The selectivity of a sequential extraction procedure for the determination of iron oxyhydroxides andiron sulfides in lake sediments

A popular sequential extraction procedure (Tessier et al. 1979) designed t o extract metals partitioned in various sediment phases, was evaluated for its selectivity. Amorphous FeOOH, FeS, and FeS₂ were added separately to natural lake sediments and sequentially extracted. The selectivity of the sequential procedure for the added solid phases was evaluated by determining the difference in the mass of Fe extracted from treated and control sediments. In the experiments where sulfide minerals were added, total S was measured in the residual solids in order to confirm selectivity of the method. Concentrations of total carbon remaining in the solid phase after each extraction step were also measured to determine the selectivity of the sequential procedure for carbon. The procedure was moderately selective for Fe added as FeOOH; a mean of 77 ± 12% (p < 0.05) of the Fe added was extracted in the step designed to reduce Fe-Mn oxyhydroxides. In experiments where FeS was added, a mean of 69 ± 11% (p < 0.05) of the Fe added as FeS was extracted in the fraction designed to oxidize sulfides and organic matter. Approximately 25% of the Fe added as FeS may have been extracted prematurely. Although less precise, total S analyses confirmed that much of the FeS was extracted in the oxidation step, yielding 104 ± 87% (p < 0.05) of the S added as FeS. The procedure was highly selective for FeS₂; 92 ± 14% (p < 0.05) of the Fe added as pyrite was extracted in the sulfide extraction step. Extraction of 80 ± 54% (p < 0.05) of S added as pyrite confirmed that FeS₂ were selectively extracted in the sulfide extraction step. Carbon in the sediments was also selectively extracted in the oxidation step (77 ± 2.4% of total C; p < 0.05). The applications and limitations of sequential extraction procedures as limnological research tools are discussed in light of our results. Request for offprints     

Reductive dechlorination of trichloroethylene by combining autotrophic hydrogen-bacteria and zero-valent iron particles

The objective of this study was to evaluate the dechlorination rate (from an initial concentration of 180 micromol l(-1)) and synergistic effect of combining commercial Fe(0) and autotrophic hydrogen-bacteria in the presence of hydrogen, during TCE degradation process. In the batch test, the treatment using Fe(0) in the presence of hydrogen (Fe(0)/H(2)), showed more effective dechlorination and less iron consumption than Fe(0) utilized only (Fe(0)/N(2)), meaning that catalytic degradation had promoted transformation of TCE, and the iron was protected by cathodic hydrogen. The combined use of Fe(0) and autotrophic hydrogen-bacteria was found to be more effective than did the individual exercise even though the hydrogen was insufficient during the batch test. By the analysis of XRPD, the crystal of FeS transformed by sulfate reducing bacteria (SRB) was detected on the surface of iron after the combined treatment. The synergistic impact was caused by FeS precipitates, which enhanced TCE degradation through catalytic dechlorination. Additionally, the dechlorination rate coefficient of the combined method in MFSB was 3.2-fold higher than that of iron particles individual use. Results from batch and MFSB experiments revealed that, the proposed combined method has the potential to become a cost-effective remediation technology for chlorinated-solvent contaminated site.     

Utilization of iron sulfides for wastewater treatment: a critical review

Acid mine drainage due to weathering of iron sulfide minerals is one of the biggest global environmental issues. However, due to the unique physicochemical properties of natural and synthesized iron sulfides (i.e. pyrite, pyrrhotite, and mackinawite), they can be effectively used for wastewater treatment. These properties, such as ≡SH functional groups as Lewis bases, reducibility of surface Fe and S species, dissolved Fe²⁺ as a catalyst, and dissolved S^2? as an electron donor, are extensively reviewed in this article. The target water pollutants include toxic metals (i.e. lead, mercury, cadmium, and hexavalent chromium) and metalloid (i.e. arsenic), radionuclides (i.e. uranium and selenium), organic contaminants (i.e. chlorinated organic pollutants, benzene and polycyclic aromatic hydrocarbons), and nutrients (i.e. nitrogen and phosphorus). The dominant interaction mechanisms between iron sulfides and these contaminants, and the removal efficiencies are elucidated. This article focuses on the role of iron sulfides as functional materials for wastewater treatment. A recent development of nanostructured pyrrhotite with a high specific surface area for wastewater treatment is also highlighted.     

Mechanism of Bacterial Pyrite Oxidation

The oxidation by Ferrobacillus ferrooxidans of untreated pyrite (FeS(2)) as well as HCl-pretreated pyrite (from which most of the acid-soluble iron species were removed) was studied manometrically. Oxygen uptake was linear during bacterial oxidation of untreated pyrite, whereas with HCl-pretreated pyrite both a decrease in oxygen uptake at 2 hr and nonlinear oxygen consumption were observed. Ferric sulfate added to HCl-pretreated pyrite restored approximately two-thirds of the decrease in total bacterial oxygen uptake and caused oxygen uptake to revert to nearly linear kinetics. Ferric sulfate also oxidized pyrite in the absence of bacteria and O(2); recovery of ferric and ferrous ions was in excellent agreement with the reaction Fe(2)(SO(4))(3) + FeS(2) = 3FeSO(4) + 2S, but the elemental sulfur produced was negligible. Neither H(2)S nor S(2)O(3) (2-) was a product of the reaction. It is probable that two mechanisms of bacterial pyrite oxidation operate concurrently: the direct contact mechanism which requires physical contact between bacteria and pyrite particles for biological pyrite oxidation, and the indirect contact mechanism according to which the bacteria oxidize ferrous ions to the ferric state, thereby regenerating the ferric ions required for chemical oxidation of pyrite.     

Plasmid profiles of Acidithiobacillus ferrooxidans strains adapted to different oxidation substrates

Plasmid profiles were studied in five Acidithiobacillus ferrooxidans strains of various origin cultivated on medium with Fe2+, as well as adapted to such oxidation substrates as S0, FeS2, and sulfide concentrate. The method used revealed plasmids in all A. ferrooxidans strains grown on medium with Fe2+. One plasmid was found in strain TFL-2, two plasmids, in strains TFO, TFBk, and TFV-1, and three plasmids were detected in strain TFN-d. The adaptation of strain TFN-d to sulfide concentrate and the adaptation of strain TFV-1 to S0, FeS2, or sulfide concentrate resulted in a change in the number of plasmids occurring in cells. In cells of strain TFN-d adapted to sulfide concentrate, the number of plasmids decreased from three to two. The number of plasmids in cells of strain TFV-1 adapted to different substrates varied from three to six depending on the energy source present in the medium: three plasmids were found after growth on FeS2, four after growth on S0, and six after growth on sulfide concentrate. The possible role of plasmids in the adaptation of A. ferrooxidans to new energy substrates and in the regulation of the intensity of their oxidation is discussed.     

O2 reactions at the six-iron active site (H-cluster) in [FeFe]-hydrogenase

Irreversible inhibition by molecular oxygen (O(2)) complicates the use of [FeFe]-hydrogenases (HydA) for biotechnological hydrogen (H(2)) production. Modification by O(2) of the active site six-iron complex denoted as the H-cluster ([4Fe4S]-2Fe(H)) of HydA1 from the green alga Chlamydomonas reinhardtii was characterized by x-ray absorption spectroscopy at the iron K-edge. In a time-resolved approach, HydA1 protein samples were prepared after increasing O(2) exposure periods at 0 °C. A kinetic analysis of changes in their x-ray absorption near edge structure and extended X-ray absorption fine structure spectra revealed three phases of O(2) reactions. The first phase (τ(1) ≤ 4 s) is characterized by the formation of an increased number of Fe-O,C bonds, elongation of the Fe-Fe distance in the binuclear unit (2Fe(H)), and oxidation of one iron ion. The second phase (τ(2) ≈ 15 s) causes a ～50% decrease of the number of ～2.7-? Fe-Fe distances in the [4Fe4S] subcluster and the oxidation of one more iron ion. The final phase (τ(3) ≤ 1000 s) leads to the disappearance of most Fe-Fe and Fe-S interactions and further iron oxidation. These results favor a reaction sequence, which involves 1) oxygenation at 2Fe(H(+)) leading to the formation of a reactive oxygen species-like superoxide (O(2)(-)), followed by 2) H-cluster inactivation and destabilization due to ROS attack on the [4Fe4S] cluster to convert it into an apparent [3Fe4S](+) unit, leading to 3) complete O(2)-induced degradation of the remainders of the H-cluster. This mechanism suggests that blocking of ROS diffusion paths and/or altering the redox potential of the [4Fe4S] cubane by genetic engineering may yield improved O(2) tolerance in [FeFe]-hydrogenase.     

Ferrihydrite-dependent growth of Sulfurospirillum deleyianum through electron transfer via sulfur cycling

Observations in enrichment cultures of ferric iron-reducing bacteria indicated that ferrihydrite was reduced to ferrous iron minerals via sulfur cycling with sulfide as the reductant. Ferric iron reduction via sulfur cycling was investigated in more detail with Sulfurospirillum deleyianum, which can utilize sulfur or thiosulfate as an electron acceptor. In the presence of cysteine (0.5 or 2 mM) as the sole sulfur source, no (microbial) reduction of ferrihydrite or ferric citrate was observed, indicating that S. deleyianum is unable to use ferric iron as an immediate electron acceptor. However, with thiosulfate at a low concentration (0.05 mM), growth with ferrihydrite (6 mM) was possible and sulfur was cycled up to 60 times. Also, spatially distant ferrihydrite in agar cultures was reduced via diffusible sulfur species. Due to the low concentrations of thiosulfate, S. deleyianum produced only small amounts of sulfide. Obviously, sulfide delivered electrons to ferrihydrite with no or only little precipitation of black iron sulfides. Ferrous iron and oxidized sulfur species were produced instead, and the latter served again as the electron acceptor. These oxidized sulfur species have not yet been identified. However, sulfate and sulfite cannot be major products of ferrihydrite-dependent sulfide oxidation, since neither compound can serve as an electron acceptor for S. deleyianum. Instead, sulfur (elemental S or polysulfides) and/or thiosulfate as oxidized products could complete a sulfur cycle-mediated reduction of ferrihydrite.     

Ferrihydrite-Dependent Growth of Sulfurospirillum deleyianum through Electron Transfer via Sulfur Cycling

Observations in enrichment cultures of ferric iron-reducing bacteria indicated that ferrihydrite was reduced to ferrous iron minerals via sulfur cycling with sulfide as the reductant. Ferric iron reduction via sulfur cycling was investigated in more detail with Sulfurospirillum deleyianum, which can utilize sulfur or thiosulfate as an electron acceptor. In the presence of cysteine (0.5 or 2 mM) as the sole sulfur source, no (microbial) reduction of ferrihydrite or ferric citrate was observed, indicating that S. deleyianum is unable to use ferric iron as an immediate electron acceptor. However, with thiosulfate at a low concentration (0.05 mM), growth with ferrihydrite (6 mM) was possible and sulfur was cycled up to 60 times. Also, spatially distant ferrihydrite in agar cultures was reduced via diffusible sulfur species. Due to the low concentrations of thiosulfate, S. deleyianum produced only small amounts of sulfide. Obviously, sulfide delivered electrons to ferrihydrite with no or only little precipitation of black iron sulfides. Ferrous iron and oxidized sulfur species were produced instead, and the latter served again as the electron acceptor. These oxidized sulfur species have not yet been identified. However, sulfate and sulfite cannot be major products of ferrihydrite-dependent sulfide oxidation, since neither compound can serve as an electron acceptor for S. deleyianum. Instead, sulfur (elemental S or polysulfides) and/or thiosulfate as oxidized products could complete a sulfur cycle-mediated reduction of ferrihydrite.     

Geochemistry of iron in the Salton Sea,California

The Salton Sea is a large, saline, closed-basin lake in southern California. The Sea receives agricultural runoff and, to a lesser extent, municipal wastewater that is high in nutrients, salt, and suspended solids. High sulfate concentrations (4× higher than that of the ocean), coupled with warm temperatures and low-redox potentials present during much of the year, result in extensive sulfate reduction and hydrogen sulfide production. Hydrogen sulfide formation may have a dramatic effect on the iron (Fe) geochemistry in the Sea. We hypothesized that the Fe(II)-sulfide minerals should dominate the iron mineralogy of the sediments, and plans to increase hypolimnetic aeration would increase the amount of Fe(III)-oxides, which are strong adsorbers of phosphate. Sequential chemical extractions were used to differentiate iron mineralogy in the lake sediments and suspended solids from the tributary rivers. Iron in the river-borne suspended solids was mainly associated with structural iron within silicate clays (70%) and ferric oxides (30%). The iron in the bottom sediments of the lake was associated with silicate minerals (71% of the total iron in the sediments), framboidal pyrite (10%), greigite (11%), and amorphous FeS (5%). The ferric oxide fraction was <4% of the total iron in these anaerobic sediments. The morphological characteristics of the framboidal pyrite as determined using SEM suggest that it formed within the water column and experiences some changes in local redox conditions, probably associated with alternating summer anoxia and the well-mixed and generally well-aerated conditions found during the winter. The prevalence of Fe(II)-sulfide minerals in the sediments and the lack of Fe(III)-oxide minerals suggest that the classic model of P-retention by Fe(III)-oxides would not be operating in this lake, at least during anoxic summer conditions. Aeration of the hypolimnion could affect the internal loading of P by changing the relative amounts of Fe(II)-sulfides and Fe(III)-oxides at the sediment/water interface. Electronic supplementary material The online version of this article (doi:) contains supplementary material, which is available to authorized users. Guest editor: S. H. Hurlbert The Salton Sea Centennial Symposium. Proceedings of a Symposium Celebrating a Century of Symbiosis Among Agriculture, Wildlife and People, 1905–2005, held in San Diego, California, USA, March 2005     

Microbial Precipitation of Arsenic Sulfides in Andean Salt Flats

An abiotic origin has traditionally been assumed for the arsenic minerals realgar and orpiment associated with thermal springs. Microbial precipitation of arsenic, however, has been studied in pure cultures and the isotopic composition of arsenic sulfides associated with some borate deposits suggests a biotic origin for those minerals. The aim of the present study is to demonstrate the role of bacterial arsenic precipitation in the biogeochemical cycle of arsenic in such borate deposits. For this purpose both enrichment and pure cultures were obtained from the natural arsenic minerals and the composition and isotopic signatures of the arsenic sulfide minerals precipitated by the cultures and those associated with boron deposits from an Andean salt flat in northern Chile were compared. Based on the microbiological and chemical evidence gathered, it is concluded that bacteria contributed to the formation of the arsenic minerals. This interpretation is based on the consistent association of a variety of features that strongly indicate microbial involvement in the precipitation process. These include: (1) enrichment and isolation of cultures with arsenic precipitation capacity from arsenic mineral samples, (2) high numbers of arsenic-precipitating bacteria in the Andean minerals and brines, (3) chemical and mineralogical properties of precipitates experimentally formed under biotic and abiotic conditions, (4) similarities in stoichiometry between natural and laboratory obtained minerals, and (5) the consistent depletion in δ³⁴S values for natural versus laboratory obtained sulfides. Thus, microbial precipitation of arsenic sulfides is a geochemically relevant metabolism.     

Resonance Raman studies indicate a unique heme active site in prostaglandin H synthase

Prostaglandin H synthase isoforms 1 and 2 (PGHS-1 and -2) catalyze the first two steps in the biosynthesis of prostaglandins. Resonance Raman spectroscopy was used to characterize the PGHS heme active site and its immediate environment. Ferric PGHS-1 has a predominant six-coordinate high-spin heme at room temperature, with water as the sixth ligand. The proximal histidine ligand (or the distal water ligand) of this hexacoordinate high-spin heme species was reversibly photolabile, leading to a pentacoordinate high-spin ferric heme iron. Ferrous PGHS-1 has a single species of five-coordinate high-spin heme, as evident from nu(2) at 1558 cm(-1) and nu(3) at 1471 cm(-1). nu(4) at 1359 cm(-1) indicates that histidine is the proximal ligand. A weak band at 226-228 cm(-1) was tentatively assigned as the Fe-His stretching vibration. Cyanoferric PGHS-1 exhibited a nu(Fe)(-)(CN) line at 446 cm(-1) and delta(Fe)(-)(C)(-)(N) at 410 cm(-1), indicating a "linear" Fe-C-N binding conformation with the proximal histidine. This linkage agrees well with the open distal heme pocket in PGHS-1. The ferrous PGHS-1 CO complex exhibited three important marker lines: nu(Fe)(-)(CO) (531 cm(-1)), delta(Fe)(-)(C)(-)(O) (567 cm(-1)), and nu(C)(-)(O) (1954 cm(-1)). No hydrogen bonding was detected for the heme-bound CO in PGHS-1. These frequencies markedly deviated from the nu(Fe)(-)(CO)/nu(C)(-)(O) correlation curve for heme proteins and porphyrins with a proximal histidine or imidazolate, suggesting an extremely weak bond between the heme iron and the proximal histidine in PGHS-1. At alkaline pH, PGHS-1 is converted to a second CO binding conformation (nu(Fe)(-)(CO): 496 cm(-1)) where disruption of the hydrogen bonding interactions to the proximal histidine may occur.     

Bacterial oxidation of ferrous iron at low temperatures

This study comprises the first report of ferrous iron oxidation by psychrotolerant, acidophilic iron-oxidizing bacteria capable of growing at 5 degrees C. Samples of mine drainage-impacted surface soils and sediments from the Norilsk mining region (Taimyr, Siberia) and Kristineberg (Skellefte district, Sweden) were inoculated into acidic ferrous sulfate media and incubated at 5 degrees C. Iron oxidation was preceded by an approximately 3-month lag period that was reduced in subsequent cultures. Three enrichment cultures were chosen for further work and one culture designated as isolate SS3 was purified by colony isolation from a Norilsk enrichment culture for determining the kinetics of iron oxidation. The 16S rRNA based phylogeny of SS3 and two other psychrotolerant cultures, SS5 from Norilsk and SK5 from Northern Sweden, was determined. Comparative analysis of amplified 16S rRNA gene sequences showed that the psychrotolerant cultures aligned within Acidithiobacillus ferrooxidans. The rate constant of iron oxidation by growing cultures of SS3 was in the range of 0.0162-0.0104 h(-1) depending on the initial pH. The oxidation kinetics followed an exponential pattern, consistent with a first order rate expression. Parallel iron oxidation by a mesophilic reference culture of Acidithiobacillus ferrooxidans was extremely slow and linear. Precipitates harvested from the 5 degrees C culture were identified by X-ray diffraction as mixtures of schwertmannite (ideal formula Fe(8)O(8)(OH)(6)SO(4)) and jarosite (KFe(3)(SO(4))(2)(OH)(6)). Jarosite was much more dominant in precipitates produced at 30 degrees C.     

Facilitated transfer of IscU-[2Fe2S] clusters by chaperone-mediated ligand exchange

The scaffold protein IscU and molecular chaperones HscA and HscB play central roles in biological assembly of iron-sulfur clusters and maturation of iron-sulfur proteins. However, the structure of IscU-FeS complexes and the molecular mechanism whereby the chaperones facilitate cluster transfer to acceptor proteins are not well understood. We have prepared amino acid substitution mutants of Escherichia coli IscU in which potential ligands to the FeS cluster (Cys-37, Cys-63, His-105, and Cys-106) were individually replaced with alanine. The properties of the IscU-FeS complexes formed were investigated by measuring both their ability to transfer preformed FeS clusters to apo-ferredoxin and the activity of the IscU proteins in catalyzing cluster assembly on apo-ferredoxin using inorganic iron with inorganic sulfide or with IscS and cysteine as a sulfur source. The ability of the HscA/HscB chaperone system to accelerate ATP-dependent cluster transfer from each IscU substitution mutant to apo-ferredoxin was also determined. All of the mutants formed FeS complexes with a stoichiometry similar to the wild-type holo-protein, i.e., IscU(2)[2Fe2S], raising the possibility that different cluster ligation states may occur during iron-sulfur protein maturation. Spectroscopic properties of the mutants and the kinetics of transfer of performed IscU-FeS clusters to apo-ferredoxin indicate that the most stable form of holo-IscU involves iron coordination by Cys-63 and Cys-106. Results of studies on the ability of mutants to catalyze formation of holo-ferredoxin using iron and different sulfur sources were consistent with proposed roles for Cys-63 and Cys-106 in FeS cluster binding and also indicated an essential role for Cys-106 in sulfide transfer to IscU from IscS. Measurements of the ability of the chaperones HscA and HscB to facilitate cluster transfer from holo-IscU to apo-ferredoxin showed that only IscU(H105A) behaved similarly to wild-type IscU in exhibiting ATP-dependent stimulation of cluster transfer. IscU(C63A) and IscU(C106A) displayed elevated rates of cluster transfer in the ±ATP whereas IscU(C37A) exhibited low rates of cluster transfer ±ATP. In interpreting these findings, we propose that IscU(2)[2Fe2S] is able undergo structural isomerization to yield conformers having different cysteine residues bound to the cluster. On the basis of the crystal structure of HscA complexed with an IscU-derived peptide, we propose that the chaperone binds and stabilizes an isomer of IscU(2)[2Fe2S] in which the cluster is bound by cysteine residues 37 and 63 and that the [2Fe2S] cluster, being held less tightly than that coordinated by Cys-63 and Cys-106 in free IscU(2)[2Fe2S], is more readily transferred to acceptor proteins such as apo-ferredoxin.     

Growth of iron(III)-reducing bacteria on clay minerals as the sole electron acceptor and comparison of growth yields on a variety of oxidized iron forms

Smectite clay minerals are abundant in soils and sediments worldwide and are typically rich in Fe. While recent investigations have shown that the structural Fe(III) bound in clay minerals is reduced by microorganisms, previous studies have not tested growth with clay minerals as the sole electron acceptor. Here we have demonstrated that a pure culture of Shewanella oneidensis strain MR-1 as well as enrichment cultures of Fe(III)-reducing bacteria from rice paddy soil and subsurface sediments are capable of conserving energy for growth with the structural Fe(III) bound in smectite clay as the sole electron acceptor. Pure cultures of S. oneidensis were used for more detailed growth rate and yield experiments on various solid- and soluble-phase electron acceptors [smectite, Fe(III) oxyhydroxide FeOOH, Fe(III) citrate, and oxygen] in the same minimal medium. Growth was assessed as direct cell counts or as an increase in cell carbon (measured as particulate organic carbon). Cell counts showed that similar growth of S. oneidensis (10(8) cells ml(-1)) occurred with smectitic Fe(III) and on other Fe forms [amorphous Fe(III) oxyhydroxide, and Fe citrate] or oxygen as the electron acceptor. In contrast, cell yields of S. oneidensis measured as the increase in cell carbon were similar on all Fe forms tested while yields on oxygen were five times higher, in agreement with thermodynamic predictions. Over a range of particle loadings (0.5 to 4 g liter(-1)), the increase in cell number was highly correlated to the amount of structural Fe in smectite reduced. From phylogenetic analysis of the complete 16S rRNA gene sequences, a predominance of clones retrieved from the clay mineral-reducing enrichment cultures were most closely related to the low-G+C gram-positive members of the Bacteria (Clostridium and Desulfitobacterium) and the delta-Proteobacteria (members of the Geobacteraceae). Results indicate that growth with smectitic Fe(III) is similar in magnitude to that with Fe(III) oxide minerals and is dependent upon the mineral surface area available. Iron(III) bound in clay minerals should be considered an important electron acceptor supporting the growth of bacteria in soils or sedimentary environments.     

Dynamics of Rhodobacter capsulatus [2FE-2S] ferredoxin VI and Aquifex aeolicus ferredoxin 5 via nuclear resonance vibrational spectroscopy (NRVS) and resonance Raman spectroscopy

We have used (57)Fe nuclear resonance vibrational spectroscopy (NRVS) to study the Fe(2)S(2)(Cys)(4) sites in oxidized and reduced [2Fe-2S] ferredoxins from Rhodobacter capsulatus (Rc FdVI) and Aquifex aeolicus (Aa Fd5). In the oxidized forms, nearly identical NRVS patterns are observed, with strong bands from Fe-S stretching modes peaking around 335 cm(-1), and additional features observed as high as the B(2u) mode at approximately 421 cm(-1). Both forms of Rc FdVI have also been investigated by resonance Raman (RR) spectroscopy. There is good correspondence between NRVS and Raman frequencies, but because of different selection rules, intensities vary dramatically between the two kinds of spectra. For example, the B(3u) mode at approximately 288 cm(-1), attributed to an asymmetric combination of the two FeS(4) breathing modes, is often the strongest resonance Raman feature. In contrast, it is nearly invisible in the NRVS, as there is almost no Fe motion in such FeS(4) breathing. NRVS and RR analysis of isotope shifts with (36)S-substituted into bridging S(2-) ions in Rc FdVI allowed quantitation of S(2-) motion in different normal modes. We observed the symmetric Fe-Fe stretching mode at approximately 190 cm(-1) in both NRVS and RR spectra. At still lower energies, the NRVS presents a complex envelope of bending, torsion, and protein modes, with a maximum at 78 cm(-1). The (57)Fe partial vibrational densities of states (PVDOS) were interpreted by normal-mode analysis with optimization of Urey-Bradley force fields. Progressively more complex D(2h) Fe(2)S(2)S'(4), C(2h) Fe(2)S(2)(SCC)(4), and C(1) Fe(2)S(2)(Cys)(4) models were optimized by comparison with the experimental spectra. After modification of the CHARMM22 all-atom force field by the addition of refined Fe-S force constants, a simulation employing the complete protein structure was used to reproduce the PVDOS, with better results in the low frequency protein mode region. This process was then repeated for analysis of data on the reduced FdVI. Finally, the degree of collectivity was used to quantitate the delocalization of the dynamic properties of the redox-active Fe site. The NRVS technique demonstrates great promise for the observation and quantitative interpretation of the dynamical properties of Fe-S proteins.     

Polymersomes Containing Iron Sulfide (FeS) as Primordial Cell Model

According to Wächtershäuser??s ??Iron-Sulfur-World?? one major requirement for the development of life on the prebiotic Earth is compartmentalization. Vesicles spontaneously formed from amphiphilic components containing a specific set of molecules including sulfide minerals may have lead to the first autotrophic prebiotic units. The iron sulfide minerals may have been formed by geological conversions in the environment of deep-sea volcanos (black smokers), which can be observed even today. Wächtershäuser postulated the evolution of chemical pathways as fundamentals of the origin of life on earth. In contrast to the classical Miller-Urey experiment, depending on external energy sources, the ??Iron-Sulfur-World?? is based on the catalytic and energy reproducing redox system $ FeS + {H_2}S \to FeS{}_2 + {H_2} $ . The energy release out of this redox reaction (?_RG°?=??38 kJ/mol, pH 0) could be the cause for the subsequent synthesis of complex organic molecules and the precondition for the development of more complex units similar to cells known today. Here we show the possibility for precipitating iron sulfide inside vesicles composed of amphiphilic block-copolymers as a model system for a first prebiotic unit. Our findings could be an indication for a chemoautotrophic FeS based origin of life.     

The effects of manipulation of sedimentary iron and organic matter on sediment biogeochemistry and seagrasses in a subtropical carbonate environment

The microbial metabolism of organic matter (OM) in seagrass beds can create sulfidic conditions detrimental to seagrass growth; iron (Fe) potentially has ameliorating effects through titration of the sulfides and the precipitation of iron-sulfide minerals into the sediment. In this study, the biogeochemical effects of Fe availability and its interplay with sulfur and OM on sulfide toxicity, phosphorous (P) availability, seagrass growth and community structure were tested. The availability of Fe and OM was manipulated in a 2 × 2 factorial experiment arranged in a Latin square, with four replicates per treatment. The treatments included the addition of Fe, the addition of OM, the addition of both Fe and OM as well as no addition. The experiment was conducted in an oligotrophic, iron-deficient seagrass bed. Fe had an 84.5% retention efficiency in the sediments with the concentration of Fe increasing in the seagrass leaves over the course of the experiment. Porewater chemistry was significantly altered with a dramatic decrease in sulfide levels in Fe addition plots while sulfide levels increased in the OM addition treatments. Phosphorus increased in seagrass leaves collected in the Fe addition plots. Decreased sulfide stress was evidenced by heavier δ³⁴S in leaves and rhizomes from plots to which Fe was added. The OM addition negatively affected seagrass growth but increased P availability; the reduced sulfide stress in Fe added plots resulted in elevated productivity. Fe availability may be an important determinant of the impact that OM has on seagrass vitality in carbonate sediments vegetated with seagrasses.     

Chemical and biological interactions during nitrate and goethite reduction by Shewanella putrefaciens 200

Although previous research has demonstrated that NO(3)(-) inhibits microbial Fe(III) reduction in laboratory cultures and natural sediments, the mechanisms of this inhibition have not been fully studied in an environmentally relevant medium that utilizes solid-phase, iron oxide minerals as a Fe(III) source. To study the dynamics of Fe and NO(3)(-) biogeochemistry when ferric (hydr)oxides are used as the Fe(III) source, Shewanella putrefaciens 200 was incubated under anoxic conditions in a low-ionic-strength, artificial groundwater medium with various amounts of NO(3)(-) and synthetic, high-surface-area goethite. Results showed that the presence of NO(3)(-) inhibited microbial goethite reduction more severely than it inhibited microbial reduction of the aqueous or microcrystalline sources of Fe(III) used in other studies. More interestingly, the presence of goethite also resulted in a twofold decrease in the rate of NO(3)(-) reduction, a 10-fold decrease in the rate of NO(2)(-) reduction, and a 20-fold increase in the amounts of N(2)O produced. Nitrogen stable isotope experiments that utilized delta(15)N values of N(2)O to distinguish between chemical and biological reduction of NO(2)(-) revealed that the N(2)O produced during NO(2)(-) or NO(3)(-) reduction in the presence of goethite was primarily of abiotic origin. These results indicate that concomitant microbial Fe(III) and NO(3)(-) reduction produces NO(2)(-) and Fe(II), which then abiotically react to reduce NO(2)(-) to N(2)O with the subsequent oxidation of Fe(II) to Fe(III).     

A new look at microbial leaching patterns on sulfide minerals

Leaching patterns on sulfide minerals were investigated by high-resolution scanning electron microscopy (SEM). Our goal was to evaluate the relative contributions of inorganic surface reactions and reactions localized by attached cells to surface morphology evolution. Experiments utilized pyrite (FeS(2)), marcasite (FeS(2)) and arsenopyrite (FeAsS), and two iron-oxidizing prokaryotes in order to determine the importance of cell type, crystal structure, and mineral dissolution rate in microbially induced pit formation. Pyrite surfaces were reacted with the iron-oxidizing bacterium Acidithiobacillus ferrooxidans (at 25 degrees C), the iron-oxidizing archaeon 'Ferroplasma acidarmanus' (at 37 degrees C), and abiotically in the presence of Fe(3+) ions. In all three experiments, discrete bacillus-sized (1-2 μm) and -shaped (elliptical) pits developed on pyrite surfaces within 1 week of reaction. Results show that attaching cells are not necessary for pit formation on pyrite. Marcasite and arsenopyrite surfaces were reacted with A. ferrooxidans (at 25 degrees C) and 'F. acidarmanus' (at 37 degrees C). Cell-sized and cell-shaped dissolution pits were not observed on marcasite or arsenopyrite at any point during reaction with A. ferrooxidans, or on marcasite surfaces reacted with 'F. acidarmanus'. However, individual 'F. acidarmanus' cells were found within individual shallow (<0.5 μm deep) pits. The size and shape (round rather than elliptical) of the pits conformed closely to the shape of F. acidarmanus (cells) pits on arsenopyrite. We infer these pits to be cell-induced. We attribute the formation of pits readily detectable (by SEM) to the higher reactivity of arsenopyrite compared to pyrite and marcasite under the conditions the experiment was conducted. These pits contributed little to the overall surface topographical evolution, and most likely did not significantly increase surface area during reaction. Our results suggest that overall sulfide mineral dissolution may be dominated by surface reactions with Fe(3+) rather than by reactions at the cell-mineral interface.