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Article

A PCR-Based Survey of Methane-Cycling Archaea in Methane-Soaked Subsurface Sediments of Guaymas Basin, Gulf of California

by
John E. Hinkle
1,*,
Paraskevi Mara
2,
David J. Beaudoin
2,
Virginia P. Edgcomb
2 and
Andreas P. Teske
1,*
1
Department of Earth, Marine and Environmental Sciences, University of North Carolina at Chapel Hill, Chapel Hill, NC 27599, USA
2
Department of Geology and Geophysics, Woods Hole Oceanographic Institution, Falmouth, MA 02543, USA
*
Authors to whom correspondence should be addressed.
Microorganisms 2023, 11(12), 2956; https://doi.org/10.3390/microorganisms11122956
Submission received: 3 November 2023 / Revised: 1 December 2023 / Accepted: 7 December 2023 / Published: 10 December 2023
(This article belongs to the Special Issue Microbial Communities Involved in the Methane Cycle)
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Abstract

:
The Guaymas Basin in the Gulf of California is characterized by active seafloor spreading, the rapid deposition of organic-rich sediments, steep geothermal gradients, and abundant methane of mixed thermogenic and microbial origin. Subsurface sediment samples from eight drilling sites with distinct geochemical and thermal profiles were selected for DNA extraction and PCR amplification to explore the diversity of methane-cycling archaea in the Guaymas Basin subsurface. We performed PCR amplifications with general (mcrIRD), and ANME-1 specific primers that target the alpha (α) subunit of methyl coenzyme M reductase (mcrA). Diverse ANME-1 lineages associated with anaerobic methane oxidation were detected in seven out of the eight drilling sites, preferentially around the methane-sulfate interface, and in several cases, showed preferences for specific sampling sites. Phylogenetically, most ANME-1 sequences from the Guaymas Basin subsurface were related to marine mud volcanoes, seep sites, and the shallow marine subsurface. The most frequently recovered methanogenic phylotypes were closely affiliated with the hyperthermophilic Methanocaldococcaceae, and found at the hydrothermally influenced Ringvent site. The coolest drilling site, in the northern axial trough of Guaymas Basin, yielded the greatest diversity in methanogen lineages. Our survey indicates the potential for extensive microbial methane cycling within subsurface sediments of Guaymas Basin.

1. Introduction

The Guaymas Basin is a young marginal rift basin in the Gulf of California, which is characterized by active seafloor spreading, volcanic sill intrusions into rapidly deposited organic-rich sediments, and steep geothermal gradients where sedimentary organic material of photosynthetic origin turns into hydrocarbons, which can potentially be utilized by microbes as substrates. The dominant hydrocarbon in Guaymas Basin sediments, methane, is of predominantly thermogenic origin, located in the hot subsurface, and gradually changes to microbially produced methane in the upper, cooler sediments [1,2,3].
Using seafloor samples collected by submersible, hyperthermophilic methanogens (Methanocaldococcus, Methanopyrus) have been isolated from hydrothermal hot spots in the southern axial trough of the Guaymas Basin [4,5]. PCR-based surveys have detected a wide range of methanogenic lineages in surficial Guaymas Basin sediments [6,7], including members of the obligately methylotrophic Methanofastidiosa lineage [8]. Sulfate-dependent anaerobic methane-oxidizing archaea (predominantly ANME-1 and ANME-2) are widespread in the surficial sediments in the Guaymas Basin [9,10,11,12]. Thermophilic ANME-1 lineages were enriched from hydrothermal sediments from the Guaymas Basin at temperatures ranging from 50 to 70 °C [13,14,15], and at 70 °C from the Pescadero Basin in the southern Gulf of California [16,17].
In contrast to the well-studied surficial sediments of the Guaymas Basin, investigations into the diversity and activity of methane-cycling microorganisms in the sedimentary subsurface of the Guaymas Basin are just beginning. Enrichments from subsurface sediments obtained during DSDP Expedition 64 demonstrated viable methanogens within the upper 20 m of the sediment column [18]. High-throughput 16S rRNA gene sequencing surveys of the shallow Guaymas Basin subsurface, down to a 5 m sediment depth, detected mainly ANME-1 archaea, and found only traces of diverse methanogen lineages [2]. The scarcity of methanogens was also noted by a recent metagenomic study of deep subsurface sediments in the Guaymas Basin [3].
To examine the diversity and distribution of methanogens and methane-oxidizing archaea, we performed PCR amplification and sequencing of the mcrA gene, which encodes the alpha (α) subunit of methyl coenzyme M reductase, also known as the MCR complex. The MCR complex is the central enzyme in anaerobic microbial methane metabolism, as it catalyzes the final step of methanogenesis, and the first step of the sulfate-dependent oxidation of methane performed by methane-oxidizing archaea (anaerobic methane oxidation [19]. While mcrA genes are diagnostic for methane-cycling archaea, they also complement the phylogenetic analysis of methane-cycling archaea through 16S rRNA genes [20,21]. Previous 16S rRNA and mcrA-based surveys of surficial Guaymas sediments yielded diverse methanogens and methane-oxidizers, using general and group-specific PCR primers [7]. These primers were constructed at a time when mcrA-containing archaea outside of Phylum Euryarchaeota were unknown, and thus not targeted [22,23,24,25]. Here we use partial mcrA gene sequences to construct phylogenetic trees for a detailed study of methane-cycling archaeal diversity in deep subsurface Guaymas sediments that were sampled during International Ocean Discovery Program (IODP) expedition 385 [26].

2. Materials and Methods

Sampling. Eight drilling sites were visited and sampled by R/V JOIDES Resolution during Expedition 385 of the International Ocean Discovery Program to Guaymas Basin (15 September–15 November 2019). The northern axial trough of Guaymas Basin and its off-axis flanking regions were targeted to explore the diversity, depth range, and in situ temperature range of methane-cycling archaea in the Guaymas Basin subsurface (Figure 1). Sediment cores were collected, split into smaller sections on board, and frozen at −80 °C by the shipboard science crew. DNA extraction and successful mcrA amplification occurred at different sites, and sediment depths that extended from 0.8 m below sea floor (mbsf) down to 142 mbsf (Table 1).
Thermal profiles. The Advanced Piston Corer Temperature Tool (APCT-3) [27] and Sediment Temperature Tool (SET-2) were used to measure downhole equilibrium temperatures. The SET-2 tool was used for temperature measurements in lithified sediments that were too stiff for the APCT-3 tool. The SET-2 tool was only used when necessary as it can lead to cracks in the sediment. These cracks lead to temperature measurements of diminished quality. Temperature values were interpolated for each sample using linear regression of the local thermal gradient (°C/m) multiplied by depth (mbsf), plus the y-axis intercept: U1545A, B, T = 0.225 × depth + 4.899; U1546A, T = 0.221 × depth + 2.627; U1547A/B, T = 0.511 × depth + 13.01; U1548A, T = 0.646 × depth + 8.301; U1548B, T = 0.804 × depth + 6.5; U1548C, T = 0.958 × depth + 15.916; U1548D/E, T = 0.271 × depth + 3.241; U1549A, T = 0.194 × depth + 3.228, U1550A, T = 0.135 × depth + 3.532; U1551A, T = 0.1 × depth + 4.741; U1552A/B, T = 0.262 × depth + 3.543.
DNA extraction. DNA was extracted from near-surface (0.8–2.1 mbsf), intermediate (15.4–54.8 mbsf), and deeper locations (65.7–142 mbsf), as summarized in Table 1. The MP Biomedical FastDNA™ SPIN Kit was used to extract DNA following manufacturer suggestions. Prior to DNA extraction, sediment samples were removed from −80 °C and were thawed on ice. A subsample of 0.5 gr homogenized sediment was transferred using autoclaved and ethanol-rinsed metallic spatula into sterile DNA/RNA-free tubes containing beads, provided by the manufacturer. All DNA extractions were performed in a UV-sterilized clean hood (two UV cycles of 15 min each) that was installed with HEPA filters. Surfaces inside the hood and pipettes were thoroughly cleaned with RNase AWAY (Thermo Scientific, Waltham, MA, USA) and with absolute ethanol (200 proof; purity ≥ 99.5%; Thermo Scientific Chemicals) before every extraction and in between extraction steps.
PCR assays and mcrA gene analysis. PCR reactions were performed with mcrA-targeting primer sets reported to successfully amplify mcrA gene sequences of diverse archaeal methane-cycling lineages identified in Guaymas surficial sediments (7). To PCR- amplify the gene of interest, we used the general mcrIRD primers (F: 5′-TWYGACCARATMTGGYT-3′; R: 5′-ACRTTCATBGCRTARTT-3′) that cover a range of known mcrA gene sequences in Guaymas Basin, and the ANME-1-specific mcrA gene primers (F: 5′-GACCAGTTGTGGTTCGGAAC-3′; R: 5′-ATCTCGAATGGCATTCCCTC-3′) that target the ANME-1 lineage involved in anaerobic methane oxidation in Guaymas Basin (7). The PCR reactions at every examined depth were performed in triplicate (n = 3) using a Takara SpeedSTAR HS DNA polymerase kit (Takara Bio USA, Madison, WI, USA) with the following modifications: each 25 µL PCR reaction contained 0.5–1 ng of template DNA, 2× Takara SpeedSTAR Buffer I, 2.5 mM dNTPs (Takara Bio USA, Madison, WI, USA), 2 mM of each primer (final concentrations), 1.25 units of SpeedSTAR HS DNA Polymerase, and DEPC water (Fisher BioReagents, Pittsburgh, PA, USA). The PCR reactions were performed at 95 °C for 5 min, followed by 35 cycles of 95 °C (30 s), 48 °C (30 s), and 72 °C (45 s) for the mcrIRD primers. The same PCR conditions were also applied for ANME-1-specific mcrA primers with the exception that the annealing temperature was set at 60 °C (30 s). To confirm the absence of contamination due to handling and PCR reagents, we included negative controls (blanks) in all PCR experiments. Negative controls did not include template DNA, but 5 µL of DEPC water. As a positive control we used DNA from surficial Guaymas sediments collected with Alvin push cores during the AT42-05 research cruise in Guaymas Basin, containing natural assemblages of methanogens and ANME-1 archaea [28].
Then, 2 μL of all PCR amplified samples were run onto 2% agarose gel (Low-EEO/Multi-Purpose/Molecular Biology Grade Fisher BioReagents) to verify the amplification of the mcrA genes. The PCR-amplified mcrA gene using mcrIRD or ANME-1 primers is ~500 base pairs in size. All successful PCR reactions per sample (n = 3) were pooled together and were purified and concentrated using the Agencourt AMPure XP protocol (Beckman Coulter, Brea, CA, USA) following the manufacturer’s suggestion. The purified/concentrated PCR products were sequenced at Georgia Genomics and Bioinformatics Core (University of Georgia) using the MiSeq Illumina Platform.
The paired reads generated with MiSeq were quality checked and trimmed using FastQC (v. 0.11.7). We analyzed the mcrA data using the QIIME2 platform [29], and the DADA2 plugin provided in the QIIME2 pipeline to denoise and optimize the merging of the forward and reverse reads. The functional annotation of the generated mcrA sequences was assigned manually using BLASTx against GenBank NR. The mcrA and ANME-1 mcrA sequences that were retained for further analyses were those that were functionally annotated as “methyl CoM reductase” and presented as e values ≥ 1 × 10−10. The manually curated sequences that were functionally misannotated were excluded from downstream analyses.
mcrA gene phylogeny. The mcrA gene sequences that were successfully annotated “methyl CoM reductase” were aligned using Multiple Sequence Comparison by Log-Expectation (MUSCLE) in MEGA11. The aligned sequences were used to construct minimum evolution phylogenetic trees checked by 1000 bootstrap replicates. Bootstrap values indicating greater than 50% support for an individual cluster were included in each phylogenetic tree. For easy reference, all mcrA gene sequences in our phylogenetic trees are included in the supplementary materials.
Nucleotide BLAST search (BLASTn) was used to find closely related sequences in GenBank NR. These closely related sequences were then included in the trees to add phylogenetic context and allow for cluster labeling. A phylogenetic tree was constructed using the five most abundant ANME-1 mcrA gene sequences from seven of the eight drilling sites. mcrA gene sequences from methanogenic lineages were placed into a separate phylogeny. To obtain a wider view of ANME-1 diversity, site-specific trees were constructed for sites where the number of sequences recovered was conducive to constructing a phylogenetic tree. For each site, all sequences with >100 clones were used to construct a phylogenetic tree. An exception was for the site U1550B’s specific tree which had 200 sequences with >100 clones. For this site, the top 25 sequences, by clone number, from samples U1550B_ 1H2, U1550B_3H2, and U1550B_7H2, (2.0, 16.9, and 54.8 mbsf, respectively; Table 1) along with two sequences from sample U1550B_ 19X2 (142 mbsf) were used to construct a phylogenetic tree.

3. Results

Site characteristics. PCR-amplified mcrA genes were obtained from nearly all drilling sites in the IODP Expedition 385 (Figure 1) which differ in their degree of hydrothermally driven heat flow [30], and in the relative extent of marine vs. terrestrial sedimentation [31]. Samples yielding PCR amplicons were generally affiliated with subsurface maxima or with broad zones of high alkalinity and DIC concentration [32], a proxy for microbial organic matter remineralization (Supplementary Figures S1a–h and S2). These geochemical layers often coincide with methane–sulfate transition zones (SMTZs), which are shown to have elevated microbial cell counts and increased microbial activity [33]. Concentration profiles for methane and sulfate are tabulated for geochemical context (Supplementary Table S2). Sediment samples, depths, in situ temperatures, geochemical regime (sulfate-replete zone, methane-replete zone, SMTZ), and PCR results are summarized in Table 1. Two neighboring sites (U1545 and U1546) on the northwestern end of Guaymas Basin [34,35] essentially differ by the presence of a massive, thermally equilibrated sill between 350 to 430 m below seafloor (mbsf) at site U1546 [36]. Two drilling sites (U1547, U1548) at the hydrothermally active Ringvent area, approximately 28 km northwest of the spreading center [2], target a shallow, recently emplaced, hot sill that creates steep thermal gradients and drives hydrothermal circulation [37]. Site U1549 [38] samples the periphery of an off-axis methane cold seep, Octopus Mound, located ~9.5 km northwest of the northern axial graben. Site U1550 is located close to DSDP Site 481 and samples the heterogeneous (marine and terrestrial) sediments that are accumulating in the northern axial valley [39]. Site U1551 represents the terrestrially influenced sediments of the southeastern Guaymas Basin with riverine sand input from the Yaqui River [40]. Site U1552 [41] sampled the subsurface of a cold seep site surrounded by shallow methane hydrates, close to the Sonora Margin.
Regarding their in situ temperature gradients, the Guaymas Basin drilling sites fall into two categories: the hot Ringvent sites with steep temperature gradients of ca. 50 to 100 °C/100 m depth, and the majority of Guaymas sites with elevated temperature gradients of approx. 20 to 25 °C/100 m (Figure 2). Even the gradient at the coolest site, U1550 with a depth of ca. 13–14 °C/100 m, is at least twice as steep as the temperature gradients commonly found for ocean crust. These distinct thermal gradients are, to some extent, reflected in the different lineages of the detected methanogens.
Detection of Methanogen lineages. Three of the seven examined sites (U1547B, U1548B, and U1550B) yielded mcrA genes related to previously established methanogens or methane-cycling archaea, using PCR primers that encompass the widest possible diversity of mcrA genes but do not capture ANME-1 [7]. Most of our positive PCR amplicon results were obtained from the upper layer of the sediment column, whereas deeper sediments yielded negative results, even after many PCR attempts (Table 1).
Two sites (U1547B and U1548B) are located at the Ringvent mound, an off-axis hydrothermal system driven by recent sill emplacement (Figure 3). Here, the temperature gradients increase rapidly along a sampling transect with tightly spaced, increasing temperature measurements towards the ring-shaped mound (Figure 2) where conspicuous hydrothermal activity and a topographical high of ca. 20 m mark the rim of the buried sill [2]. At Ringvent sites U1547B and U1548B, the most abundant phylotypes were close relatives of the extreme hyperthermophile and obligate hydrogenotroph Methanocaldococcus bathoardescens (Figure 4), originally isolated from low-temperature hydrothermal fluid (26 °C) at the Axial Seamount on the Juan de Fuca Ridge [42]. Although isolated from relatively temperate fluids, Methanocaldococcus bathoardescens is a hyperthermophile that grows under temperatures from 48 to 90 °C, with a thermal optimum of 82 °C [42]. Samples from the Ringvent mound sites also yielded mcrA genes of the Methanosarcinaceae (capable of using acetate, CO2, and methyl substrates for methanogenesis) and the mostly hydrogenotrophic Methanomicrobiaceae (Figure 4).
At the cool axial site, U1550B, greater methanogenic diversity was observed, including the obligately acetoclastic Methanosaetaceae, the metabolically diversified Methanosarcinaceae, and the most hydrogenotrophic or (occasionally) ethanol-utilizing Methanomicrobiaceae and Methanobacteraceae (Figure 4). Additionally, the uncultured mcrA “group E” lineage related to anaerobic methane-oxidizing ANME archaea [21], and an uncultured Guaymas group without any cultured relatives were detected at this site [7].
ANME-1 diversity. While methanogen populations were only observed at three sites (U1547B, U1548B, and U1550B), seven sites yielded mcrA gene sequences affiliated with the ANME-1 lineage (Methanophagales), using primers that were fine-tuned for this order-level lineage (7). Extensive searches in GenBank NR and comparisons to database sequences showed that ANME-1 phylotypes from Guaymas Basin subsurface samples were closely related to reference sequences from the Napoli mud volcano [43], from subsurface sediments of the Mississippi Canyon 118 seep site in the Gulf of Mexico [44], and from shallow subsurface sediments recovered by piston coring and push coring in Guaymas Basin [2,45]. Almost all ANME-1 mcrA gene sequences could be accommodated in sixteen distinct phylogenetic clusters (Figure 5). These clusters were further examined and confirmed through site-specific mcrA gene phylogenies for five sites, U1547B, U1548B, U1550B, U1551B, and U1552B (Supplementary Figures S3–S7).
In searching for thermophilic ANME-1 lineages, we found that cluster 8, consisting of mcrA genes from ANME-1 enrichments in surficial sediments at 50 °C [13], also included Guaymas subsurface mcrA genes from site U1551B. However, we observed no overlap of the Guaymas subsurface mcrA genes with mcrA genes from thermophilic methane-oxidizing ANME-1 enrichment cultures that are active at 70 °C [15,17].
The habitat and site preferences of different mcrA gene lineages were visualized with a bubble plot of mcrA gene recovery, color-coded by habitat type (Figure 6, and Supplementary Figure S8). From the relatively cool northwestern site, U1545B, only a single sample yielded mcrA gene sequences, all of them members of cluster 3 (color-coded in grey). Gene sequences from the hydrothermal Ringvent sites (in red, Figure 6) were highly diverse, and affiliated with clusters 1, 2, 5, 6, 10, 11, 12, 14, 15, and 16. Gene sequences from the axial site U1550B were also diverse (color-coded in green, Figure 6). Gene sequences from the terrestrially influenced site U1551B were largely affiliated with group 13 (Figure 5), plus smaller proportions of U1551B-derived sequences that fell into clusters 1, 3, 8, and 10 (Figure 6). Cluster 13, which dominated the samples from site U1551, did not include any sequences from other sites, and thus provides the best example within this dataset for a strong habitat preference within a particular lineage (color-coded in brown, Figure 6). No published mcrA genes that would fall into this cluster were found in GenBank NR. Finally, gene sequences from the cold seep site U1552B were affiliated with clusters 3, 7, and 9 (color-coded in blue, Figure 6).

4. Discussion

ANME-1 diversity. The methane-oxidizing group ANME-1, is widespread in the Guaymas Basin, as it was observed at every site examined, particularly above or near depths where methane–sulfate interfaces occur (Supplementary Table S2). Methane–sulfate interfaces are present at varying depths in the subsurface, depending on geologic formations and methane flux. To some extent, the different regions in the Guaymas Basin are characterized by different ANME-1 types. While it is possible that some clades may not be detected due to sensitivity issues or sequencing artifacts, our data identify clades that show an observable preference for particular sites, which differ in temperature and geochemistry. This differentiation can be observed by comparing the clusters in the phylogenies constructed specifically for each drilling site. For example, when comparing the ANME-1 phylogenies from sites U1548B and U1552B, the methane hydrate site U1552B contains three distinct ANME-1 clusters, two of which are not shared with the phylogeny of hydrothermally influenced Ringvent site U1548B (Figures S4 and S8 in the supplemental material). These differences in ANME-1 cluster representation across sites suggest how the locally distinct thermal profiles (Figure 2) and in situ temperature conditions contribute to shaping the microbial biogeography of the Guaymas Basin.
Connection with deeply sourced geofluids. Close phylogenetic relationships between sequences from cold seeps, mud volcano, and deep subsurface sediments were observed in the general ANME-1 phylogeny (Figure 5). Previous research indicates that these similarities reflect the role of cold seeps and mud volcanoes as a “window to the deep subsurface”, dispersing microbes from the deep subsurface into the hydrosphere, as deep geofluid seepage and mud volcano eruptions bring gas-rich fluidized sediment and its microbial populations from the deep subsurface to the seafloor [46]. Cold seeps and mud volcanoes could garner more attention as an alternative way to study the deep marine biosphere since R/V JOIDES Resolution will be decommissioned in October 2024 and plans for a replacement vessel have been paused for a prolonged period [47].
Hyperthermophilic methanogens at Ringvent sites. Hyperthermophilic methanogens (family Methanocaldococcaceae) at the hot Ringvent sites U1547B (51 °C at 74.2 mbsf) and U1548B (68 °C at 76.5 mbsf) were not recovered from deep, hot sediments, but were recovered from shallow, cool, and relatively oxidizing (sulfate-reducing) sediment samples between 2.1 and 9.1 mbsf (up to 17.4 °C). This apparent paradox can be explained by the low cell abundances (≤105 cells per cm3 of sediment) detected at those two sites when sediments reached temperatures ≥ 45 °C [48], and by the environmental regime that exists in the Ringvent area. The Ringvent mound is underlaid by a hot volcanic sill, which drives hydrothermal circulation at the relatively thinly sedimented surface of the mound and brings hot hydrothermal fluids (up to 75 °C) to the sediment surface [2]. Hyperthermophiles could rise with methane-rich hydrothermal fluids from deeper sediments or may originate from localized hydrothermal hot spots that have been observed at the sediment/water interface at the Ringvent [2]. Either way, hydrothermal circulation could deposit microbial cells in the wider Ringvent area and seed cool, surficial sediments with hyperthermophiles. Previous studies have detected thermophilic methanogen lineages in cool, surficial Guaymas Basin sediments, and have proposed transport to the surface via hydrothermal flow [6].
Methanogen scarcity. Many ANME-1 sequences were collected from our sampling sites; however, methanogen sequences were relatively scarce. This poses a question: Why is ANME-1 so abundantly detected, yet methanogens so rare, in the Guaymas Basin deep subsurface?
While methodological limitations, such as PCR primer range and sensitivity, could play a role, methanogen scarcity is not only observed in this mcrA gene survey, but also in 16S rRNA analyses [2,12], in metagenomic investigations [3], and in cultivation studies [49]. It seems unlikely that these conceptually and technically distinct methods are consistently biased against methanogens, and to such a degree that they would miss a large swath of methanogenic diversity. While undetected, “exotic” methanogenic lineages cannot be excluded with certainty, they would have to hide in plain sight (for example, in poorly described uncultured phylogenetic lineages) to comprise a significant portion of methanogenic diversity.
The likely scarcity of methanogens in the Guaymas Basin deep subsurface has implications for the origin and microbial processing of subsurface methane. Methane clumped isotope measurements show that the proportion of biogenic methane increases towards the sediment surface, whereas methane in deep, hot sediments is predominantly thermogenic [3]. If the population density of active methanogens in the Guaymas subsurface sediments is relatively low, the massive reservoir of biogenic subsurface methane must have accumulated over geological time [3]. Methanogenic gene expression is predominately observed in surficial sediments where most methane cycling occurs [50]. Some of this methane produced in surficial sediments could be incorporated into the subsurface reservoir of biogenic methane.
Thermal preferences of methanogens. Notably, the cooler axial site (U1550B) exhibits greater methanogenic diversity than the much warmer Ringvent mound sites (U1547B and U1548B). This difference in diversity may reflect the methanogens’ general preference for moderate temperatures [12]. While thermophilic methanogenic lineages have been isolated from deep-sea vent systems [4,42], most cultured methanogenic lineages are not thermophilic [51]. Observing greater methanogenic diversity in cooler sediments of the Guaymas subsurface underscores the linkage between sediment depth/temperature and methane origin, by supporting the observation that biogenic methane predominates in shallower, cooler sediments, whereas thermogenic/abiotic methane predominates in deeper, warmer sediments [3].
Future directions. A future direction of this research lies in investigating the matching 16S rRNA datasets and pulling mcrA genes from entire genomes. mcrA genes pulled from previously published genomes will allow for the strengthening of our current mcrA phylogenies. The construction of 16S rRNA phylogenies to complement the existing mcrA phylogenies will allow for a comprehensive PCR-based survey of methane-cycling microbial communities in the Guaymas Basin subsurface. Additionally, there is the possibility of linking our mcrA-based phylogenies to genome-based phylogenies of ANME-1 [17].
The diversity of Guaymas Basin subsurface sediments suggests that they would contain mcrA-containing archaea outside of Phylum Euryarchaeota. Candidates could even be hiding in published metagenomes, for example, metagenomes related to Phylum Verstraetearchaeota [52]. Further development of mcrA primers to capture these groups would aid in their detection [23,53].
Another research direction focuses on the role of volcanic sills in methane cycling in the Guaymas Basin. Current research suggests that the abundance of methane located at and in these sills is of predominately thermogenic origin, resulting from the thermal maturation of organic matter [1,3,37]. However, these sills are known to harbor sediment intrusions, which could contain microbes, and even methanogens. The sediment–sill interfaces remain within the temperature range for methanogenic hyperthermophiles [5]. While it is unknown if there is enough accessible energy to support cellular metabolism, sill intrusion contributes to the thermal maturation of organic matter and provides a potential influx of low-molecular-weight maturation products that would be available for microbial metabolism [54,55]. Future metagenomic analyses of recovered veined rock samples will seek to address this issue.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/microorganisms11122956/s1, Figure S1: Samples and geochemical context; Figure S2: Synopsis of PCR results; Figure S3: Phylogeny for Site U1547B; Figure S4: Phylogeny for Site 1548B; Figure S5: Phylogeny for Site 1550B; Figure S6: Phylogeny for Site 1551B; Figure S7: Phylogeny for Site 1552B; Figure S8: Annotated mcrA gene amplicon abundance plot; Table S1: PCR results for all samples; Table S2: Methane and sulfate concentrations for Guaymas Basin subsurface sediment samples; File S1: Supplementary Data File 1—Methanogen sequences; File S2: Supplementary Data File 2—ANME1 sequences.

Author Contributions

J.E.H. wrote the first draft of the manuscript, conducted the mcrA phylogenetic analyses, and created phylogeny figures. P.M. conducted the mcrA PCR amplifications, and the manual curation and functional annotation of the mcrA sequence data. D.J.B. conducted the DNA extractions and the mcrA sequence data analyses. V.P.E. collected sediment samples, supervised P.M. and D.J.B. on the mcrA data generation and analyses. A.P.T. conceptualized the study design, provided figures, and contributed to subsequent drafts of the manuscript. All authors have read and agreed to the published version of the manuscript.

Funding

Sampling in Guaymas Basin and post-cruise research in the Teske lab was supported by the International Ocean Discovery Program (IODP). This research used samples and data provided by the International Ocean Discovery Program. We thank David Geller-McGrath for an early version of Figure 6. This study was supported by NSF Grant OCE-2046799 to V.P.E., P.M., A.P.T. and R. Hatzenpichler, and by NSF grant OCE-1829903 to V.P.E., P.M. and A.P.T. Current research in the Teske lab is supported by NASA Exobiology grant 21-5477 and by NSF Biological Oceanography grant 2048489.

Data Availability Statement

All mcrA generated sequences were deposited into the National Center for Biotechnology Information (NCBI) Sequence Read Archive database under project BioProject ID PRJNA909197. The accession numbers for the mcrA sequences from samples U1550B_7H2, U1548B_2H3, and U1547B_2H2 are SRR23604134, SRR23604145, and SRR23604146 respectively. The accession number for the ANME-1 mcrA sequences from sample U1545B_4H3 is SRR23604132. The accession number for the ANME-1 mcrA sequences from samples 1547B_8H2 and 1547B_9H2 are SRR23604131 and SRR23604130, respectively. The accession numbers for ANME-1 mcrA sequences from samples 1548B_1H2, 1548B_2H3, 1548B_3H4 and 1548B_9H3 are SRR23604128, SRR23604129, SRR23604127 and SRR23604126, respectively. The accession number for the ANME-1 mcrA sequences from sample 1549B_6H3 is SRR23604144. The accession numbers for ANME-1 mcrA sequences from samples 1550B_1H2, 1550B_3H2, 1550B_7H2 and 1550B_19X3 are SRR23604143, SRR23604142, SRR23604141 and SRR23604140, respectively. The accession numbers for ANME-1 mcrA sequences from samples 1551B_1H1, 1551B_2H2, 1551B_3H2 and 1551B_5H2 are SRR23604139, SRR23604138, SRR23604137 and SRR23604136, respectively. The accession numbers for ANME-1 mcrA sequences from samples 1552B_1H2 and 1552B_3H3 are SRR23604135 and SRR23604133, respectively.

Conflicts of Interest

The authors declare no conflict of interest.

References

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Figure 1. Guaymas Basin drilling site map. The sites follow broadly a northwest-to-southeast transect across the northern Guaymas axial valley. Grey, northwestern off-axis sites U1545 and U1546; red, hydrothermally active Ringvent sites U1547 and U1548; blue, cold seep sites U1549 and U1552; green, northern Trough axial site U1550; brown, southeastern terrestrially influenced site U1551.
Figure 1. Guaymas Basin drilling site map. The sites follow broadly a northwest-to-southeast transect across the northern Guaymas axial valley. Grey, northwestern off-axis sites U1545 and U1546; red, hydrothermally active Ringvent sites U1547 and U1548; blue, cold seep sites U1549 and U1552; green, northern Trough axial site U1550; brown, southeastern terrestrially influenced site U1551.
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Figure 2. Temperature profiles of Guaymas drilling sites, plotted from measurements tabulated in the site chapters of Expedition 385 [35,36,37,38,39,40,41].
Figure 2. Temperature profiles of Guaymas drilling sites, plotted from measurements tabulated in the site chapters of Expedition 385 [35,36,37,38,39,40,41].
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Figure 3. Ringvent mound site with IODP Expedition 385 drilling sites and hole positions (U1547A–E and U1548A–E), and multichannel seismic lines for subsurface mapping [37] The topographical high marks the edge of the shallow subsurface sill where hydrothermally circulating fluids reach the sediment surface. Sequence data from cores U1547B and U1548B represent the microbial communities within the interior sedimented bowl and the hydrothermally impacted communities just outside the sill.
Figure 3. Ringvent mound site with IODP Expedition 385 drilling sites and hole positions (U1547A–E and U1548A–E), and multichannel seismic lines for subsurface mapping [37] The topographical high marks the edge of the shallow subsurface sill where hydrothermally circulating fluids reach the sediment surface. Sequence data from cores U1547B and U1548B represent the microbial communities within the interior sedimented bowl and the hydrothermally impacted communities just outside the sill.
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Figure 4. Phylogenetic diversity of methanogen lineages detected with general methanogen primers, resulting in 23 ASVs of partial mcrA gene sequences. The phylogeny was constructed using the minimum evolution method of phylogenetic inference and included bootstrap values >50%. ASVs from Ringvent sites U1547B and U1548B are plotted in red, and ASVs from axial site U1550B are plotted in green. Each taxon label starts with the ASV number, followed by the IODP sample code (drilling site, subcore number, and segment), and the number of sequences within each ASV. Methanocaldococcaceae ASVs No. 2 and 7 were recovered from both samples each, U1547B_2H2 and U1548B_2H2. Sequences used to construct this phylogeny are available in Supplementary Data File S1.
Figure 4. Phylogenetic diversity of methanogen lineages detected with general methanogen primers, resulting in 23 ASVs of partial mcrA gene sequences. The phylogeny was constructed using the minimum evolution method of phylogenetic inference and included bootstrap values >50%. ASVs from Ringvent sites U1547B and U1548B are plotted in red, and ASVs from axial site U1550B are plotted in green. Each taxon label starts with the ASV number, followed by the IODP sample code (drilling site, subcore number, and segment), and the number of sequences within each ASV. Methanocaldococcaceae ASVs No. 2 and 7 were recovered from both samples each, U1547B_2H2 and U1548B_2H2. Sequences used to construct this phylogeny are available in Supplementary Data File S1.
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Figure 5. General ANME-1 minimum evolution phylogeny based on partial mcrA gene sequences, encompassing the five most frequently recovered ASVs from each drilling site and sample. Reference site U1545B sequences are plotted in grey, those from Ringvent sites U1547B and U1548B are plotted in red, axial site U1550B sequences appear in green, terrestrial site U1551B sequences in brown, and seep site U1549B and U1552B sequences are plotted in blue. Each taxon label starts with the IODP sample code (drilling site, subcore number, and segment), followed by the ASV number and the number of sequences within each ASV. Site-specific phylogenies that include a greater number of ASVs (more than five) for each site are available in Supplemental Figures S3–S7. The sequences used to construct this phylogeny are available in Supplementary Data File S2.
Figure 5. General ANME-1 minimum evolution phylogeny based on partial mcrA gene sequences, encompassing the five most frequently recovered ASVs from each drilling site and sample. Reference site U1545B sequences are plotted in grey, those from Ringvent sites U1547B and U1548B are plotted in red, axial site U1550B sequences appear in green, terrestrial site U1551B sequences in brown, and seep site U1549B and U1552B sequences are plotted in blue. Each taxon label starts with the IODP sample code (drilling site, subcore number, and segment), followed by the ASV number and the number of sequences within each ASV. Site-specific phylogenies that include a greater number of ASVs (more than five) for each site are available in Supplemental Figures S3–S7. The sequences used to construct this phylogeny are available in Supplementary Data File S2.
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Figure 6. Abundance dot plot of mcrA gene amplicons (represented by >1000 sequences) color-coded by site, as in Figure 1, Figure 4 and Figure 5. Dot size indicates the number of sequences. The x-axis indicates the samples, and the y-axis indicates the mcrA sequences and their clustering. A version with full sample annotation on the left margin is available as Supplementary Figure S8. ASVs that are only peripherally associated with specific mcrA gene lineages, lacking bootstrap support, are labeled with “p”.
Figure 6. Abundance dot plot of mcrA gene amplicons (represented by >1000 sequences) color-coded by site, as in Figure 1, Figure 4 and Figure 5. Dot size indicates the number of sequences. The x-axis indicates the samples, and the y-axis indicates the mcrA sequences and their clustering. A version with full sample annotation on the left margin is available as Supplementary Figure S8. ASVs that are only peripherally associated with specific mcrA gene lineages, lacking bootstrap support, are labeled with “p”.
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Table 1. PCR results for Guaymas Basin subsurface sediment samples. Sample depths are noted as meters below seafloor (mbsf). The (+) and (−) symbols indicate successful PCR (+), and no PCR (−) amplifications. Geochemical zones are abbreviated as SR, sulfate-replete zone; SMTZ, sulfate-methane transition zone, MR, methane-replete zone. A version of this table that includes all samples where PCR amplification was attempted can be found in the Supplementary Materials (Supplementary Table S1).
Table 1. PCR results for Guaymas Basin subsurface sediment samples. Sample depths are noted as meters below seafloor (mbsf). The (+) and (−) symbols indicate successful PCR (+), and no PCR (−) amplifications. Geochemical zones are abbreviated as SR, sulfate-replete zone; SMTZ, sulfate-methane transition zone, MR, methane-replete zone. A version of this table that includes all samples where PCR amplification was attempted can be found in the Supplementary Materials (Supplementary Table S1).
Site (Position)Sample IDDepth (mbsf)T (°C)Geochemical ZonemcrA ANME-1 Specific PrimersmcrA General Primers (mcrIRD)
U1545B
(27°38.2301′ N,
111°53.3295′ W)		1545B_1H21.75.3SR−−
1545B_4H325.810.7SMTZ+−
U1547B
(27°30.4128′ N, 111°40.7341′ W)		1547B_2H28.617.4SR−+
1547B_8H265.746.6SR+−
1547B_9H274.251.0SR+−
U1548B
(27°30.2540′ N, 111°40.8601′ W)		1548B_1H22.18.2SR+−
1548B_2H39.113.7SR+−
1548B_3H420.422.9SR++
1548B_9H376.568.0SR+−
U1549B
(27°28.3383′ N, 111°28.7927′ W)		1549B_6H345.612.1SMTZ+−
U1550B
(27°15.1704′ N, 111°30.4451′ W)		1550B_1H22.03.8SR+−
1550B_3H216.95.8MR+−
1550B_7H254.810.9MR++
1550B_19X2142.022.7MR+−
U1551B
(27°12.3832′ N, 111°13.1841′ W)		1551B_1H10.84.8SR+−
1551B_2H25.85.3SR+−
1551B_3H215.46.3SR+−
1551B_5H234.28.2MR+−
U1552B
(27°33.2885′ N, 111°32.9640′ W)		1552B_1H20.83.8SR+−
1552B_3H319.28.6MR+−
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MDPI and ACS Style

Hinkle, J.E.; Mara, P.; Beaudoin, D.J.; Edgcomb, V.P.; Teske, A.P. A PCR-Based Survey of Methane-Cycling Archaea in Methane-Soaked Subsurface Sediments of Guaymas Basin, Gulf of California. Microorganisms 2023, 11, 2956. https://doi.org/10.3390/microorganisms11122956

AMA Style

Hinkle JE, Mara P, Beaudoin DJ, Edgcomb VP, Teske AP. A PCR-Based Survey of Methane-Cycling Archaea in Methane-Soaked Subsurface Sediments of Guaymas Basin, Gulf of California. Microorganisms. 2023; 11(12):2956. https://doi.org/10.3390/microorganisms11122956

Chicago/Turabian Style

Hinkle, John E., Paraskevi Mara, David J. Beaudoin, Virginia P. Edgcomb, and Andreas P. Teske. 2023. "A PCR-Based Survey of Methane-Cycling Archaea in Methane-Soaked Subsurface Sediments of Guaymas Basin, Gulf of California" Microorganisms 11, no. 12: 2956. https://doi.org/10.3390/microorganisms11122956

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