Archaea

Volume 2013 (2013), Article ID 582646, 13 pages

http://dx.doi.org/10.1155/2013/582646

Research Article

Dynamics of the Methanogenic Archaea in Tropical Estuarine Sediments

María del Rocío Torres-Alvarado,¹ Francisco José Fernández,² Florina Ramírez Vives,² and Francisco Varona-Cordero¹

¹Department of Hydrobiology, Universidad Autónoma Metropolitana-Iztapalapa, Avenida San Rafael Atlixco No. 86, Colonia Vicentina, 09340 Mexico City, DF, Mexico

²Department of Biotechnology, Universidad Autónoma Metropolitana-Iztapalapa, Avenida San Rafael Atlixco No. 86, Colonia Vicentina, 09340 Mexico City, DF, Mexico

Received 27 July 2012; Revised 30 October 2012; Accepted 3 December 2012

Academic Editor: Martin Krüger

Copyright © 2013 María del Rocío Torres-Alvarado et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

Methanogenesis may represent a key process in the terminal phases of anaerobic organic matter mineralization in sediments of coastal lagoons. The aim of the present work was to study the temporal and spatial dynamics of methanogenic archaea in sediments of tropical coastal lagoons and their relationship with environmental changes in order to determine how these influence methanogenic community. Sediment samples were collected during the dry (February, May, and early June) and rainy seasons (July, October, and November). Microbiological analysis included the quantification of viable methanogenic archaea (MA) with three substrates and the evaluation of kinetic activity from acetate in the presence and absence of sulfate. The environmental variables assessed were temperature, pH, Eh, salinity, sulfate, solids content, organic carbon, and carbohydrates. MA abundance was significantly higher in the rainy season (10⁶–10⁷ cells/g) compared with the dry season (10⁴–10⁶ cells/g), with methanol as an important substrate. At spatial level, MA were detected in the two layers analyzed, and no important variations were observed either in MA abundance or activity. Salinity, sulfate, solids, organic carbon, and Eh were the environmental variables related to methanogenic community. A conceptual model is proposed to explain the dynamics of the MA.

1. Introduction

Coastal and marine environments, including estuaries and coastal lagoons, are characterized by large amounts of organic matter, which is mineralized primarily in sediments through anaerobic processes, sulfate reduction being the dominant metabolic pathway [1, 2]. However, although these ecosystems are the typical habitat of sulfate-reducing prokaryotes (SRP), methanogenic archaea (MA) and methane production have also been detected [3, 4].

MA are strict anaerobes that produce methane as end-product of their metabolism. These organisms are common in anoxic environments in which electron acceptors such as nitrate and sulfate are either absents or present at low concentrations and are usually dominant in freshwater environments. In the presence of these electron acceptors, methanogenesis is outcompeted by anaerobic respiration, mainly for thermodynamic reasons [5]. MA distribution patterns and its number, as well as physical, chemical, and nutritional parameters controlling their abundance and distribution have been studied in lacustrine sediments [6] and in coastal environments [7, 8].

Most of the ecological studies assessing the structure of methanogenic communities in estuarine systems have been performed in temperate latitudes where temperature is one of the major factors regulating ecosystem function. These investigations have included an evaluation of the MA in the intertidal zone of marshes with the presence of Spartina alterniflora, whose roots provide organic carbon and contribute to create aerobic microhabitats [9, 10]. MA abundance has been quantified with two or three substrates, of which acetate and hydrogen have been reported as the two most important ones [4, 11]. Additionally, it has been established that in estuaries, where a salinity gradient exists from the marine zone to a river entrance, MA are prevalent upstream in the freshwater region and decrease towards the brackish and marine ends; sulfate reduction has been identified as the key factor related to the MA distribution [7, 10, 12, 13]. Depth profiles of MA distribution have been observed, their abundance increase in deeper layers of the sediment column, because the MA are dependent on heterotrophs and fermenters during the organic matter decomposition, its decline is also related to a decrease in both sulfate concentration and redox potential [8].

In contrast to estuaries, coastal lagoons generally have restricted communication with the sea and in tropical lagoons, as a result of strong seasonal precipitation patterns, there are significant fluctuations in river discharge, and associated hydrological conditions (salinity). These variations might affect the structure of microbial communities involved in the terminal phases of the anaerobic organic matter mineralization, as well as to the biogeochemical processes related to it. In spite of its importance, studies focused on these ecosystems to assess the dynamics of anaerobic microbiota, especially MA, are scarce. It has been reported that MA using methylamines are the primary microbial components in sediments of coastal lagoons associated to mangroves, with higher densities during the summer and premonsoon [14, 15]. In another study, a peak of methane production in mangrove sediments has been recorded in the postmonsoon season [16]. In Mexico, where coastal lagoons are abundant, investigations on methanogenic communities are virtually absent; hence, the aim of the present study was to explore the spatial and temporal dynamics of the methanogenic community in sediments from two tropical coastal systems: Chantuto-Panzacola and Carretas-Pereyra, located in the Mexican southern Pacific and to propose a conceptual model on MA dynamics in sediments for the tropical coastal lagoons studied.

2. Materials and Methods

2.1. Study Site

The Chantuto-Panzacola and Carretas-Pereyra lagoon systems are located in the State of Chiapas, Mexican Pacific coast (Figure 1); they are part of the International Biosphere Reserve “La Encrucijada”. The climate of the region is warm (28°C) and humid (89%) with abundant summer rainfall; annual rainfall ranges between 1,300 and 3,000 mm. The rainy season begins between May and June and continues through November; the dry season occurs from December to May [17]. Lagoon systems are characterized by high temperatures in the water column (29–35.5°C), with a variable salinity ranging from 0 to 34.5‰  in Chantuto-Panzacola and from 0 to 22.7‰  in Carretas-Pereyra, depending on the season. There is a limited exchange with the sea and a significant phosphorus supply from rivers, which favors high chlorophyll-a levels. Systems are bordered by mangrove forests and freshwater wetlands. Mangrove detritus results in high humic substance levels (>150 mg/L) in the rainy season [18] also recording high ammonium concentrations derived from mineralization [19].

(a)  Coastal lagoon system of Carretas-Pereyra, Chiapas

(b) Coastal lagoon system of Chantuto-Panzacola, Chiapas

Figure 1: Study area and sampling sites (●).

The Chantuto-Panzacola lagoon has an area of 18,000 ha and comprises five lagoons: Chantuto, Campón, Teculapa, Cerritos, and Panzacola. In this system, samples were collected from the Cerritos and Campón lagoons (Figure 1). The Cerritos lagoon (15°09′54.4′′N, 92°45′34.0′′W) has a mean depth of 1.1 m in the dry season and 1.3 m during the rainy season. The Cintalapa River flows into this lagoon, contributing a volume between 66.2 m³/s in October and 0.4 m³/s in May (dates proportionated by the National Water Commission in Mexico). The Campon lagoon (15°12′30.0′′N, 92°51′24.2′′W) has a mean depth of 0.8 m in the dry season and of 0.9 m in the rainy season. The Cacaluta River flows into this lagoon, with a maximum inflow in October (144.2 m³/s) and a minimum inflow in May (0.5 m³/s). Sediments are a mixture of silt and sand in both lagoons. The Carretas-Pereyra system covers an area of 3,696 ha and comprises four water bodies: Pereyra, Carretas, Bobo, and Buenavista, sampling took place in Pereyra and Bobo (Figure 1). The Pereyra lagoon (15°31′26.1′′N, 92°51′24.2′′W) has a mean depth of 0.7 m in the dry season and 1.0 m in the rainy season. Sediment is silt-sand. The Margaritas River drains into the Pereyra lagoon (discharge volume unknown). The Bobo lagoon (15°29′22.0′′N, 93°08′44.6′′W) has a mean depth of 0.5 m and 0.7 m in the dry and rainy seasons, respectively. It lacks freshwater inputs and sediment is silt-sand.

2.2. Sample Collection and Preparation Procedures

Sediment cores were collected with a 45 cm long and 4.5 cm wide plexiglass coring device during the dry (February, May, and early June) and rainy seasons (July, October, and November). Temperature, Eh, and pH were simultaneously measured when sampling the cores at two sediment depths (6 and 12 cm) using standard electrodes and an Ionanalizer (Conductronic pH 120). pH was measured with a glass electrode and the sediment redox potential was measured using a platinum electrode and a saturated KCl calomel reference electrode (Instrulab, Mexico). The standard potential of the reference (+198) was added to the mean value to obtain the Eh of the sediment medium. Electrodes were routinely standardized in the field using a ZoBell Solution [20]. Subsequently, samples were transported to the laboratory.

Cores obtained in each sampling station were segmented in two sections (0–6 cm and 6–12 cm) under a nitrogen atmosphere. After each section was homogenized in a plastic bag using steady shaking, subsamples were immediately taken to quantify MA. The remaining sediment was maintained under low temperature to perform physical-chemical analyses.

2.3. Microbiological Analyses

Enumeration of viable MA was performed using the Most Probable Number (MPN) method by a ten-fold dilution series (10⁻¹ to 10⁻¹⁰) for each sample using four tubes per dilution. The MPN analyses included the quantification with substrates commonly used by the different groups of MA: acetate, CO₂ + H₂, and methanol, with the basic medium by Balch et al. [21]. Salinity in the culture medium was adjusted with a NaCl (330 g/L) solution to obtain similar values to those measured in the original sediment sample; the pH was adjusted to 7.2 with a bicarbonate (10%) solution. Cultures were incubated at 32°C for one month. Methane was detected with a GOW-MAC Series 580 GC with a thermal conductivity detector (TCD) under the following operation conditions: column, detector, and injector temperatures of 140, 190, and 170°C, respectively; 25°C/min rate; column packed with carbosphere 80/100, helium as carrier gas at 25 mL/min; polarity of 120 mA.

In order to determine the effect of sulfate on MA for a competitive substrate, methanogenic activity was determined in a medium without sulfates (sulfate-free), using 125-mL serum bottles, with 42 mL of the Balch et al. [21] and acetate as substrate to a final concentration of 20 mM. Experiments were conducted in parallel in which the culture medium was supplemented with sulfate (final concentration 20 mM). Bottles were inoculated with 8 mL of moist sediment and incubated at 32°C in the dark for 42 days; the incubations were shaken three times per week. Each experiment was run by duplicate for each sample, including the respective controls (without acetate), with and without sulfates in the medium. Mineralization was evaluated by determining changes in acetate concentration and percent methane production in bottles. For acetate analysis, 1.5 mL samples were centrifuged at 1,120 gf for 10 min. The supernatant was filtered. A 950 μL aliquot was acidified with 50 μL of HCl (2.2 M). The acetate concentration was measured by flame ionization gas chromatography (Agilent Series 6890 Plus) using an Agilent crosslinked FFAP capillary column (15 m × 0.530 mm × 1.00 μm). Column, injection port, and FID temperatures were 120, 130, and 150°C, respectively. The temperature of the column, detector, and injector were 120, 150, and 130°C, respectively. The carrier gas was N₂ (4.5 mL/min).

2.4. Physicochemical Analyses

Sediment samples were centrifuged at 1,602.76 gf at low temperature (4-5°C) for 20 minutes to separate porewater from sediments [22]. Porewater was filtered through 0.45 μm Millipore membranes and the following parameters were determined: salinity, with an optical refractometer (American Optical); sulfate [23] and total dissolved carbohydrates, with the phenol-sulfuric acid technique [24]. Total solids and volatile solids were quantified in moist sediments [25], porosity was determinate by measuring the weight loss by drying sediment samples of know volumes and weights. Organic carbon content was measured through the method by Gaudette et al. [26] in a sediment sample dried at 60°C.

2.5. Statistical Analyses

The data matrix included MA abundances and physicochemical variables. To meet the normality assumptions, data for variables were transformed through [27]. For the temporal analysis, variables were grouped into two climate seasons (dry and rainy); for the spatial analysis, data were grouped into two depth categories (0–6 cm and 6–12 cm). An analysis of variance (ANOVA) was conducted to test for significant differences between seasons in each system, on the one hand, and between depth categories, on the other. The significance of specific differences was assessed through the Tukey-Kramer multiple comparison test [27]. A Canonical Correspondence Analysis (CCA) was used to investigate the relationship between microbial abundance and environmental variables [28]. These analyses were conducted with the Statistica 10 (Academic) and MVSP 3.12b Software.

3. Results and Discussion

The aim of this study was to analyze the changes in the abundance and activity of MA and relate these community characteristics with some physicochemical variables to propose a conceptual model of methanogenic community dynamics in coastal lagoon sediments.

3.1. Environmental Variables

Conditions in the sedimentary habitat in the Chantuto-Panzacola and Carretas-Pereyra lagoon systems resulted from seasonal variations between the dry and rainy seasons. Temperature in the sediment was higher in the dry season in comparison with rainy season (Table 1); the temporal variations were significant in Chantuto-Panzacola (Table 2). Significant differences in pH were observed (Table 2). In the dry season, a greater marine influence favors neutral conditions; by contrast, in the rainy season the higher fluvial inflow decreased marine influence, and acid conditions were registered (Table 1). The redox conditions were similar to those reported for sediments from mangroves [29] and were significantly less reductive in the rainy season (Table 1) when the freshwater inflow favored sediment suspension in the water column (turbidity = 126–224 NTU), with an increase in porosity and less reduced conditions at the sediments. In the dry season redox potential decreased as a result of sediment deposition (turbidity = 31–107 NTU).

Table 1: Environmental variables in the coastal lagoon sediments of Chantuto-Panzacola and Carretas-Pereyra, Chiapas. Mean ± Standard deviation.

Dry season
Rainy season

Depth
6
12
6
12

Chantuto-Panzacola

Temperature (°C)

Salinity (‰)

Sulphate (mM)

pH

Eh (mV)
−206 ± 76
−356 ± 34
−104 ± 4
−286 ± 53

Total Solids (TS, g/L)

Volatile Solids (VS, g/L)

Porosity (g/cm³)

Organic matter (%)

Organic carbon (%)

Carbohydrates (mg/L)

Carretas-Pereyra

Temperature (°C)

Salinity (‰)

Sulphate (mM)

pH

Eh (mV)
−296 ± 83
−411 ± 66
−152 ± 46
−369 ± 99

Total Solids (TS, g/L)

Volatile Solids (VS, g/L)

Porosity (g/cm³)

Organic matter (%)

Organic carbon (%)

Carbohydrates (mg/L)

Table 2: Results of the ANOVA (F) and multiple comparisons analysis (MCA) (Tukey test) of environmental and microbiological variables between seasons and sediment depth in Chantuto-Panzacola and Carretas-Pereyra. P: significance. Seasons: D: dry and R: rainy. Depth: 6 cm and 12 cm.

Variables
Season
Depth

F
P
MCA
F
P
MCA

Chantuto-Panzacola

Temperature (°C)
4.66
0.0421
D > R
3.75
0.0684
—

Salinity (‰)
62.03
0.0000
D > R
0.08
0.9311
—

Sulphate (mM)
109.00
0.0000
D > R
0.45
0.5349
—

pH
28.81
0.0000
D > R
0.01
0.9427
—

Eh (mV)
4.54
0.0446
D < R
38.04
0.0000
6 < 12

MA-Acetate (cells/g)
112.38
0.0000
D < R
0.01
0.7842
—

MA-Hydrogen (cells/g)
15.10
0.0008
D < R
0.05
0.8195
—

MA-Methanol (cells/g)
5.92
0.0236
D < R
3.36
0.0528
—

Activity + SO₄ (mM acetate/g VS/day)
14.71
0.0009
D > R
1.50
0.2321
—

CH₄ + SO₄
66.12
0.0000
D < R
0.85
0.3085
—

CH₄ − SO₄
4.96
0.0364
D < R
2.17
0.0831
—

Carretas-Pereyra

Temperature (°C)
0.97
0.3344

1.28
0.2705
—

Salinity (‰)
154.47
0.0000
D > R
0.26
0.6156
—

Sulphate (mM)
210.03
0.0000
D > R
0.45
0.5101
—

pH
10.47
0.0038
D > R
1.09
0.3088
—

Eh (mV)
3.80
0.0641
—
19.80
0.0002
6 < 12

MA-Acetate (cells/g)
4.82
0.0390
D < R
0.13
0.7193
—

MA-Hydrogen (cells/g)
9.39
0.0057
D < R
0.48
0.4952
—

MA-Methanol (cells/g)
2.71
0.1142
—
1.06
0.3142
—

Activity + SO₄ (mM acetate/g VS/day)
12.62
0.0018
D > R
0.46
0.5042
—

CH₄ + SO₄
15.39
0.0007
D < R
6.24
0.0204
6 < 12

CH₄ − SO₄
7.21
0.0135
D < R
7.88
0.0103
6 < 12

The major changes were determined in salinity and sulfate content (Tables 1 and 2). Maximum values were recorded in the dry season and minimum in the rainy season; even totally freshwater conditions existed in both systems in October (0‰). The decrease in salinity and sulfates was due to an increase in fluvial inflow and precipitation. Salinity in coastal lagoons varies according to annual cycles, which depend on the local climate, continental freshwater runoff, connection with the sea, and influence of tides. Knoppers and Kjerfve [30] point out that seasonal pulses in freshwater inflow exert a marked impact on the ecology of coastal lagoons, besides controlling salinity, increasing the water level, and holding open communication to the sea.

No significant temporal variations were observed in the concentration of total solids and organic fractions (volatile solids, organic matter, organic carbon, and carbohydrates) (); and their supply was constant through rivers and wetlands. The high rate of freshwater inflow with organic debris from land and run-off as well as from adjacent mangroves is a key factor related to the contribution of organic matter in coastal zones [31].

Spatially there was no pattern of physicochemical conditions in the sedimentary habitat as evidenced by the null significance observed for the temperature, pH, salinity and sulfates (). An exception was the Eh, which decreased significantly with depth (Tables 1 and 2). The vertical fluctuations in Eh may be attributed to a reduction in the oxygen diffusion rate in porewater as the depth of the sediment column increases [32]. There were no significant variations in solids content and organic fractions () (Table 1). However the organic carbon content was higher in the sediment layer of 12 cm, dos Santos Fonseca et al. [33] point out that this behavior seems to result from the fact that the most labile substrate is readily used by the microbial community in the top centimeters of sediment, and the refractory fraction builds up in deeper layers, where it will be degraded slowly. The presence of refractory material (wood and phytoplankton debris identified with a light microscope Zeiss Axioscop) concentrated largely in the 6–12 cm-deep layer in Pereyra and Campón lagoons seem to support this hypothesis.

3.2. Abundance and Distribution of MA

Viable MA in the sediments of Chantuto-Panzacola and Carretas-Pereyra systems were evaluated with MPN, obtaining a range of abundance between 10⁴ and 10⁷ cells/g. MA density reached peak levels in the rainy season, with a significant decrease of as much as two orders of magnitude during the dry season () (Figures 2(a)–2(c)). In the rainy season, increased freshwater input created favorable conditions for MA proliferation. In this season highest levels of MA were recorded with acetate and methanol in Chantuto-Panzacola and with methanol and H₂-CO₂ in Carretas-Pereyra. During the dry season, high MA levels were obtained with methanol in both lagoon systems; the second substrate in importance was H₂-CO₂ and the lowest levels correspond to acetate (Table 3).

Table 3: Abundance of MA, acetoclastic activity, and methane production in sediments of Chantuto-Panzacola and Carretas-Pereyra, Chiapas. Mean values.

Dry season
Rainy season

Depth
6
12
6
12

Chantuto-Panzacola

MA-acetate (cells/g)
1.30 × 10⁵
2.99 × 10⁴
2.20 × 10⁷
2.09 × 10⁷

MA-Hydrogen (cells/g)
1.63 × 10⁶
9.55 × 10⁴
9.37 × 10⁶
8.63 × 10⁶

MA-methanol (cells/g)
1.79 × 10⁶
1.97 × 10⁷
1.17 × 10⁷
2.06 × 10⁷

Acetate activity without (mM acetate/g VS/day)
0.03
0.03
0.02
0.01

Acetate activity with (mM acetate/g VS/day)
0.05
0.03
0.01
0.01

% CH₄ without
4.81
7.91
23.50
29.73

% CH₄ with
2.78
4.63
5.64
8.77

Carretas-Pereyra

MA-acetate (cells/g)
4.52 × 10⁴
6.17 × 10⁴
1.90 × 10⁶
1.32 × 10⁶

MA-Hydrogen (cells/g)
1.34 × 10⁵
1.51 × 10⁵
4.49 × 10⁶
2.64 × 10⁶

MA-methanol (cells/g)
1.34 × 10⁶
8.24 × 10⁶
1.27 × 10⁷
2.21 × 10⁷

Acetate activity without (mM acetate/g VS/day)
0.03
0.02
0.01
0.01

Acetate activity with   (mM acetate/g VS/day)
0.04
0.03
0.01
0.01

% CH₄ without
7.83
13.01
15.42
23.47

% CH₄ with
4.02
6.55
6.41
13.02

Figure 2: Temporal and spatial variation in the abundance of MA (log cells/g TS).

The constant occurrence of MA was probably the result of their ability to use different electron donors in an ecosystem with a constant supply of organic matter provided by the rivers and run-off from adjacent mangroves. Verma et al. [34] mentioned that the continued presence of MA in coastal lagoons is possible by the presence of “noncompetitive” substrates, (methanol and methylamines), that are used exclusively by the MA, as well as the constant availability of “competitive” substrates (acetate and hydrogen), used by methanogen and other anaerobic microorganisms.

Methanol was an important substrate in both seasons, may be released from methoxy groups during degradation of lignin. Methanol-utilizing MA have a broad substrate spectrum, can also grow on acetate, growth on H₂-CO₂ is restricted to some Methanosarcina species [5]. There is evidence supporting the hypothesis that cometabolism of a broad range of substrates by generalist microorganisms may confer competitive advantages [35]. Purdy et al. [13] mention that, within the methanogenic community, the presence of generalist groups implies that these are better adapted to the variations in the estuarine conditions. Additionally methanol allows MA to maintain their populations in the presence of sulfate, which act favoring sulfate reduction. The key role of other methylated compounds was demonstrated in mangrove areas in India, where MA were quantified from methylamines [14, 15].

In the rainy season, methanol remained important, but the abundance of MA from hydrogen and acetate increased under low sulfate concentrations, hydrogen theoretically contributes 33% to total methanogenesis when carbohydrates or similar organic matter are degraded, being important in environments with high sedimentation rates (≈10 cm/year) and organic carbon supplementation [36]. In the coastal lagoons studied, a high concentration of organic carbon (3.4–14.5%) was quantified, and a sedimentation rate of 6 cm/year was observed in Carretas-Pereyra. Acetate can produce approximately two thirds of total methane in freshwater sediments; however, its contribution to methane formation decreases when is consumed in other anaerobic processes as the sulfate reduction [4]. The effect of sulfate on methanogenesis was demonstrated in temperate estuaries, where the contribution of acetate for this process has been found to increase when sulfate concentration is low in freshwater zone, and the sulfate reduction decreased [7, 13]. The acetate and hydrogen are also important substrates for methanogenesis in salt marshes areas [10].

This study has revealed that acetate-utilizing and hydrogen-utilizing MA does not have a distinct vertical distribution pattern in Chantuto-Panzacola and Carretas-Pereyra sediments, whereas the methanol-based group apparently being more abundant in the 6–12 cm layer (). The presence of MA along 12 cm of sediment column seems to be a result of the availability of substrates for these microorganisms; the constant supply of different substrates favors the presence of MA at different sediment layers as also has been demonstrated in sediments of tidal flats, coastal marshes, and mangroves [8, 10, 14].

3.3. Acetoclastic Metabolic Activity

In all kinetic experiments, there was an increase in the concentration of acetate in the first days, along with other volatile fatty acids (propionate and butyrate); this pattern reveals the presence of fermentation processes in sediments. The continued presence of acetate along with other intermediaries (butyrate and propionate) is similar to that reported in other studies where methanogenesis has been assessed [37]. Acetate is an important intermediate produced during the anaerobic mineralization of organic matter, followed by propionate and other volatile fatty acids [38]. The fermentation activity is important because it releases organic substrates, such as acetate, that can be used by the MA, which cannot directly use complex organic compounds. Subsequent to the production of volatile fatty acids, acetate consumption started on day 7 in sulfate-enriched media and between days 14 and 21 in sulfate-free media. Methane production was recorded on day 21.

Acetoclastic activity in sulfate-free experiments had no significant temporary differences () (Figures 3(a)–3(c)). The experiments with sulfate showed significant temporal fluctuations, with high values in the dry season (Table 3; Figures 3(a)–3(c)). Vertical variations did not reach statistical significance ().

Figure 3: Temporal and spatial variations of acetoclastic activity and methane production in Chantuto-Panzacola (a, b) and Carretas-Pereyra (c, d).

Methane formation was observed in all experiments, with differences depending on the specific conditions of each medium. The addition of acetate results in an increase in methane production in relation to the amount observed in controls (no carbon supplementation).

Methane production was higher in sulfate-free media compared with sulfate-enriched media (Table 3; Figures 3(b)–3(d)). Temporal differences () in methane production from acetate were observed in both systems. Methane levels were higher in the rainy season than in the dry season (Table 3). Significant vertical changes () were observed only in Carretas-Pereyra: a lower production in the upper 6 cm and a higher methane production in the 6–12 cm layer (Table 3, Figures 3(b)–3(d)).

The presence of sulfate in the culture media influenced methanogenic activity. In the sulfate-free experiments a peak of acetoclastic activity was observed coupled with a rise in methane production in sediments during the rainy season and in the deep layer, suggesting that methanogenesis was favored. Studies demonstrated that potential methanogenesis from acetate was higher in the absence of sulfates [37]. By contrast, the addition of sulfate resulted in an increase of acetoclastic activity in the dry months and in the upper sediment layer, and methane production declined. In sediments of coastal lagoons and mangrove areas in India, an increase in the production and emission of methane was determined in freshwater areas compared to brackish regions. Also, methane emissions were higher in the postmonsoon season, when salinity and sulfate concentration were lower [16, 34].

3.4. Environmental Variables and MA

The correlation coefficients between environmental variables and ordination axes (interset correlation) obtained by CCA denote the relative importance of each environmental variable in the distribution of the methanogenic community. For Chantuto-Panzacola, the MA-environment correlation was 0.92 corresponded to a salinity-sulfate gradient and 0.60 for pH. CCA results for Carretas-Pereyra showed a correlation of 0.74 for pH and volatile solids, and 0.43 for volatile solids. The ordination diagram obtained by CCA showed a change in the structure of the methanogenic community with regard to certain environmental variables (Figure 4). The first axis accounted for 65.62% of total variance in Chantuto-Panzacola, corresponding to a salinity-sulfate gradient (Figure 4(a)). In the right side of the diagram, those sites with the highest sulfate concentration, temperature, and pH (dry season) were grouped, in these conditions methanol-utilizing MA were abundant. The left side of the plot-grouped sites with highest total solids content where hydrogen-utilizing MA prospered, whereas acetate-utilizing MA abound in sites with a higher porosity and less reduced conditions (Figure 4(a)). In Carretas-Pereyra, to the plot’s upper left side, the first axis accounted for 29.08% of variance and salinity-sulfate, Eh and organic carbon concentration were all correlated with hydrogen-utilizing MA abundance, mainly during the rainy season. Abundance of methanol-utilizing MA was correlated with volatile solids during the dry season and acetate-utilizing MA prospered in a pH gradient in both seasons.

(a)

(b)

Figure 4: Relationship between environmental variables and methanogenic community in Chantuto-Panzacola (a) and Carretas-Pereyra (b).

The presence of sulfate significantly influenced the abundance of MA in both systems. In sulfate-rich conditions the anaerobic process that is most favored is the sulfate reduction. Elevated levels of SRP in the dry season (10⁸–10¹⁰ cells/g) and decrease in the rainy season (10⁵–10⁷ cells/g) quantified in coastal lagoons studied support this hypothesis [39]. The relationship between MA and sulfate content is consistent with knowledge on these communities in sediments of temperate estuaries, tropical coastal lagoons, coastal marshes, and mangroves [7–10, 13, 14, 16].

The temperature, pH, Eh, and organic fractions were other variables contributing to the presence of MA. In this study the bacteria grew in a temperature range of 26.7–29.4°C, the optimum temperature reported for the development of methanogens is 30–32°C in tropical wetlands, whereas in mangrove sediments MA have been observed at temperature ranges between 26 and 30°C [14, 15]. The pH conditions (6.7–7.1) were favorable for methanogenic community. Mohanraju and Natarajan [15] associated the presence of MA with pH values of 6.6–7.2 in mangrove sediments, whereas in coastal marshes sediments MA were recorded in pH ranges of 6.1–7.5 [10]. The reducing (−100 to +100 mV) and highly reducing (−300 to −100 mV) characteristics of sediment also contributed to MA development, these have been reported at levels from Eh below −150 mV in coastal marshes [40].

4. Conclusions

The MA was a constant component involved in anaerobic mineralization of organic matter in the sediments of the coastal systems Chantuto-Panzacola and Carretas-Pereyra. Their populations were active by its ability to utilize different substrates, especially methanol. In these ecosystems, changes in precipitation and its influence on fluvial inputs significantly impacted salinity and sulfate content, which was the main factor regulating the temporal dynamics of methanogenic community. In the rainy season, the increase in river inflow to lagoons produces freshwater conditions, low sulfate concentrations, sediment resuspension, and less reducing redox potentials. The environmental characteristics that prevail in this season lead to an increase in MA abundance, with the following decreasing rank by substrate: methanol > H₂-CO₂ > acetate (Figure 5(a)). Methanogenic activity from acetate is higher and results in a rise in methane production. The peak of methanogenic activity in the rainy season suggests that these ecosystems may be an important source of atmospheric CH₄ and CO₂ in this season. In the dry season, the freshwater inflow declines and salinity, sulfate, and inorganic solids content increases, along with more negative redox conditions. In this conditions a lower MA density was observed (Figure 5(b)), with the following order by substrate: methanol > acetate > H₂-CO₂. Our hypothesis is that this mechanism is cyclic and is controlled by changes associated to the seasonal fluctuations in fluvial inflow and precipitation. We considered that this model could be applied to other coastal lagoons and wetlands (mangroves) in tropical latitudes, characterized by a high organic matter concentration and a permanent river discharge, with significant seasonal variations in discharge volume. These characteristics favor the continued presence of the MA in tropical coastal systems and control their temporal dynamics. In estuaries, the absence of barriers that restrict communication with the sea difficult to apply this model because the tidal influence decreases the impact of freshwater input. In these systems the freshwater influence is more important at spatial level.

(a) Rainy season

(b) Dry season

Figure 5: Conceptual model on MA dynamics in sediments for tropical coastal lagoons.

Conflict of Interests

Authors of the paper have no conflict of interests with Millipore, Statistica 10 (Academic) and MVSP (3.12b Software). The authors do not have any association with Millipore or companies who designed Statistica 10 (Academic) and MVSP (3.12b Software).

Acknowledgment

This study was funded by the project “Ecological study of estuarine systems Chantuto-Panzacola and Carretas-Pereyra, Chiapas” DCBS, Universidad Autónoma Metropolitana-Iztapalapa.

References

B. B. Jørgensen, “Mineralization of organic matter in the sea bed—the role of sulphate reduction,” Nature, vol. 296, no. 5858, pp. 643–645, 1982.

M. Fukui, J. Suh, Y. Yonezawa, and Y. Urushigawa, “Major substrates for microbial sulfate reduction in the sediments of Ise Bay, Japan,” Ecological Research, vol. 12, no. 2, pp. 201–209, 1997.

D. Marty, P. Bonin, V. Michotey, and M. Bianchi, “Bacterial biogas production in coastal systems affected by freshwater inputs,” Continental Shelf Research, vol. 21, no. 18-19, pp. 2105–2115, 2001.

D. E. Canfield, E. Kristensen, and B. Thamdrup, “The methane cycle,” in Advances in Marine Biology. Aquatic Geomicrobiology, A. Southward, P. A. Tyler, C. M. Young, and L. A. Fuiman, Eds., vol. 48, chapter 10, pp. 383–418, Elsevier, London, UK, 2005.

R. K. Thauer, A. K. Kaster, H. Seedorf, W. Buckel, and R. Hedderich, “Methanogenic archaea: ecologically relevant differences in energy conservation,” Nature Reviews Microbiology, vol. 6, no. 8, pp. 579–591, 2008.

K. Zepp Falz, C. Holliger, R. Großkopf et al., “Vertical distribution of methanogens in the anoxic sediment of Rotsee (Switzerland),” Applied and Environmental Microbiology, vol. 65, no. 6, pp. 2402–2408, 1999.

K. J. Purdy, M. A. Munson, D. B. Nedwell, and T. M. Embley, “Comparison of the molecular diversity of the methanogenic community at the brackish and marine ends of a UK estuary,” FEMS Microbiology Ecology, vol. 39, no. 1, pp. 17–21, 2002.

R. Wilms, H. Sass, B. Köpke, J. Köster, H. Cypionka, and B. Engelen, “Specific Bacterial, Archaeal, and Eukaryotic communities in tidal-flat sediments along a vertical profile of several meters,” Applied and Environmental Microbiology, vol. 72, no. 4, pp. 2756–2764, 2006.

M. J. Franklin, J. W. William, and W. B. Whitman, “Populations of methanogenic bacteria in a Georgia salt marsh,” Applied and Environmental Microbiology, vol. 54, no. 5, pp. 1151–1157, 1988.

M. A. Munson, D. B. Nedwell, and T. M. Embley, “Phylogenetic diversity of Archaea in sediment samples from a coastal salt marsh,” Applied and Environmental Microbiology, vol. 63, no. 12, pp. 4729–4733, 1997.

R. Segers and S. W. M. Kengen, “Methane production as a function of anaerobic carbon mineralization: a process model,” Soil Biology and Biochemistry, vol. 30, no. 8-9, pp. 1107–1117, 1998.

S. Takii and M. Fukui, “Relative importance of methanogenesis, sulfate reduction and denitrification in sediments of the lower Tama river,” Bulletin of Japanese Society of Microbial Ecology, vol. 6, no. 1, pp. 9–17, 1991.

K. J. Purdy, M. A. Munson, T. Cresswell-Maynard, D. B. Nedwell, and T. M. Embley, “Use of 16S rRNA-targeted oligonucleotide probes to investigate function and phylogeny of sulphate-reducing bacteria and methanogenic archaea in a UK estuary,” FEMS Microbiology Ecology, vol. 44, no. 3, pp. 361–371, 2003.

T. Ramamurthy, R. Mohanraju, and R. Natarajan, “Distribution and ecology of methanogenic bacteria in mangrove sediments of Pitchavaram, east coast of India,” Indian Journal of Marine Sciences, vol. 19, no. 4, pp. 269–273, 1990.

R. Mohanraju and R. Natarajan, “Methanogenic bacteria in mangrove sediments,” Hydrobiologia, vol. 247, no. 1–3, pp. 187–193, 1992.

H. Biswas, S. K. Mukhopadhyay, S. Sen, and T. K. Jana, “Spatial and temporal patterns of methane dynamics in the tropical mangrove dominated estuary, NE coast of Bay of Bengal, India,” Journal of Marine Systems, vol. 68, no. 1-2, pp. 55–64, 2007.

INE-SEMARNAP, Programa de Manejo Reserva de la Biósfera La Encrucijada, Instituto Nacional de Ecología-Secretaría del Medio Ambiente, Recursos Naturales y, Pesca, Mexico, 1999.

F. J. Flores-Verdugo, F. González-Farías, D. S. Zamorano, and P. Ramírez-García, “Mangrove ecosystems of the Pacific Coast of Mexico: distribution, structure, litter fall, and detritus dynamics,” in Coastal Plant Communities of Latin America, U. Seliger, Ed., vol. 17, pp. 269–288, Academic Press, New York, NY, USA, 1992.

F. J. Flores-Verdugo, G. de la Lanza-Espino, F. Contreras-Espinosa, and C. M. Agraz-Hernández, “The tropical Pacific Coast of Mexico,” in Coastal Marine Ecosystems of Latin American, Ecological Studies, U. Seliger and B. Kjerve, Eds., vol. 144, pp. 307–314, Springer, Berlin, Germany, 2001.

D. Langmuir, “Eh-pH determination,” in Proceedings Sediments and Petrology, R. E. Conver, Ed., p. 653, Wiley-Interscience, New York, NY, USA, 1971.

W. E. Balch, G. E. Fox, L. J. Magrum, C. R. Woese, and R. S. Wolfe, “Methanogens: reevaluation of a unique biological group,” Microbiological Reviews, vol. 43, no. 2, pp. 260–296, 1979.

B. L. Howes, “Effects of sampling technique on measurements of porewater constituents in salt marsh sediments,” Limnology and Oceanography, vol. 30, no. 1, pp. 221–227, 1985.

R. W. Howarth, “A rapid and precise method for determining sulfate in seawater, estuarine waters, and sediment pore waters,” Limnology and Oceanography, vol. 23, no. 5, pp. 1066–1069, 1978.

M. Dubois, K. A. Gilles, J. K. Hamilton, P. A. Rebers, and F. Smith, “Colorimetric method for determination of sugars and related substances,” Analytical Chemistry, vol. 28, no. 3, pp. 350–356, 1956.

APHA, AWWA, and WPCF, Eds., Standard Methods For the Examination of Water and Wastewater, American Public Health Association, American Water Works Association and Water Pollution Control Federation, Washington, DC, USA, 2005.

H. Gaudette, W. Fligh, L. Toner, and D. Folger, “An inexpensive titration method for the determination of organic carbon in recent sediments,” Journal of Sediments and Petrology, vol. 44, no. 1, pp. 249–253, 1974.

J. H. Zar, Bioestatistical Analysis, Prentice Hall, New York, NY, USA, 1999.

C. J. F. Ter Braak, “Canonical correspondence analysis: a new eigenvector technique for multivariate direct gradient analysis,” Ecology, vol. 67, no. 5, pp. 1167–1179, 1986.

E. Lallier-Vergès, B. P. Perrussel, J. R. Disnar, and F. Baltzer, “Relationships between environmental conditions and the diagenetic evolution of organic matter derived from higher plants in a modern mangrove swamp system (Guadeloupe, French West Indies),” Organic Geochemistry, vol. 29, no. 5–7, pp. 1663–1686, 1998.

B. Knoppers and B. Kjerfve, “Coastal lagoons of Southeastern Brazil: physical and biogeochemical characteristics,” in Estuaries of South America, G. M. E. Perillo, M. C. Piccolo, and M. Pino-Quivira, Eds., pp. 35–66, Springer, New York, NY, USA, 1997.

M. R. Preston and P. Prodduturu, “Tidal variations of particulate carbohydrates in the Mersey estuary,” Estuarine, Coastal and Shelf Science, vol. 34, no. 1, pp. 37–48, 1992.

R. W. Howarth, “Microbial processes in salt-marsh sediments,” in Aquatic Microbiology, T. E. Ford, Ed., pp. 239–260, Blackwell Scientific Publications, Boston, Mass, USA, 1993.

A. L. dos Santos Fonseca, M. Minello, C. Cardoso Marinho, and F. de Assis Esteves, “Methane concentration in water column and in pore water of a coastal lagoon (Cabiúnas Lagoon, Macaé, RJ, Brazil),” Brazilian Archives of Biology and Technology, vol. 47, no. 2, pp. 301–308, 2004.

A. Verma, V. Subramanian, and R. Ramesh, “Methane emissions from a coastal lagoon: vembanad Lake, West Coast, India,” Chemosphere, vol. 47, no. 8, pp. 883–889, 2002.

T. Egli, “The ecological and physiological significance of the growth of heterotrophic microorganisms with mixtures of substrates,” in Advances in Microbial Ecology, J. Gwynfryn, Ed., vol. 14, pp. 305–386, Plenum Press, New York, NY, USA, 1995.

R. Conrad, “Contribution of hydrogen to methane production and control of hydrogen concentrations in methanogenic soils and sediments,” FEMS Microbiology Ecology, vol. 28, no. 3, pp. 193–202, 1999.

M. Holmer and E. Kristensen, “Coexistence of sulfate reduction and methane production in an organic-rich sediment,” Marine Ecology Progress Series, vol. 107, no. 1-2, pp. 177–184, 1994.

H. T. S. Boschker, W. de Graaf, M. Köster, L. A. Meyer-Reil, and T. E. Cappenberg, “Bacterial populations and processes involved in acetate and propionate consumption in anoxic brackish sediment,” FEMS Microbiology Ecology, vol. 35, no. 1, pp. 97–103, 2001.

M. R. Torres-Alvarado, Determinación de la diversidad y actividad bacteriana sulfatorreductora y metanogénica en los sedimentos de dos ecosistemas estuarino-lagunares del Estado de Chiapas [Ph.D. thesis], Universidad Autónoma Metropolitana-Iztapalapa, México, Mexico, 2009.

H. K. Kludze and R. D. DeLaune, “Methane emissions and growth of Spartina patens in response to soil redox intensity,” Soil Science Society of America Journal, vol. 58, no. 6, pp. 1838–1845, 1994.