acetate, two common substrates for methanogenic archaea, did not induce CH4 production within the period of incubation (60 d). Even though no methanogenesis was observed, the concentration of H2 CO2 changed. This may be indicative of competition for substrates, likely by sulfate-reducing microorganisms facilitated by abundant sulfate supplies that penetrate up to metres deep into the sediment in marine environments (Jørgensen, 1983) or, in this case, incubations with ample supplies of sulfate. Amendment with methoxyphenol (MPH) and trimethoxybenzoate (TMB), substrates used by methoxydotrophic methanogens, did not induce CH4 production, and a TMB concentration of 3 mM appeared to be inhibitory to the methanogenic community. Neither aerobic nor anaerobic methanotrophic activity was observed, indicating the absence of an in situ biological CH4 filter (Figs. S3, S5).
3.7 Microbial community composition
16S rRNA gene quantification shows the dominance of archaea over bacteria in all cores. Archaeal and bacterial abundances in each core section were assessed by qPCR. In all cores, archaea were more abundant than bacteria (Table S3 and Fig. S4). Cores 6 and 7 had archaea-to-bacteria ratios of 7.0 and 9.0, whereas cores 17 and 26 had ratios of 55.1 and 43.9, respectively. Archaeal 16S rRNA gene copy numbers ranged from 1.3 to 8.1×107, while bacterial 16S rRNA gene copy numbers ranged from 1.7 to 3.2×106.
3.7.1 Dominance of Bathyarchaeota and prevalence of methanogenic archaea
Bathyarchaeota dominated the archaeal communities at all locations, with an average relative abundance of 71 % (range 35.9 %–92.2 %). The relative abundance of Bathyarchaeota was highest at the Max Gundelach site, with an average of 86 % of the archaeal 16S rRNA gene reads. The phylum Bathyarchaeota is a potentially metabolically diverse microbial group that is found in a wide range of organic-rich environments, including deep-sea and freshwater sediments (Evans et al., 2015). Among the four sites for which DNA sequencing was performed, methanogenic archaea were detected at Vittorio, Max Gundelach and Westland but not Senator Westphal S (Figs. 6 and S4). Methanogenic archaeal species belonging to Methanomassiliicoccaceae were detected in these three cores, whereas Methanoregulaceae were only observed at Max Gundelach. The Max Gundelach site contained the highest relative abundance of methanogenic archaea, with an average of 10.3 %, compared to averages of 3.9 % and 3.0 % at the Vittorio and Westland sites, respectively.
Lokiarchaea were most abundant at the Vittorio site (32.2 %) and were present in only low abundance at the Westland site (2.8 %) and below the 2 % threshold at the other sites (Fig. 6). Marine Benthic Group D and DHVEG-1 were more abundant at the Senator Westphal S and Westland sites (30.3 % and 21.2 %, respectively) and were present only in low abundance at the Vittorio and Max Gundelach sites (1.4 % and 2.7 %, respectively). Genomic analysis of the Asgard candidate phylum “Candidatus Lokiarchaeota” has indicated the potential for an acetogenic lifestyle, hydrogen dependency, and mixotrophic potential (Sousa et al., 2016; Spang et al., 2019).
3.7.2 Diverse bacterial communities dominated by candidate phylum JS1
Candidate phylum JS1 dominated the bacterial communities, with an average relative abundance of 22.9 % (Fig. 6). The highest relative abundances, 33.7 % and 26.3 %, were observed at the Vittorio and Max Gundelach sites, respectively. Dehalococcoidia were mainly observed at the Vittorio and Max Gundelach sites, with respective abundances of 12.3 % and 18.4 %. At the Senator Westphal S and Westland sites, the abundances of Dehalococcoidia were low, with averages of 1.6 % and 0.8 %, respectively. The JS1 lineage is a subgroup of the candidate phylum Atribacteria (Nobu et al., 2016). Metabolic reconstructions have indicated the potential of JS1 bacteria for fermentative metabolism and syntrophic acetate oxidation (Lee et al., 2018). Aerophobetes and GIF9 phylum bacteria were more characteristic of the Senator Westphal S (6.7 %) and Westland (8.1 %) sites and were present only in low abundance at the Vittorio (1.6 %) and Max Gundelach (0.8 %) sites. Candidate GIF9 bacteria were only detected at the Senator Westphal S (3.4 %) and Westland (7.2 %) sites. In addition, MSB.5B2, TA06, SBR1031, Pla_1 lineage (Senator Westphal S site only), Pirellulales (Senator Westphal S site only), and Phycisphaerales (Westland site only) were unique to specific cores.
3.7.3 Archaeal and bacterial diversity analyses
Archaeal species diversity was greater at the Senator Westphal S (Simpson: 0.24; Shannon: 2.13) and Westland (Simpson: 0.19; Shannon: 2.85) sites than at the Vittorio (Simpson: 0.21; Shannon: 2.28) and Max Gundelach (Simpson: 0.23; Shannon: 1.96) sites (Fig. S6a). The archaeal community structure was similar among the cores, as supported by non-metric multidimensional scaling (Fig. S7).
The high microbial diversity of these peat sediments was reflected in the alpha diversity indices. Compared to inundated mangrove peat soils, the bacterial alpha diversity in the North Sea peat sediments sampled in the present study was higher (Shannon diversity of up to 5 vs. 2.81; Fig. S6b.) (Chambers et al., 2016). The indicators of diversity observed here were comparable to or higher than those observed in tropical peat swamp forests in Thailand (Shannon diversity of 5.07) and Indonesia (2.0–2.5), but the largest estimated Chao1 index was much higher (1054 for Thailand peat vs. 1500–4500 observed in our study) (Chambers et al., 2016; Kwon et al., 2016).
These findings indicate that basal peats have the potential to function as CH4 storage facilities and may improve global inventories of marine carbon, CO2, and CH4.
4.1 Origins of this newly measured CH4 store
These findings confirm the long held hypothesis that pools of CH4 are present in North Sea basal peats (Judd et al., 1997; Missiaen et al., 2002). We estimate 0.411 Tg CH4 remains trapped within these basal peats. Peatlands in the present-day North Sea basin developed due to rising groundwater linked to postglacial sea level rise and were rapidly capped by marine clays and sand deposits. It is likely that the rapid inundation of the peatland led to the production of large volumes of CH4 by methanogenic microbial populations. Seismic surveys of the southern North Sea have indicated that CH4-containing pockmarks are likely of biogenic origin due to a lack of observed underlying marine seeps that would be a necessary conduit of geological CH4 into shallow sediments (Missiaen et al., 2002). Whilst seismic studies in the northern North Sea hypothesized that CH4-containing shallow sand sediments are of both biogenic and geological origin due to ascending gas emission pathways through the sediment, these pathways have not been observed (Hovland and Judd, 1988; Hovland et al., 1987; Niemann et al., 2005).
We see two potential explanations for the production of biogenic in situ CH4 in these basal peats. Firstly, this CH4 may have been produced during the postglacial flooding of active peatlands in the region that is now the North Sea basin, and without sufficient methanotrophic metabolization, remains were trapped by overlying sediment in basal peat deposits. Alternatively, the CH4 may have been produced in the present day, with the activity of methanogens exceeding the activity of methanotrophs.
Whilst the incubations show that methanogenic populations were revived within a 2 week window, methanogens were not observed to be active in the present day (Fig. 5). Further, microbial-activity-based analyses show that neither aerobic nor anaerobic methanotrophic prokaryotes were activated by oxic or anoxic incubations. Therefore, we did not observe processes indicating biogenic CH4 may have been produced in the present day.
Whilst the processes of diffusion, ebullition, and methanotroph metabolization of CH4 are likely to have occurred during the postglacial flooding of peatlands, pools of CH4 may remain if inhibited by a sufficiently dense, sufficiently rapidly deposited overlying sediment layer. The overlying sediment layers may be sufficiently dense to inhibit upward gas diffusion and ebullition. It is likely that the compacted nature of basal peats impacts the diffusion of CH4 through the sediment (Grunwald et al., 2009).
We conclude that in the observed absence of active methanogenic and methanotrophic microbial populations, the in situ CH4 observed in this study is trapped pockets of millennia-old CH4. This supports previous seismic studies not undertaken in situ that have indicated that pools of CH4 are present in the basal peats beneath the North Sea but contradicts the hypothesis that this CH4 was produced in the present day (Missiaen et al., 2002). Future studies may consider isotopic analysis to confirm the origin.
4.2 In the context of the global CH4 budget
Due to unattributable changes in atmospheric CH4 concentrations in the last decade, quantification of the global CH4 budget has been a focal point of discussion in the literature. In these quantification efforts, wetland emissions provided the largest source of uncertainty (Saunois et al., 2020). Methane present in basal peats went unaccounted for and is therefore underrepresented in these CH4 accounting efforts.
For comparison with global CH4 inventories, the estimated 0.411 Tg CH4 present in these submerged sediments is equivalent to almost one quarter of the annual biogenic oceanic CH4 emissions (2 Tg CH4 yr−1) (Saunois et al., 2020), 1 month of the global growth of atmospheric CH4 that occurred during the years 2000–2009 (5.8 Tg yr−1), or 1.5 weeks of the global atmospheric CH4 growth that occurred in 2017 (16.8 Tg yr−1) (Saunois et al., 2020).
The CH4 concentrations of 1–30 µmol L−1 observed in the peat layer of the middle and southern North Sea in the present study are an order of magnitude higher than background concentrations measured in shallow North Sea sediments (< 0.1 µmol L−1; Niemann et al., 2005; Steinle et al., 2016) and much higher than concentrations observed in the water column (maximum of 1.1 µmol L−1; Borges et al., 2016), with the exception of muddy sediments like those of the Helgoland Bight, where observed CH4 concentrations reached values of up to 6 mmol L−1 (Aromokeye et al., 2020). Borges et al. (2016) reported average CH4 concentrations in the water column of 0.139 µmol L−1 (near-shore) and 0.024 µmol L−1 (off-shore) and a maximum concentration of 1.128 µmol L−1.
Due to a lack of published research, it is not possible to compare the CH4 concentrations measured here with those of other basal peat deposits. Compared to studies that have measured CH4 concentrations in marine sediments (Egger et al., 2016, 2017; Niemann et al., 2005; Steinle et al., 2016), the geographic expanse of this study area is large. At all sites, CH4 concentrations were above previously reported background concentrations of shallow sediments and background concentrations of bottom seawater. The broad distribution of the sample locations (study area in Fig. 1a; 43 158 km2) is indicating that this dataset has reliably captured the variability of the CH4 concentrations present in southern and mid-North-Sea basal peats. The CH4 concentrations measured in this study are higher than those measured in the water column in the same area (Zhuang et al., 2018). The Darci site is influenced by a known biogenic CH4 gas seep located ∼ 600 m beneath the seafloor (Schroot et al., 2005). The CH4 concentrations observed in these peat deposits are lower than but similar in magnitude to those found in a near-surface (< 0.2 m d.b.s.f.) highly active gas seep in the northern North Sea (Niemann et al., 2005). The highest CH4 concentrations were measured at the Vittorio site, the site of the second thickest peat layer. However, we did not find evidence that the thickness of the basal peat was linked to CH4 concentrations as both thick and thin peat layers harboured both high and low concentrations (Fig. 3).
4.3 A newly measured carbon store
The study area spans 43 158 km2, approximately 10 % of present-day European peatlands (Xu et al., 2018) and larger than the surface area of the Netherlands. We estimate the total carbon stored in these submerged basal peat deposits to be 741 Tg C, corresponding to an average of 0.017 Tg C km−2. The 741 Tg C stored in these submerged peats is equivalent to 70 % of the 1030 Tg C stored in Dutch peatlands today (Erkens et al., 2016) or 2.4 % of the 30 600 Tg C stored in the globe's largest peatland C storage facility, the Congo Basin complex (Dargie et al., 2017). This C has the potential to be released into the overlying water column in the occurrence of a marine seep that could be initiated naturally or an outcome of fossil fuel extraction (Schneider von Deimling et al., 2015).
4.4 Methanogenic but no methanotrophic communities
Oxic and anoxic batch incubations were used to assess both the CH4 production and consumption potential of these basal peat deposits. Methanogenesis was observed on methylated compounds only. In contrast to H2 CO2 and acetate, methylated compounds are a non-competitive methanogenic substrate that is metabolized by Methanosarcinales (Lyimo et al., 2000). Surprisingly, observations did not indicate the presence of this methanogenic family.
No aerobic or anaerobic methanotrophic prokaryotes were found in these peat deposits. Like many marine sediments, the anoxic and marine nature of the environment likely led to the exclusion of an aerobic methanotrophic population (Conrad et al., 1995). In addition, the low CH4 partial pressure probably inhibited sulfate-dependent anaerobic oxidation of CH4 (Thauer, 2011). Sulfate reduction in these sediments is likely linked to H2 and acetate oxidation (Oremland and Polcin, 1982). Environments with methanogens but not methanotrophs are uncommon but have occasionally been identified, e.g. in coal wells and masonry (Kussmaul et al., 1998; in 't Zandt et al., 2018). The absence of methanotroph activity is congruent with their absence in the results of 16S rRNA gene amplicon sequencing and confirms that methanotrophic species are most likely not present or active in this environment.
Methanotrophs have the potential to be activated in the presence of additional CH4. Such additional CH4 may occur due to emission caused by leakage from fossil fuel extraction, which has occurred in the local area previously (Schneider von Deimling et al., 2015). Upon activation, methanotrophs would have the potential to consume both the newly added and existing CH4 sources.
4.5 Microbial communities are diverse across sites and depths
We observed pronounced differences among the microbial populations at the four sampled locations (Vittorio, Max Gundelach, Senator Westphal S, and Westland sites). This heterogeneity of in situ microbial populations may be linked to the availability of residue minerals provided by plant species (Gastaldo et al., 2004; Stocker, 2012) in contrast to the homogenous results that would have been expected of an otherwise sedimentary marine ecosystem. We carried out a qPCR to investigate the relative abundance of bacteria and archaea in these samples. This is especially relevant for microorganisms in the CH4 cycle since all methanogenic microorganisms are found in the archaeal domain and provide an indication of the relative contribution of methanogenic archaea in these ecosystems.
The high CH4 concentrations observed at the Vittorio and Darci sites occurred in the presence of nitrate and ammonium (Table S2), minerals that are indicative of increased rates of biological mineralization (Burdige, 1991). However, the high ammonium concentrations observed at the Westland site were not linked to CH4 concentrations. Pore water analysis described a characteristic marine system (Table S2) indicating that marine microbes have been introduced into sediments that previously harboured freshwater microbial communities. This is reflected by the occurrence of Dehalococcoidia and candidate phylum JS1 bacteria, which are characteristic of marine sediments. These species showed the highest abundances in the two sites located nearest to each other in the study area, Vittorio and Max Gundelach SW (Nobu et al., 2016; Wasmund et al., 2014). Candidate phylum JS1 bacteria were omnipresent, whereas Dehalococcoidia were more abundant in 3 of the 12 layers, without a clear link to depth or local conditions. Although the sampling resolution was limited, this study provides the first insights into the microbial diversity of basal peat deposits and queries the role of the carbon source for the present-day microbial community composition (Figs. 5 and S4). Future studies with higher sampling resolution may provide a better understanding of the relationship between plant and microbial species.
4.6 Plant succession is analogous across sites
The parallel sequences observed at the Max Gundelach site in the Vlieland region and Fredricksborg NE site in the Dogger Bank region began and ended at different times, suggesting that a comparable geomorphological context was present at both sites but during different periods. The Max Gundelach peatland was established 10 120 cal yr BP, whereas the Fredricksborg NE peatland was established 11 885 cal yr BP. It is striking that the same three-step bryophyte-dominated sequence of Sphagnum–Tomentypnum nitens–Warnstorfia/Drepanocladus occurs in both geographically and temporally different sites. However, in contrast to the sequence of the Max Gundelach site, where Sphagnum magellanicum is present only at the start of the sequence, Sphagnum papillosum is present throughout the peat sequence at the Fredricksborg NE site. In general, plant remains are better preserved in the layers dominated by Sphagnum spp. than in those dominated by brown mosses.
These changes are aligned with the peat growth described by Wolters et al. (2010) which prevailed for ca. 1300 years before inundation occurred. The vegetation description of Wolters et al. (2010) is primarily based on pollen analysis, representative of regional-scale changes in vegetation composition. Active peat formation is dependent on the ability of peat to “keep up” with the rising groundwater table, but it is also susceptible to local topography. The differences in the duration and rate of peat accumulation are likely the result of the differences in the rate of sea level rise between these two locations, in addition to other, largely unknown palaeoenvironmental factors.
4.7 Dominance of Bathyarchaeota suggests a role in OM turnover
Bathyarchaeota dominated the archaeal communities of the peat sediments, with an average relative abundance of 70 %. This phylum is an evolutionarily diverse microbial group that is found in a wide range of organic-rich environments, including deep-sea and freshwater sediments (Evans et al., 2015). Bathyarchaeota often dominate marine subsurface archaeal communities, with relative abundances ranging from 10 % to 100 % (Fry et al., 2008; Zhou et al., 2018). Peatlands are rich in cellulose and lignin (McMorrow et al., 2004), which are eventually converted to fluvic and humic acids that are more accessible to the microbial community (Bozkurt et al., 2001). The growth of Bathyarchaeota subgroup 8 (Bathy-8) on lignin suggests a key role of these species in the degradation of peat OM (Yu et al., 2018), and based on chemical rate estimation, they have been identified as one of the most active phyla in deep-sea sediments (Fry et al., 2008). These findings support the high relative abundance observed in our study and the potential role played by Bathyarchaeota in the degradation of peatland biochemicals. However, further experimental evidence is needed to confirm the role of Bathyarchaeota.
4.8 Lokiarchaea may play an important role in microbial fermentation
Lokiarchaeal sequences were highly abundant in the three samples of Vittorio, and this location also showed the highest CH4 accumulation values (Figs. 6 and S4). Genome-based studies have indicated that their cellular machinery includes eukaryotic signature proteins, a cytoskeleton, and phagocytic potential, suggesting Lokiarchaea are “missing link” microorganisms between prokaryotes and eukaryotes (Spang et al., 2015). Lokiarchaea have not been previously detected in peat sediments, but a previous 16S rRNA gene- and metagenome-based study of sub-seafloor sediments of the Costa Rica Margin also found Lokiarchaeota among the major microbial phyla; thus, Lokiarchaeota may be indicative of a marine environment (Martino et al., 2019). Genomic analyses of “Candidatus Lokiarchaeota” have indicated an acetogenic lifestyle, hydrogen dependency, and mixotrophic potential (Sousa et al., 2016; Spang et al., 2019). Similarly, metabolic activity analyses of Namibian shelf sediments have revealed potential for homoacetogenesis (Orsi et al., 2020). Populations of Lokiarchaea may provide metabolic functions in OM degradation and methanogenic microbial guilds in marine sediments.
4.9 Candidate JS1 phylum bacteria dominate the potentially heterotrophic bacterial community
The JS1 lineage is a subgroup of the candidate phylum Atribacteria (Nobu et al., 2016). Metabolic reconstructions indicate their potential for fermentative metabolism and syntrophic acetate oxidation (Lee et al., 2018), and several studies have indicated they are abundant within marine sediments (Fry et al., 2008; Lee et al., 2018). Studies in the Skagerrak, the German Wadden Sea, and the Benguela Upwelling System showed that the upper sediment layers were mainly dominated by Delta- and Gammaproteobacteria, whereas deeper parts of the sub-seafloor were dominated by the JS1 lineage and Chloroflexi (Parkes et al., 2007; Wilms et al., 2006). This distribution is in line with our findings of high relative abundances of JS1 lineage bacteria in the peat deposits (Fig. 6). A 16S rRNA PCR-DGGE study of two Wadden Sea tidal flats (Neuharlingersieler Nacken and Gröninger Plate) found that JS1 lineage bacteria were most abundant in the Neuharlingersieler Nacken samples with the highest total organic carbon contents (1 %–2 %) (Webster et al., 2007). Considering these previous findings of JS1 lineage bacteria in organic-rich environments, it is not unexpected that JS1 are dominant bacteria in these organic rich peat deposits.
4.10 Basal peats and associated microbiological communities are highly diverse
Here we summarize our responses to the original hypotheses. Firstly, low CH4 concentrations were widespread across the study region with local high concentrations. Secondly, we did not find methanogens to be actively producing CH4 in the present day. Thirdly, parallel plant macrofossil sequences indicated comparable ecosystems developed across sites earmarked by paludification and inundation. This occurred at differing times, according to the influence of sea level rise on ground water. We did not observe similar patterns in microorganism populations. It is likely that the sample size of this study was too small to identify a relationship between the highly heterogeneous peat-forming vegetation and microbial populations. Our results suggest, but do not prove, North Sea basal peats harbour trapped pockets of millennia-old CH4. We hope that this provides an ecosystem overview and that this work can be used to design future interdisciplinary research questions to identify processes linking these different components.
Methane concentrations were generally low with localized exceptions. North Sea basal peat deposits function as a storage bank of observed CH4 that, in the event of physical disturbance, may be at risk of being released into the atmosphere. Microbial community structure analysis using 16S rRNA gene-based sequencing techniques and incubations indicated the absence of a CH4 biofilter. Large C stores in the presence of methanogens and in the absence of methanotrophs have the potential to be metabolized into CH4. Whilst the source of CH4 remains unconfirmed, we conclude that in the observed absence of active methanogenic and methanotrophic microbial populations, the in situ CH4 observed in this study are most likely trapped pockets of millennia-old CH4.
All data needed to evaluate the conclusions in the paper are present in the paper itself and/or the Supplement. Additional data related to this paper may be requested from the authors. Amplicon sequencing data were deposited in the GenBank database under the BioProject PRJNA639452 and can be accessed with SRA identifiers SRR12014238 – SRR12014261.
The supplement related to this article is available online at: https://doi.org/10.5194/bg-18-5491-2021-supplement.
TJRL, MHitZ, and HAJD designed the project. TJRL, FSB, MPH, and TdG collected the data. TJRL, MHitZ, NNLvdP, PvdV, ZvA, TdG, MPH, and FSB analysed the data with assistance from OHM and CPS. TJRL, MHitZ, CUW, and HAJD prepared the manuscript with contributions from NNLvdP, MSMJ, and HN.
The authors declare that they have no conflict of interest.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We thank Theo van Alen, Sihle Patience Ginindza, Cornelis Kasse, and Dave van Wees for technical assistance. We thank the Royal Netherlands Institute for Sea Research (NIOZ) and particularly Gert-Jan Reichhart, who was instrumental in organizing the two cruises. We thank the captain and the entire crew of the R/V Pelagia for enabling the success of the two sampling campaigns.
This research has been supported by the Nederlandse Organisatie voor Wetenschappelijk Onderzoek (grant nos. 024.002.002 and 024.002.001) and the European Research Council, H2020 European Research Council (grant nos. AG Ecomom 339880 and SyG Marix 854088).
This paper was edited by Aninda Mazumdar and reviewed by Rhiannon Mondav and one anonymous referee.
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