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Article

Transformation of S-Bearing Minerals in Organic Matter-Rich Sediments from a Saline Lake with Hydrothermal Inputs

by
Gabriel Ricardo Cifuentes
1,
Juan Jiménez-Millán
2,*,
Claudia Patricia Quevedo
1 and
Rosario Jiménez-Espinosa
2
1
Faculty of Science and Engineering, Water Resources Research Group, University of Boyacá, Campus Tunja 15003, Colombia
2
Department of Geology and CEACTEMA, University of Jaén, Campus Las Lagunillas, 23071 Jaén, Spain
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(6), 525; https://0-doi-org.brum.beds.ac.uk/10.3390/min10060525
Submission received: 17 May 2020 / Revised: 5 June 2020 / Accepted: 5 June 2020 / Published: 9 June 2020
(This article belongs to the Special Issue Mineral and Geochemical Composition of Lake Sediments)
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Abstract

:
Geothermal systems can provide significant amounts of hydrothermal sulfur to surface waters, increasing salinity and avoiding some of the common anthropic uses. The objective of this study was to investigate the sedimentary neoformation of S-bearing phases in organic matter-rich sediments from a saline lake with hydrothermal inputs (Sochagota Lake, Colombia). Detrital kaolinite and quartz are the main minerals of the materials deposited in the Sochagota Lake. Neoformed clay minerals (illite and illite-dioctahedral vermiculite mixed layers) are concentrated in the central and northern part of the lake in sediments with high organic matter content. The most organic matter-rich materials are characterized by S-bearing minerals: mackinawite, pyrite, and elemental sulfur (S°). FESEM, high-resolution transmission electron microscopy (HRTEM), EDS, and Raman microspectrometry have revealed the presence of cell-shape aggregates of mackinawite nanoparticles filling the inner part of plant fragments, indicating that microorganisms were involved in the hydrothermal sulfur uptake. The alteration of mackinawite in free sulfide excess environment produced the formation of framboidal pyrite. The evolution to conditions with the presence of oxygen favored the formation of complex S° morphologies.

1. Introduction

The presence of sulfur as an important component is widely extended in many hydrothermal systems controlling the geochemistry and distribution of most of the trace elements in geothermal systems [1,2]. In geothermal systems, the presence of alkaline hot springs is very frequently found as surface waters, representing the composition of the geothermal reservoir [3]. The boiling of the reservoir can produce fluids enriched in volatile gases such as CO2 and H2S, which proportion can change depending on the degree of boiling (H2S content increases with increasing of boiling). H2S hydrothermal fluids mix with non-thermal surface waters producing SO42−-rich waters due to the oxidation of the hydrothermal H2S [1,4]. Spring discharges of SO42−-rich fluids may alter the surface waters, producing important environmental effects in downstream waters, e.g., increasing salinity and avoiding some of the anthropic uses of the waters. The presence of natural or constructed lakes that accumulate this type of waters generates hydrologically restricted environments. Under tropical conditions, strong eutrophication [5,6] favors the deposit of organic matter-rich materials where the interaction with saline fluids and organic activity catalyze mineral reactions in the sediments [7]. Microbial redox reactions involving S compounds can control some mineral authigenic sedimentary processes in these environments [8,9,10]. These reactions are commonly influenced by the formation of sulfide minerals. Rickard and Luther [11] exhaustively reviewed the chemistry of iron sulfides. The Fe monosulfide resulting from the precipitation of Fe2+ and S2− is mackinawite (see, e.g., [12]). It precipitates as unstable tetragonal particles that transform to ordered crystals. Mackinawite is transformed through different pathways, according to O2 and H2S concentrations, to greigite (Fe3S4), pyrite (FeS2), elemental sulfur (S°), and ferric oxides and hydroxides. H2S concentrations in sedimentary environments under low-temperature conditions are associated with the activity of the sulfate-reducing microorganisms [13]. Some studies (e.g., [14]) indicated that mackinawite and greigite are infrequently conserved in the sedimentary rocks, but its formation can be controlled by microorganisms and they possibly have a critical reactive function in the current biogeochemical cycles of Fe and S. Among sulfide minerals, pyrite is characterized by its high stability and abundance [13]. Recent research [15] has indicated the importance of the sulfur biogeochemical cycle of native sulfur (S°), which is produced by oxidation reactions (chemical or biological) of other S-bearing phases with lower oxidation state.
This study aims to investigate the sedimentary neoformation of S-bearing phases in organic matter-rich sediments from a saline lake with hydrothermal inputs. High-resolution microscopy techniques, such as field emission scanning electron microscopy (FESEM), high-resolution transmission electron microscopy (HRTEM)), coupled to high spectral resolution techniques, such as energy dispersive X-ray spectrometry (EDX) and Raman spectroscopy, were used in a fine-scale characterization to reveal the processes involved in the sedimentary uptake and transformation of the hydrothermal S.

2. Materials and Methods

2.1. Study Site

The Sochagota Lake is located in the Paipa province (Boyacá department, Colombia) (Figure 1a,b). This lake has, mainly, a recreational use. The surface area of the lake is 1.8 km2 and the deepest point is 3.20 m. It is an artificial lake on a previous natural wetland forming a small endorheic basin in the lower course of the Salitre River (Paipa), a tributary of the Chicamocha River.
The average annual temperature in Paipa is 14.4 °C. The average rainfall is 911 mm/year, with this precipitation well distributed throughout the year. The climate is subtropical highland (altitude, 2496 m) oceanic (classified as Cfb by the Köppen system).
From the geological perspective, the Sochagota Lake is situated in the main geothermal area of the Andean Cordillera in the Colombian territory, with hydrothermal systems located mainly around the volcanoes of the Andean Cordillera in the Colombian territory. These volcanoes predominantly intrude cretaceous siliceous sedimentary rocks (conglomerates, sandstones, shales, and claystones) (Figure 2). The presence of evaporitic rocks or other types of salt-bearing rocks has not been described in the stratigraphic column of the area. To the south of the small endorheic basin of the Sochagota Lake outcrop the materials of one of these volcanoes, the Paipa volcano [16], which is an eroded explosive volcanic building formed by acid pyroclastic deposits (alkaline rhyolites and trachyandesites) of Pliocene-Pleistocene age. This structure includes a collapsed caldera of 3 km diameter that has several hydrothermal vents. The presence of these materials may be related to the heat source of the intense geothermal system in the area as well as to the presence of S-bearing materials. A high-temperature geothermal system related to a magmatic heat source has been proposed for the area [17]. The heat upflow is controlled by deep faults and a shallow mixing process producing a highly mineralized sodium-sulfate water that hides the chemical composition of the deep reservoir fluid.
The Sochagota Lake stores natural hydrothermal saline waters [18] mixed with rain surface waters. Table 1 shows that lake waters have high electrical conductivity (2440 µS/cm) and pH (9.27). These waters are enriched in SO42− (2165 mg/L), Na+ (1493 mg/L), and K+ (280 mg/L). The isotopic composition of the water samples is characterized by mean values of 6.4‰ for δ34S and 8.1 for δ18O [19]. The isotope contents (see, e.g., [20,21]) and the absence of evaporitic deposits in the geological context strongly suggest the hydrothermal origin of the S responsible for the high salinity of the lake.
The sediments were sampled from 20 points in a grid covering the entire area of the lake (Figure 1c). A standard stainless Shelby tube was used for sampling, and cores up to 50 cm deep were obtained. Coring polypropylene tubes with samples were capped at top and bottom with silicone rubber preserved in frozen tubes with dry ice at −80 °C, included in closed polyethylene bags that were transported to the laboratory until further processing. The extracted cores were divided into two sections: (a) 0–25 cm depth segment (samples ending with –s in Table 2) and (b) 25–50 cm segment (samples ending with –p in Table 2).

2.2. Methods

We prepared oriented aggregates (whole sample and <2 µm fraction) to obtain X-ray diffraction (XRD) data. Samples were previously washed with ultrapure water to remove salts [22]. Oriented aggregates were obtained by sedimentation in a glass. Centrifugation was used to separate the <2 µm fraction. Ethylene glycol and heating treatments at 400 °C and 550 °C were carried out to identify expandable clay minerals.
The diffractograms were obtained in a PANalytical X’Pert Pro diffractometer (CuKα radiation, 45 kV, 40 mA), equipped with an X’Celerator solid-state linear detector, which was used to obtain the diffraction patterns (0.008° 2θ step increment and 10 s/step of counting time) (CICT, University of Jaén, Jaén, Spain). A scan between 3° and 62° 2θ was carried on the air-dried samples, while for the treated samples, the scan was done between 2° and 30° 2θ to help with the identification of clay minerals [22].
We used polished sections to obtain back-scattered electrons (BSE) images and tridimensional sediment fragments to acquire secondary electron (SE) images in a field emission scanning electron microscope (FESEM, Merlin Carl Zeiss of the CICT of the University of Jaén, Jaén, Spain). Polished samples used for BSE images were previously impregnated under vacuum with a polyester resin [23]. BSE images were acquired at 15 kV with a working distance of 8 mm using an AsB detector, whereas SE images were acquired at 15 kV using conventional and in-lens detectors, according to Reference [24]. These images provided the information for a textural and microchemical characterization.
The nanometric characterization was carried out by high-resolution transmission electron microscopy (HRTEM) following the experimental procedure indicated by Nieto and collaborators [25] in two electron microscopes at the CIC of the University of Granada (FEI TITAN and the Philips CM20) (Granada, Spain). Au and Cu grids were used to prepare samples from alcohol or distilled water of sample particles dispersion.
A FESEM with a Raman spectrometer (CIC, University of Granada, Granada, Spain) was used for the Raman spectrometry following the experimental procedure indicated by Guerra and Cardell [26] (Zeiss Supra 40Vp FESEM with a Renishaw spectrometer In Via fitted with a Nd:YAG 532 nm laser and a near-infrared diode 785 nm laser, maximum powers of 500 mW and 100 mW, respectively, coupled to a Peltier-cooled CCD detector and single-grating monochromators, 1200 and 1800 lines mm−1).
Total organic carbon (TOC) was measured after preparing five replicate samples for every core segment using high-temperature (720 °C) catalytic oxidation (Pt-alumina) on a Shimadzu TOC-V CSH Total Organic Carbon Analyzer [27] from the IRNAS at CSIC-Sevilla (Sevilla, Spain). Sediment samples were precisely weighed (2–3 mg ± 0.01 mg) on silver capsules. Analytical replication of reference material (PACS-2) was run every 10 samples. The limit of quantification was calculated as 0.03%. Standard deviation for every core segment is indicated in Table 1.

3. Results

The materials accumulated in the Sochagota Lake are microlaminated sediments. There are important differences between the materials sampled in the south part of the lake and those from the central and north areas.
Samples from the south part are light-colored and compact. XRD analyses reveal the presence of high amounts of kaolinite, quartz, and feldspars (Figure 3a). Scanning electron microscope images show that quartz and feldspar appear as large sub-idiomorphic crystals sized from 100 to 800 μm (Figure 4a). Feldspar crystals are characterized by the presence of very altered surfaces (Figure 4b). Acid volcanic glass particles very rich in microvesicles, whose size varies between 2 and 10 μm, can also be observed.
On the other hand, sediments from the central and north areas are very fine grain sized. X-ray diffraction analysis shows that these materials are frequently enriched in clay minerals (Figure 3b), of which mineral assemblage is made of illite, illite-dioctahedral vermiculite mixed layers, and kaolinite (Figure 5a) [28]. FESEM images show that the clay-rich matrix of the sediments is often crossed by elongated plant rests, diameter of which can reach up to 50 μm (Figure 5b).
Sulfur-bearing minerals are especially concentrated in materials rich in organic matter from the central and north areas. Figure 6 and Figure 7 show FESEM and HRTEM micrographs, as well as EDX and micro-Raman spectra of sulfur-containing minerals from the Sochagota Lake sediments.
Pyrite is the most abundant S-bearing mineral in the organic matter-rich materials. Microcrystals and pyrite spherules of around 500 nm appear between the micropores of the sediment (Figure 6a). EDX microanalyses of these grains show a Fe:S ratio close to 2. The aggregation of pyrite crystals produces less than 10 μm sized framboids (Figure 6b–d). Accumulations of framboidal pyrite is especially important in areas rich in organic matter remains (Figure 6e). Near these pyrite-rich zones appear individual grains of elemental S of around 10 µm in size (Figure 6f) and S-aggregates formed by microfilaments and micro-spherules that generate a vesicular texture (Figure 6g). Raman spectra of these regions (Figure 6h) allow the identification of pyrite, with peaks at 344 and 379 cm−1 [29] and elemental S with peaks at 152 and 220 cm−1 [30]. Weak mackinawite peaks (208, 260, and 298 cm−1) were also observed [31].
In contrast, other Fe2+ sulfides were detected in the inner part of some cores enriched in organic matter (Figure 7). EDX analyses indicates that its Fe-S atomic ratio is close to 1 for some of these minerals filling plant fragments, which corresponds to the mackinawite composition FeS (Figure 7a,b).
Detailed high magnification images of the inner part of the plant fragments revealed the presence of clusters of fine FeS nanoparticles (around 80 nm) forming aggregates, which shape and size (1–2 µm) is similar to the bacterial cell morphology (Figure 7c–e). HRTEM images also show scattered extracellular nanoparticles (Figure 7f). EDX microanalyses of nanoparticles from the HRTEM study also shows the same Fe:S ratio. Raman spectra of the FeS minerals filling plant rests confirmed the presence of mackinawite with an important peak at 298 cm−1, a secondary one at 208 cm−1, and a very weak peak at 260 cm−1 (Figure 7g) [31]. Greigite was not identified in any samples.
Regarding the organic matter content, TOC in the sediments oscillated from 0.28% to 11.1% (Table 2). The lowest concentrations were located in materials rich in kaolinite, quartz, and feldspars formed in the south part of the lake, near the El Salitre hydrothermal input, and where plant vegetation is scarce. The highest concentrations of total organic carbon were found in the materials rich in 2:1 phyllosilicates (illite-dioctahedral vermiculite mixed layers (I-DV) and illite) at the central and northern part of the lake, frequently close vegetation rich zones. These fine sized sediments have the highest contents of sulfide minerals.

4. Discussion

The relationship between detrital materials, hydrothermal input, high organic matter content, and S-containing mineral precipitation occurring in the Sochagota lake was evaluated in this study.

4.1. Detrital Minerals and Neoformed Clay Minerals

The results of this study revealed that the materials formed at the Sochagota Lake exhibited significant differences in the grain size, mineral assemblage, and organic matter content according to the distance from the entrance of the hydrothermal inputs (El Salitre). From the entrance to the inner portion and the northern border of the lake, the amount of fine particles of clay minerals (illite and mixed-layer clay mineral) increases. The formation of illite and I-DV was occurred during the strong interaction of the sediments with the saline water-pore under the reduced conditions provided by the high content in organic matter [32]. Similar illitization processes in other saline and organic matter-rich environments, such as those occurring in mangroves, have been described [7]. On the other hand, the higher hydrodynamic conditions of the lake entrance and the low organic matter content of these materials avoided the formation and accumulation of the fine clay mineral particles in the southern area of the Sochagota Lake [32].

4.2. Hydrothermal Inputs and Reduced Microenvironments Favored by Organic Matter

Isotopic composition of the waters from the Sochagota Lake (mean values of 6.4‰ for δ34S and 8.1 for δ18O) is inside the reference fields indicated in several studies [20,21] for active hydrothermal systems. These data and the absence of evaporitic deposit or any other type of sulfate-bearing rocks in the geological context [16] clearly indicate that sulfur dissolved in the water and precipitated in the materials of the lake is of hydrothermal origin.
S-bearing minerals are concentrated at the organic matter-rich materials from the deeper central and northern part of the lake. Organic matter-rich layers are able to maintain oxygen depleted conditions due to the capability of decaying organic matter to provide electrons for reactions of reduction. In saline environments, such as that of the Sochagota Lake, following the availability of easily degradable organic matter, microorganisms most likely can create microenvironments with reduced Fe and aqueous sulfides in which some processes lead to the precipitation of insoluble sulfides (see, e.g., [33]).

4.3. The S Cycle in the Materials of the Sochagota Lake

Figure 4, Figure 5, Figure 6 and Figure 7 suggest that the presence of S-bearing minerals is not associated to the sediment depth. The main factor controlling the formation of these minerals was the amount of organic matter, which is heterogeneously distributed among both depths (Table 2). Pyrite is the more extended S-bearing mineral from these organic matter-rich materials. This indicates that the uptake of Fe is associated with the existence of S-bearing phases in the materials with finest particles and close to vegetation-rich areas, suggesting the association of a pyritization process to the organic matter abundance. Crystallization of individual pyrite crystals and framboidal aggregates associated with organic matter have been extensively described in anoxic sediments (e.g., [34,35]). For example, nanobacterial cells are frequently found coating pyrite microcrystals associated with decaying organic matter [35]. Pyrite framboids can be formed within templates provided by organic carbon matrix [36]. Experimental studies and field observations suggest that pyrite framboids formation is promoted by the nucleation and growth of iron monosulfides, which are later converted to pyrite (e.g., [37,38,39]). According to Hu and collaborators, most of the organic matter-rich materials are thought to undergo three processes that contribute to the crystallization of pyrite in framboids [40]: (a) formation and development of precursors (FeS); (b) transformation of FeS to FeS2; and (c) pyrite growth.
In the materials investigated in this study, high spatial and spectral resolution spectromicroscopy techniques allow to identify textural traces of microorganisms’ activity associated with the first stage of the framboidal sulfides formation. High-resolution electron microscopy studies are one of the best tools to determine the presence of sulfide nanoparticles, its volume, morphology, composition, and disposition in organic matter-rich environment, allowing to elucidate the importance of the factors controlling its formation, such as the microbial-mineral interactions or the changes in aqueous and sediment chemistry (see, e.g., [14,41,42]). Figure 7c–e shows the remarkable morphological and dimensional features of spherical and oval-shaped FeS nanoparticle aggregates in the organic matter-rich sediments of the Sochagota Lake materials, suggesting bacterially induced precipitation of FeS. Raman microspectrometry confirmed the accumulation of these mackinawite particles at the inner part of plant fragments.
Therefore, the FESEM, HRTEM, and Raman microspectrometry data from this study reveal that sulfate-reducing bacteria cells facilitated decisively the uptake of Fe particles from the Sochagota Lake materials through the formation of mackinawite FeS nanoparticles. The experimental study of Picard and collaborators [14] has confirmed the ability of microbial cells to uptake metals (Fe) that concentrate in crusts on the surface of microorganisms as sulfide minerals, suggesting that the cell membrane of sulfate-reducing microorganisms and their extracellular materials can act as templates for the formation and growth of sulfide minerals. Kraal and collaborators [12] suggested that rapid burial under anoxic conditions prevent dissolution of FeS in organic-rich reducing sediments.
Pyrite and S° were likely produced by the alteration of mackinawite produced by a free sulfide excess that generate iron monosulfide dissolution and a later pyrite recrystallization [11,43]. The conversion of monosulfides to pyrite can also be influenced by sulfate-reducing bacteria activity, supplying H2S, or organic sulfur able to accept electrons, which facilitate the formation of FeS2 [44,45,46].
The transformation of sulfide to S° by inorganic oxidation reaction is very slowly produced, which suggest that oxidation by microorganisms is the prevalent process for S° crystallization in low-temperature environments [47]. However, Cosmidis and Templeton [48] discovered that H2S can interact with organic matter under an oxygenated environment to form inorganic S°, producing filamentous and complex morphologies similar to those observed in the Lago Sochagota materials.

5. Conclusions

We have investigated the sedimentary neoformation of S-bearing phases in organic matter-rich sediments from the Sochagota Lake (Colombia), a saline lake in tropical latitude with hydrothermal inputs. The sedimentary processes occurring under saline and reduced conditions carried out the fixation of the hydrothermal sulfur enriched in the water lake.
Most of the materials deposited in the Sochagota Lake are made of detrital quartz and kaolinite. Sediments from the central and northern part of the lake are enriched in neoformed clay minerals (illite and I-DV) by saline transformations due to the interaction with the waters of the lake and high content in organic matter. The isotopic composition of these waters suggest that the sulfur dissolved in these waters is of hydrothermal origin. The hydrothermal input was responsible for the salinity of the waters.
The cycle of sulfur in the lake is related to a pyritization process associated with the abundance of organic matter. The first step of the process was evidenced by FESEM, HRTEM, EDS, and Raman microspectrometry, which revealed the presence of mackinawite particles (sometimes forming cell-shape aggregates) at the inner part of plant fragments of some organic matter-rich cores. The crystallization of mackinawite strongly support that hydrothermal SO42− dissolved in the waters of the Sochagota Lake underwent sulfate reduction processes associated with the decay of the organic matter to form S-bearing minerals in the sediments. Microorganisms favored the formation and growth of mackinawite and its transformation to pyrite and S°. Pyrite was formed by mackinawite alteration in an environment with excess of free sulfide. Filamentous and complex morphologies of S° were formed inorganically by H2S and organic matter reaction in an oxygen-richer environment.

Author Contributions

C.P.Q. and G.R.C. conducted field observations and sampling. J.J.-M., R.J.-E., C.P.Q., and G.R.C. performed microscopic observations SEM and TEM (mineralogical, textural, chemical analyses, and Raman spectrometry) and interpreted the X-ray diffractograms and TOC. All authors discussed the analytical results and prepared the manuscript. All authors have read and agreed to the published version of the manuscript.

Funding

This work has been financed by the Spanish research project PGC2018-094573-B-I00 from the MCIU-AEI-FEDER and research group RNM-325 of the Junta de Andalucía (Spain). Our gratitude is also extended to Asociación Universitaria Iberoamericana de Posgrado (AUIP) and the Universidad de Boyacá. We would also like to thank Colombian Research groups Gestión Ambiental COL0005468 and Gestión de Recursos Hídricos COL0005477.

Acknowledgments

We would like to acknowledge to two anonymous reviewers for their suggestions and comments that helped to improve the manuscript.

Conflicts of Interest

The authors declare no conflict of interest. The funders had no role in the design of the study; in the collection, analyses, or interpretation of data; in the writing of the manuscript; or in the decision to publish the results.

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Figure 1. Geographical setting of the study area and sampling location. (a) Global context of the area; (b) Local situation in Colombia; (c) Location of the sampling points 1 to 20 at the Sochagota Lake.
Figure 1. Geographical setting of the study area and sampling location. (a) Global context of the area; (b) Local situation in Colombia; (c) Location of the sampling points 1 to 20 at the Sochagota Lake.
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Figure 2. Geological map of the Sochagota Lake Basin. The lake does not receive sediments from the north area. Modified from Reference [16].
Figure 2. Geological map of the Sochagota Lake Basin. The lake does not receive sediments from the north area. Modified from Reference [16].
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Figure 3. XRD diagrams of air-dried oriented aggregates from samples of the Sochagota Lake. (a) Representative sample from the south part of the lake (segment 0–25 cm depth). (b) Representative sample from the central and north areas (segment 25–50 cm depth). Kln: kaolinite, I-DV: illite-dioctahedral vermiculite mixed layers, Ilt: illite, Qz: quartz. Red: air-dried (AD) pattern; blue: 400 °C heated pattern; green: 550 °C heated pattern.
Figure 3. XRD diagrams of air-dried oriented aggregates from samples of the Sochagota Lake. (a) Representative sample from the south part of the lake (segment 0–25 cm depth). (b) Representative sample from the central and north areas (segment 25–50 cm depth). Kln: kaolinite, I-DV: illite-dioctahedral vermiculite mixed layers, Ilt: illite, Qz: quartz. Red: air-dried (AD) pattern; blue: 400 °C heated pattern; green: 550 °C heated pattern.
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Figure 4. FESEM images of samples from the south part of the lake. (a) back-scattered electrons (BSE) image of crystals of quartz in a kaolinite-rich matrix (sample from segment 25–50 cm depth); (b) SE image of feldspar crystal with altered surface (sample from segment 0–25 cm depth). Kln: kaolinite, Qz: quartz, Fsp: feldspar.
Figure 4. FESEM images of samples from the south part of the lake. (a) back-scattered electrons (BSE) image of crystals of quartz in a kaolinite-rich matrix (sample from segment 25–50 cm depth); (b) SE image of feldspar crystal with altered surface (sample from segment 0–25 cm depth). Kln: kaolinite, Qz: quartz, Fsp: feldspar.
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Figure 5. FESEM images of samples from the north part of the lake. (a) HRTEM image showing the mineral assemblage made of illite, illite-dioctahedral vermiculite mixed layers, and kaolinite (sample from segment 0–25 cm depth); (b) FESEM-SE image showing the clay-rich matrix of the sediments crossed by elongated plant rests (sample from segment 25–50 cm depth). Kln: kaolinite, Ilt: illite, I-DV: illite-dioctahedral vermiculite mixed layers, OM: organic matter.
Figure 5. FESEM images of samples from the north part of the lake. (a) HRTEM image showing the mineral assemblage made of illite, illite-dioctahedral vermiculite mixed layers, and kaolinite (sample from segment 0–25 cm depth); (b) FESEM-SE image showing the clay-rich matrix of the sediments crossed by elongated plant rests (sample from segment 25–50 cm depth). Kln: kaolinite, Ilt: illite, I-DV: illite-dioctahedral vermiculite mixed layers, OM: organic matter.
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Figure 6. Electron microscope image and spectroscopy data (EDS and Raman) of pyrite and S° in the organic matter-rich materials of the lake (samples from segments 0-(samples from segments 25–50 cm depth, except for a) 25 cm depth, except for a). (a) SE image of microcrystals of pyrite between the micropores of the sediment; (b), (c) and (d) SE images of pyrite framboids; (e) BSE image of an accumulation of framboidal pyrite near organic matter rests; (f) SE image of an individual grain of native sulfur near pyrite-rich zones; (g) BSE image of a S-aggregate formed by microfilaments that generate a vesicular texture; (h) Raman spectrum of pyrite-rich region. Py: pyrite, OM: organic matter, S: elemental sulfur, M: mackinawite.
Figure 6. Electron microscope image and spectroscopy data (EDS and Raman) of pyrite and S° in the organic matter-rich materials of the lake (samples from segments 0-(samples from segments 25–50 cm depth, except for a) 25 cm depth, except for a). (a) SE image of microcrystals of pyrite between the micropores of the sediment; (b), (c) and (d) SE images of pyrite framboids; (e) BSE image of an accumulation of framboidal pyrite near organic matter rests; (f) SE image of an individual grain of native sulfur near pyrite-rich zones; (g) BSE image of a S-aggregate formed by microfilaments that generate a vesicular texture; (h) Raman spectrum of pyrite-rich region. Py: pyrite, OM: organic matter, S: elemental sulfur, M: mackinawite.
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Figure 7. Electron microscope image and spectroscopy data (EDS and Raman) of mackinawite in the organic matter-rich materials of the lake (samples from segments 25–50 cm depth, except for a). (a) and (b) FeS filling plant fragments in a SE image (a) and in a BSE image (b); EDX analysis indicates that its Fe-S atomic ratio is close to 1; (c), (d) and (e) Detailed high magnification SE images of the inner part of the plant fragments revealing FeS nanoparticles aggregates with bacterial cell morphology; (f) HRTEM image showing scattered FeS nanoparticles; (g) Raman spectrum of the FeS minerals filling plant rests confirming the presence of mackinawite. M: mackinawite.
Figure 7. Electron microscope image and spectroscopy data (EDS and Raman) of mackinawite in the organic matter-rich materials of the lake (samples from segments 25–50 cm depth, except for a). (a) and (b) FeS filling plant fragments in a SE image (a) and in a BSE image (b); EDX analysis indicates that its Fe-S atomic ratio is close to 1; (c), (d) and (e) Detailed high magnification SE images of the inner part of the plant fragments revealing FeS nanoparticles aggregates with bacterial cell morphology; (f) HRTEM image showing scattered FeS nanoparticles; (g) Raman spectrum of the FeS minerals filling plant rests confirming the presence of mackinawite. M: mackinawite.
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Table
Table 1. Average physical-chemical parameters of the Sochagota Lake waters from Reference [19].
Table 1. Average physical-chemical parameters of the Sochagota Lake waters from Reference [19].
Physical-Chemical Parameters and UnitsAverage Values
Cl¯ (mg/L)672.3
SO2¯4 (mg/L)2165.0
HCO¯3 (mg/L)204.2
CO2¯3 (mg/L)1.5
NO¯3 (mg/L)314.9
Na+ (mg/L)1493.1
Mg2+ (mg/L)9.1
Ca2+ (mg/L)55.5
K+ (mg/L)280.7
pH9.27
E.C. (µS/cm)2440.0
Temperature (°C)22.0
E.C. Electrical conductivity.
Table
Table 2. Content in inorganic carbon (IC), total organic carbon (TOC), and total carbon from the materials deposited in the Sochagota Lake. *: 0–25 cm core segment; **: 25–50 cm core segment; ***: 0–50 cm core segment. Standard deviation is indicated in parenthesis.
Table 2. Content in inorganic carbon (IC), total organic carbon (TOC), and total carbon from the materials deposited in the Sochagota Lake. *: 0–25 cm core segment; **: 25–50 cm core segment; ***: 0–50 cm core segment. Standard deviation is indicated in parenthesis.
SampleIC (%)TOC (%)Total C (%)
1p **0.149 (0.01)9.15 (0.04)9.30
1s *0.142 (0.01)4.11 (0.02)4.25
2p **0.269 (0.03)1.01 (0.01)1.28
2s *0.176 (0.01)1.17 (0.01)1.34
3p **0.290 (0.02)1.88 (0.02)2.17
3s *0.188 (0.01)1.74 (0.01)1.93
4p **0.161 (0.01)0.996 (0.01)1.16
4s *0.090 (0.01)2.01 (0.01)2.10
5p **0.131 (0.01)3.04 (0.03)3.18
5s *0.121 (0.01)2.51 (0.03)2.63
6p **0.123 (0.02)11.1 (0.01)11.20
6s *0.142 (0.01)3.59 (0.04)3.73
M7 ***<0.1001.16 (0.01)1.24
7p **0.253 (0.01)1.41 (0.01)1.66
7s *0.229 (0.01)1.21 (0.01)1.43
M8 ***<0.10 (0.01)1.25 (0.03)1.33
8p **0.181 (0.01)2.12 (0.01)2.30
8s *0.264 (0.01)2.26 (0.01)2.52
M9 ***<0.1002.10 (0.01)2.11
9p **1.26 (0.03)0.66 (0.01)1.93
9s *0.683 (0.02)0.62 (0.01)1.31
10p **0.199 (0.01)3.64 (0.04)3.84
10s *0.194 (0.01)3.18 (0.02)3.38
11p **0.195 (0.01)1.52 (0.01)1.72
11s *0.200 (0.01)1.57 (0.01)1.77
12p **0.206 (0.01)1.24 (0.01)1.45
12s *0.141 (0.01)1.80 (0.01)1.94
13p **0.216 (0.01)1.27 (0.01)1.48
13s *0.957 (0.01)0.37 (0.01)1.33
M14 ***<0.100.96 (0.01)0.96
14p **0.218 (0.01)3.45 (0.04)3.67
14s *0.149 (0.01)2.24 (0.01)2.38
15p **0.218 (0.01)1.73 (0.01)1.94
15s *0.188 (0.01)1.59 (0.01)1.78
16p **0.408 (0.01)0.48 (0.01)0.89
17p **0.156 (0.01)0.64 (0.01)0.80
17s *0.309 (0.01)0.31 (0.01)0.62
18p **0.212 (0.01)4.35 (0.05)4.56
18s *1.180 (0.02)0.29 (0.01)1.48
19p **0.257 (0.01)1.64 (0.02)1.89
19s *0.137 (0.01)1.78 (0.01)1.89
M20 ***<0.1000.69 (0.01)0.70
20p **0.158 (0.01)1.79 (0.02)1.95
20s *0.189 (0.01)2.59 (0.03)2.78

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Cifuentes, G.R.; Jiménez-Millán, J.; Quevedo, C.P.; Jiménez-Espinosa, R. Transformation of S-Bearing Minerals in Organic Matter-Rich Sediments from a Saline Lake with Hydrothermal Inputs. Minerals 2020, 10, 525. https://0-doi-org.brum.beds.ac.uk/10.3390/min10060525

AMA Style

Cifuentes GR, Jiménez-Millán J, Quevedo CP, Jiménez-Espinosa R. Transformation of S-Bearing Minerals in Organic Matter-Rich Sediments from a Saline Lake with Hydrothermal Inputs. Minerals. 2020; 10(6):525. https://0-doi-org.brum.beds.ac.uk/10.3390/min10060525

Chicago/Turabian Style

Cifuentes, Gabriel Ricardo, Juan Jiménez-Millán, Claudia Patricia Quevedo, and Rosario Jiménez-Espinosa. 2020. "Transformation of S-Bearing Minerals in Organic Matter-Rich Sediments from a Saline Lake with Hydrothermal Inputs" Minerals 10, no. 6: 525. https://0-doi-org.brum.beds.ac.uk/10.3390/min10060525

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