Neotropical peatland methane emissions along a vegetation and biogeochemical gradient.

Tropical wetlands are thought to be the most important source of interannual variability in atmospheric methane (CH4) concentrations, yet sparse data prevents them from being incorporated into Earth system models. This problem is particularly pronounced in the neotropics where bottom-up models based on water table depth are incongruent with top-down inversion models suggesting unaccounted sinks or sources of CH4. The newly documented vast areas of peatlands in the Amazon basin may account for an important unrecognized CH4 source, but the hydrologic and biogeochemical controls of CH4 dynamics from these systems remain poorly understood. We studied three zones of a peatland in Madre de Dios, Peru, to test whether CH4 emissions and pore water concentrations varied with vegetation community, soil chemistry and proximity to groundwater sources. We found that the open-canopy herbaceous zone emitted roughly one-third as much CH4 as the Mauritia flexuosa palm-dominated areas (4.7 ± 0.9 and 14.0 ± 2.4 mg CH4 m-2 h-1, respectively). Emissions decreased with distance from groundwater discharge across the three sampling sites, and tracked changes in soil carbon chemistry, especially increased soil phenolics. Based on all available data, we calculate that neotropical peatlands contribute emissions of 43 ± 11.9 Tg CH4 y-1, however this estimate is subject to geographic bias and will need revision once additional studies are published.

Introduction

Inverse modelling reveals that tropical wetlands account for much of the variability in global atmospheric concentrations of the important greenhouse gas, methane (CH4) [1]. Yet tropical wetlands remain absent from Earth system models because of a scarcity of ground-based data to parameterize bottom-up models, making these ecosystems a ‘missing link’ in the global carbon cycle [2]. In the Amazon basin, for example, modelled bottom-up source strength based on water table depth cannot explain top-down detected emissions patterns [3]. Some researchers speculate that cryptic wetlands [4] or vegetation sources [5] may account for this discrepancy, but the recent finding that perennially flooded peatlands in South America cover three to four times more area than previously realized [6] may point to a missing and/or misunderstood Amazon CH4 source.

Although CH4 emissions from high latitude peatlands have been well-studied [7], relatively little data have been published from the tropics and almost none exists for South America [8], yet this continent is now thought to contain the largest area of tropical peatland cover [6]. The scarcity of grounpan>d-based CH4 data from neotropical peatlands is the major reason why these important ecosystems are not included in many regional or global scale greenhouse gas models [2].

Studies of wetland CH4 dynpan>amics from other regions have revealed generalizable patterns that provide a framework for how Amazonian peatlands might funpan>ction. First, emissions differences within and between wetlands tend to be governed primarily by hydrology, which determines soil redox conditions [9]. Second, plant biomass and carbon quality directly related to the amount of available substrate for methanogenic microorganisms, and thus CH4 emissions often varies across vegetation zones [10]. Third, it has been shown that peat containing higher concentrations of plant-derived phenolics will block peat decomposition and greenhouse gas emissions [11,12]. And finally, ombrotropic peatlands tend to emit less CH4 than minerotrophic wetlands because of inhibitory effects of low pH [13]. It is worth retesting these assumptions in the context of Amazonian peatlands because of their potential importance to global CH4 budgets and because they are so poorly studied.

In this paper we measured CH4 emissions and soil chemistry from the most pervasive peatland communpan>ity type in Amazonia, the Mauritia flexuosa palm swamp. We sampled across three zones of one such swamp in the southern Peruvian to test the following hypotheses: 1) magnitudes of CH4 emission are greater in high productivity palm-dominated neotropical peatlands compared to lower productivity systems covered by herbaceous vegetation that provides less carbon substrate; and 2) tropical peatlands with low pH or high phenolics content will emit less CH4 than circum-neutral pH or low phenolic sites because of associated constraints on decomposition. We also summarize the few published data from neotropical peatlands to estimate the aggregate CH4 source strength of these ecosystems and assess sources of variability between them.

Methods

Study site

We collected field data for this study from a 250 ha peatland near the Los Amigos Biological Station, or Centro de Interpretacion y Capacitacion de Rio los Amigos (subsequently referred to as ‘CICRA peatland’) in mid-December 2016. Householder et al (2012) describe in detail the hydrogeomorphic setting of this and other peatlands in the Madre de Dios region. We briefly summarize the critical details here. The CICRA peatland abuts a steep terrace escarpment and is fed by numerous small perennial seeps. The regional climate has wet and dry seasons, but since the peatland is fed by groundwater, it is believed to remain inundated year round. The canopy is dominated by the palm Mauritia flexuosa which thrives in areas with permanently saturated soils throughout lowland neotropical forests from Panama to southern Brazil [14]. Formal floristic surveys of the CICRA peatland have yet to be published. A map of CICRA peatland bathymetry reveals the presence of three distinct components: two basins with peat depth exceeding 900 cm and ‘Intrabasin Flats’ with much shallower peat depth of 100 to 200 cm. In the Intrabasin Flats canopy coverage of M. flexuosa abruptly decreases from more than 85% to less than 10% giving way to open Cyperaceae mires. The extent to which emergent vegetation contributes to peat formation in these ecosystems is not clear, but the association between high palm density and deep peats is consistent with the conventional wisdom that the dense underground root system of M. flexuosa is a major contributor to soil carbon accumulation [14].

We divided our sampling effort between three zones of the CICRA peatland (Fig 1) in order to test hypotheses about the effects of vegetation type and minerotropic status. One sampling site was located in the secondary basin close to the terrace escarpment and grounpan>dwater seep sources (referred to as ‘Basin Periphery’). A second site was located in the secondary basin roughly 500 m from the terrace to represent a more ombrotrophic but otherwise similar system in terms of vegetation and peat depth (‘Basin Interior’). The third site was located in an open herbaceous zone of the Intrabasin Flats.

Fig 1

Map of the Los Amigos peatland in Madre de Dios, Peru, with sampling locations marked by stars.

Basin Periphery: -12.55664 S, -70.1117 W; Basin Interior: -12.55926 S, -70.11702 W; Intrabasin Flats: -12.55947 S, -70.12037 W. Background image from ArcMap 10.3.

Sample collection

Soils

To test for the presence of a minerotrophic-ombrotropic gradient from peatland periphery to interior, we measured a suite of soil chemical properties: total carbon, total nitrogen, total phosphorus, soluble phenolic compounds, extractable nitrate/nitrite, extractable ammonia/ammonium, and pH. From each site we extracted three replicate cores using a stainless steel peat box corer. We split each core into 5 cm sections in the field and stored them in sealed plastic bags for transport to the Duke University Wetland Center laboratory for analysis. We attempted to limit exposure of soil cores to oxygen, but any ammonium oxidation that may have occurred during sample transport would bias extractable nitrate/nitrite and extractable ammonia/ammonium values.

We measured total n class="Chemical">carbon and n class="Chemical">nitrogen content using an elemental analyzer (CE Instruments, Wigan, UK) and total phosphorus using a nitric-perchloric digestion and the molydenate blue spectrophotometric method [15]. We performed a 12-h deionized water extraction of soil subsamples and analyzed extracts for soluble phenolics following Lowe (1993) [16], and for nitrate/nitrite and ammonia/ammonium using a Lachat Quickchem 8000 autoanalyzer. We measured soil pH using both a 5:1 ratio of wet soils to DI water followed by the addition of 0.125 mL of CaCl2 following the methods outlined in Carter and Gregorich (2007) [17].

Methane

We used a static chamber method to measure n class="Chemical">CH4 flux [18,19]. We used 30 cm diameter plastic collars with n class="Chemical">water-fillable gutters and sampled using a rod for chamber top setup and sampling to avoid disturbing soil adjacent to chambers [20]. Rather than embed collars into the soil, as is often the practice, we simply rested them unanchored onto the soil surface in order to avoid unnecessary disturbance. This was possible because all sites were flooded with up to 10 cm of standing water. We placed six collars pseudo-randomly at each site [except four at the Secondary Basin periphery] avoiding areas where overlying vegetation or palm debris would interfere with chamber setup.

We extracted four 50 ml headspace samples from opaque chambers at 5–10 minute intervals for incubations lasting a total of 20 to 30 min and total extracted gas was roughly 1% of the 20 L headspace volume. We recorded internal chamber temperature at the time of each sample extraction and the height of each chamber in order to calculate gas concentration using the Ideal Gas Law. We stored samples in gas-tight mylar bags and transported them to the Duke University Wetland Center laboratory in North Carolina, USA for analysis within one week on a Varian 450 gas chromatograph. We calculated flux using linear regression of headspace concentration over time, which yielded r-squared values of at least 0.95 in all cases.

We measured the concentration of CH4 in soil pore water using a headspace equilibrium method [21]. We collected 4 replicates samples of 40 ml pore water from 10–15 cm soil depth at each site (except 2 replicates from Secondary Basin periphery) using a custom-made slotted metal sipper and injected them directly, without exposure to ambient air, into mylar bags pre-loaded with 100 ml of dinitrogen (N2). Dissolved gases were allowed to equilibrate with headspace N2 during the 48 to 72 hours of transport time to the Wetland Center laboratory, at which point 60 ml of headspace gas was extracted and deposited into an empty mylar bag for dry storage until samples could be analyzed on a Varian 450 gas chromatograph within one week. We used Henry’s Law to calculate the concentration of CH4 in pore water based on the concentration of CH4 measured in headspace.

Statistical analyses

We tested for differences in mean CH4 flux between the Secondary Basin Periphery, Secondary Basin Interior and Intrabasin Flats using Analysis of Variance (ANOVA). Finding that mean CH4 flux was not equal across the three areas, we followed up with the pairwise post-hoc Tukey’s test of honest significant differences. We performed a Welch’s t-test to test for differences in mean CH4 flux between the Secondary Basins (Periphery and Interior data combined) and the Intrabasin Flats. Since we lacked sufficient replication to compare mean pore water dissolved CH4, we lump the two basins sites and compare means of Secondary Basin versus Intrabasin Flats via a Welch’s t-test. We compared peat soil variables among sites using a Tukey’s honest significant difference test. All statistics were calculated using the R programming language [22].

Literature synthesis and extrapolation

We searched Google Scholar and ISI Web of Science for publications matching the terms “methane mauritia -mauritius” or “methane amazon” to find ground-based measurements of CH4 emissions from South American peatlands and/or palm swamps. We excluded several studies pertaining to floodplain mineral soil systems [23-28]. We included a study of a Raphia taedigera palm peat swamp in Panama [29], despite its location outside of continental South America and the Amazon basin, because of the climatic similarity and geographic proximity.

To estimate the total annual contribution of neotropical peatlands to annual n class="Chemical">CH4 emissions we multiply the mean and standard error of published emissions rates from our literature synpan>thesis by the recent estimate of 750,000 km2 of peatlands in tropical/subtropical Central and South America [6].

Results

We found that emissions were highly variable at the local scale within the CICRA peatland (ANOVA p = 0.019). Mean CH4 emissions at the Intrabasin Flats of 4.7 ± 0.9 mg CH4 m2 h-1 were significantly lower than those of 17.2 ± 3.7 mg CH4 m2 h-1 at the Secondary Basin Periphery according to Tukey’s honest significant differences test (p < 0.02) (Fig 2). Mean emissions at the Secondary Basin Interior of 11.9 ± 3.0 CH4 m2 h-1 were intermediate and not significantly different from emissions at the other sites (p = 0.13 and p = 0.39 for Intrabasin Flats and Secondary Basin Periphery, respectively). When we compared combined data from both basins to those of the Intrabasin Flats we found strong evidence for unequal mean CH4 emissions (Welch’s t-test; p = 0.004), with mean emissions from the basins roughly three times greater.

Fig 2

Tukey’s boxplots of methane emissions data from three sites at the Los Amigos peat swamp in Madre de Dios, Peru.

Whiskers extend to data within 1.5 of intra-quartile range; no outliers were removed. Letters correspond to results of Tukey’s honest significant differences test at α = 0.05. The data used to generate this figure can be found in S1 Table.

Poren class="Chemical">water n class="Chemical">CH4 concentrations followed a pattern mirroring that of emissions across the CICRA peatland. We found the two measures to be highly correlated (r2 = 0.99) after removing one outlier (for which porewater CH4 was more than double the next highest value from the data set) from the Secondary Basin Interior (Fig 3).

Fig 3

Mean (± standard error) methane emissions and methane dissolved in soil pore water from three sites at the Los Amigos peat swamp in Madre de Dios, Peru.

The data used to generate this figure can be found in S1 Table.

Many of the soil properties also showed significant variability between sites and may help explain site CH4 flux differences. The Intrabasin Flats stood out from one or both of the secondary basin sites for having significantly higher total phosphorus, soluble phenolics and pH (see Table 1). Soils of the two basin sites appeared to be more similar though the periphery had significantly less total nitrogen and carbon compared to the interior site.

Table 1

Mean (± standard deviation) surface soil (0–40 cm) chemistry (total nitrogen, total carbon, total phosphorus, phenolic compounds, extractable nitrate/nitrite, extractable ammonia/ammonium, water pH, salt pH) from three sites at the Los Amigos peat swamp in Madre de Dios, Peru.

Letters (a,b) refer to Tukey groupings and bold indicates where Tukey’s honest significant differences were found between sites. The data used to generate these values can be found in S2 Table.

Site	TN	TC	TP	Phenol	NOx	NHx	pH aq	pH salt
	%	%	μg g-1	μg C g-1	μg g-1	μg g-1	-	-
Basin Periphery	1.80a	33.9a	832a	222ab	0.24a	0.57a	5.63ab	3.56a
	±0.20	±4.4	±74	±16	±0.02	±0.08	±0.10	±0.11
Basin Interior	2.18b	42.4b	801a	208a	0.21a	0.68a	5.48a	3.57a
	±0.19	±1.7	±155	±50	±0.17	±0.61	±0.22	±0.16
Interbasin Flats	2.31b	41.9b	1060b	357b	0.19a	0.56a	5.92b	3.92b
	±0.19	±1.0	±51	±156	±0.20	±0.60	±0.25	±0.06

Overall the M. flexuosa-dominated Secondary Basin of the CICRA peatland emitted on average 14.0 ± 2.4 mg CH4 m-2 h-1, and the open-canopy Cyperacea-dominated Intrabasin Flats emitted 4.7 ± 0.9 mg CH4 m-2 h-1. By averaging these values with those reported for other neotropical peatlands (Table 2), we estimate that 750,000 km2 of such systems [6] will emit 43 ± 11.9 Tg CH4 y-1. However, emissions rates vary by nearly an order of magnitude across sites despite the fact that almost all of data comes from Peru.

Table 2

Summary of published CH4 emissions data from neotropical peatlands.

Location	Peatland Type	CH4 flux	Source
		mg CH4 m-2 h-1
Panama	Raphia taedigera Swamp	7.1	Wright et al 2013 [29]
Peru	Mauritia flexuosa Swamp	8.9	Van Haren and Cadillo-Quiroz 2015 [30]
N. Peru	Mauritia flexuosa Swamp	2.0	Murphy et al 2016 [31]
N. Peru	Mixed Palm Swamp	2.9	Murphy et al 2016 [31]
S. Peru	Mauritia flexuosa Swamp	14.0	this study
S. Peru	Cyperaceae Swamp	4.7	this study
Mean		6.6
Std. Dev.		4.4

Discussion

Vegetation

We found little evidence to support the hypothesis that the magnitudes of CH4 emission from palm-dominated and open herbaceous neotropical peatlands are similar. Methane emissions were lower from the open-canopy herbaceous zone of the Intrabasin Flats compared to emissions from the adjacent palm-dominated Secondary Basin, but given that these are the only CH4 measurements available for this poorly studied peatland type, it is impossible to know whether our result is generalizable to other regions of Amazonia. Typically, higher productivity wetlands emit more CH4 because of increased inputs of carbon substrate [32] and based on high rates of peat accumulation, M. flexuosa systems are thought to be highly productive [33]. Therefore it is likely that higher net primary productivity in the palm-dominated versus herbaceous zones of the CICRA peatland may be driving the differences in CH4 emissions we observed, but further research on the productivity and CH4 of these systems is needed.

Neotropical peatlands have yet to be systematically classified into dominant vegetation zones, but based on remote sensing of the Pastaza-Marañon foreland basin peatland complex in northern Peru, palm swamps dominate, covering 78% of total peatland areas [34].

Pole forest, for which no n class="Chemical">CH4 data is available, and Open-canopy herbaceous areas, for which we provide the first n class="Chemical">CH4 emissions measurements, each cover roughly equal parts of the remaining 22% [34].

The finding that significant quantities of CH4 are emitted through M. flexuosa palm trunks also suggests that CH4 emissions from palm-dominated peatlands based on soil flux chambers alone may be underestimating total efflux rates by 20% [30]. Emissions via woody vegetation has been shown to account for 62 to 87% of ecosystem CH4 emissions in a southeast Asian peatland [35] and further research in a temperate wetland found that unlike soil emissions, water table fluctuations had a minimal impact of tree stem CH4 flux [36]. It is possible that emissions via M. flexuosa trunks are proportionally more important to net CH4 flux during dry seasons when CH4 oxidation can be high if surface soils become exposed. More work is needed to investigate how much CH4 is emitted through plants in other Amazonian peatlands and whether the relative strength of tree flux varies with hydrology as soil flux does.

Soil properties

Although we found CH4 emissions to diminish along a distance gradient from grounpan>dwater seep sources, the ombrotrophic conditions we expected to find in the peatland interior proved not to exist. We actually found soil pH to be higher at the Intrabasin Flats, the opposite of the pattern we had predicted. Furthermore we found the Intrabasin Flats soils to have higher total phosphorus and nitrogen content compared to the basin sites closer to groundwater sources indicating that the hydrologic inputs to the center of the peatland are not dominated by precipitation. Thus distance from groundwater source turns out to be a poor predictor of nutrient limitation and trophic state in this context. It is likely the much shallower depth of the peat at the Intrabasin location could have enhanced the transfer of nutrients from the mineral substrate to the upper peat layers. However, the slightly higher pH and total nitrogen and phosphorus at the Intrabasin Flats cannot explain the low CH4 emissions and porewater concentrations we observed. Importantly, we did find significantly higher phenolic content in the Intrabasin Flats peat soil, which has been shown to decrease GHG fluxes and decomposition rates in southern compared to northern peatlands [12]. Further research is needed to test the importance of phenolics in tropical peatlands and our original hypothesis regarding ombrotrophic versus minerotrophic CH4 patterns in the neotropics. Truly ombrotrophic tropical peatlands are known to occur in northern Peru with coverage by M. flexuosa or pole forest [34,37] and our original hypothesis could be retested at these sites.

Hydrology

At the CIRCRA peatland, groundwater seeps from the adjacent terrace apparently keep the site perennially inunpan>dated [14] creating hydrologic conditions conducive to potent CH4 emissions year round. The strong correlation between soil porewater dissolved CH4 and emissions we found at the CICRA peatland is typical of wetlands with a months-long history of inundation and minimal CH4 oxidation capacity of soils [38]. The hydrologic setting at CICRA contrasts with that of a palm-dominated peatland in Panama where water levels and CH4 emissions rates fluctuate in concert with patterns of precipitation, resulting in relatively low mean CH4 emissions because of regular oxidation of surface soils [39]. High frequency CH4 measurements at CICRA and other Amazonian peatlands coupled with automated hydrologic monitoring will be needed to clarify the relationship between CH4 emissions and hydrology.

The high poren class="Chemical">water n class="Chemical">CH4 concentrations we found at the CICRA peatland may point to a potentially important source of underestimation in net ecosystem flux. Groundwater supersaturated with CH4 will feed into headwater streams where outgassing will occur from surfaces waters. This phenomenon has been documented in the Brazilian Amazon where researchers found high concentrations of CH4 in stream surface water which they attributed to allochthonous sources in the watershed [40].

Geographic distribution

The spatial clustering of CH4 studies in Peru (and the additional Panama site lying outside of the Amazon region) poses a serious regional bias problem in our analysis. The other data are sourced from northern Peru so our study in southern Peru does increase the spatial coverage, but CH4 dynamics of much of Amazonia’s peatlands remain unstudied. We also found in our data review that CH4 emissions rates from neotropical peatlands vary by nearly an order of magnitude. High variability combined with a small sample size of sites makes our estimate for the total contribution of these ecosystems to the global CH4 budget highly uncertain, but provides some of the first field evidence for the potential importance of these peatlands to the global CH4 budget. The latest study of the distributions of neotropical peatlands asserts that Colombia has an area of peat coverage comparable to that of Peru, while four times more exists in Brazil [6]. No studies of peatland CH4 emissions have been published to date in Brazil or Colombia, two of the world’s top four countries by tropical peatland area. Access is a major limitation as the vast majority of Amazonian peatland sites lie far from transportation infrastructure. Given the above noted constraints we estimate that the newly recognized vast areas of neotropical peatlands [6] may contribute 4.9 to 8.6 percent of the global CH4 budget of 645 Tg CH4 y-1 [41] based on the available ground-based data. This estimate is a first effort to bridge the ‘missing link’ of these tropical wetlands [2], but it will likely need significant revision as future studies lend additional data to the limited data set.

Conclusions

Methane fluxes were variable across the peat soil chemical gradient founpan>d in the swamp peatlands at Madre de Dios, Peru. Overall the more productive M. flexuosa-dominated swamp sites on deep peat emitted CH4 at three times the rate found in the shallower peat open-canopy Cyperacea-dominated flats. The lower rates were found at sites with higher phenolics, N and P content as well as higher pH. Improvements to our understanding of the relationship between hydrology, vegetation community, productivity, soil chemistry and CH4 emissions from these ecosystems will hopefully allow us to better extrapolate from inevitably sparse spatial and temporal flux measurements leading to further refinements in estimates of tropical fluxes of CH4.

The past decade of growth in atmospheric concentrations of n class="Chemical">CH4 appears to be associated with a tropical biogenic source, which highlights the need for further study of biogeochemical funpan>ctioninpan>g of tropical wetlands [42]. Loominpan>g threats to Amazonia make the need for further research inpan> these peatlands especially urgent. A recent study has founpan>d that Amazonian forests may be less resilient to drought and fire than previously thought, with floodplainpan>s representinpan>g an ‘Achilles heel’ [43]. Inpan> additional to potential impacts posed by climate change, unpan>regulated minpan>inpan>g [14] and the expansion of commercial agriculture are serious anthropogenic threats to the hydrologic and ecologic inpan>tegrity of Amazonian peatlands [44]. It will be critical to unpan>derstand the ecological and biogeochemical funpan>ctioninpan>g of these ecosystems before they are funpan>damentally altered by anthropogenic change.

Methane emissions and dissolved methane in porewater at 10 to 15 cm depth from three sites at the CICRA Peatland in Madre de Dios, Peru.

(XLSX)

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Soil chemistry data from three sites at the CICRA in Madre de Dios, Peru.

(XLSX)

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