Advances in the biotechnology of hydrogen production with the microalga Chlamydomonas reinhardtii

Biological hydrogen production is being evaluated for use as a fuel, since it is a promising substitute for carbonaceous fuels owing to its high conversion efficiency and high specific energy content. The basic advantages of biological hydrogen production over other “green” energy sources are that it does not compete for agricultural land use, and it does not pollute, as water is the only by-product of the combustion. These characteristics make hydrogen a suitable fuel for the future. Among several biotechnological approaches, photobiological hydrogen production carried out by green microalgae has been intensively investigated in recent years. A select group of photosynthetic organisms has evolved the ability to harness light energy to drive hydrogen gas production from water. Of these, the microalga Chlamydomonas reinhardtii is considered one of the most promising eukaryotic H₂ producers. In this model microorganism, light energy, H₂O and H₂ are linked by two excellent catalysts, the photosystem 2 (PSII) and the [FeFe]-hydrogenase, in a pathway usually referred to as direct biophotolysis. This review summarizes the main advances made over the past decade as an outcome of the discovery of the sulfur-deprivation process. Both the scientific and technical barriers that need to be overcome before H₂ photoproduction can be scaled up to an industrial level are examined. Actual and theoretical limits of the efficiency of the process are also discussed. Particular emphasis is placed on algal biohydrogen production outdoors, and guidelines for an optimal photobioreactor design are suggested.     

Mars Primordial Crust: Unique Sites for Investigating Proto-biologic Properties

The Martian meteorite collection suggests that intact outcrops or boulder-scale fragments of the 4.5 Ga Martian crust exist within tens of meters of the present day surface of Mars. Mars may be the only planet where such primordial crust samples, representing the first 100 Ma of a planet’s environment, are available. The primordial crust has been destroyed on Earth by plate tectonics and other geological phenomena and is buried on the Moon under hundreds or thousands of meters of megaregoltih. Early Mars appears to have been remarkably similar to early Earth, and samples of rock from the first few Ma or first 100 Ma may reveal “missing link” proto-biological forms that could shed light on the transition from abiotic organic chemistry to living cells. Such organic snapshots of nascent life are unlikely to be found on Earth. Presented at: National Workshop on Astrobiology: Search for Life in the Solar System, Capri, Italy, 26 to 28 October, 2005.     

What's up down there?

The development of careful quality assurance criteria assuring freedom from contamination in all aspects of sample recovery has opened the window to studies of a fascinating new microbial biome in the deep subsurface. Organisms have been recovered with unusual metabolic capabilities and a chemosynthetic lifestyle independent of the recent surface photosynthetically derived energy inputs. The properties of the subsurface microbiota are critical when assessing aspects such as the utility of burying radioactive waste, the remediation of mixtures of organics, metals, and nuclides, and the search for life in extreme environments on Earth as well as on Mars and other extraterrestrial sites. In addition this pioneering work provides a foundation for examining life processes in extreme environments, such as the environment beneath the ocean floor.     

Microbial diversity of deep-sea extremophiles--Piezophiles, Hyperthermophiles, and subsurface microorganisms]

Knowledge of our Planet's biosphere has increased tremendously during the last 10 to 20 years. In the field of Microbiology in particular, scientists have discovered novel "extremophiles", microorganisms capable of living in extreme environments such as highly acidic or alkaline conditions, at high salt concentration, with no oxygen, extreme temperatures (as low as -20 degrees C and as high as 300 degrees C), at high concentrations of heavy metals and in high pressure environments such as the deep-sea. It is apparent that microorganisms can exist in any extreme environment of the Earth, yet already scientists have started to look for life on other planets; the so-called "Exobiology" project. But as yet we have little knowledge of the deep-sea and subsurface biosphere of our own planet. We believe that we should elucidate the Biodiversity of Earth more thoroughly before exploring life on other planets, and these attempts would provide deeper insight into clarifying the existence of extraterrestrial life. We focused on two deep-sea extremophiles in this article; one is "Piezophiles", and another is "Hyperthermophiles". Piezophiles are typical microorganisms adapted to high-pressure and cold temperature environments, and located in deep-sea bottom. Otherwise, hyperthermophiles are living in high temperature environment, and located at around the hydrothermal vent systems in deep-sea. They are not typical deep-sea microorganisms, but they can grow well at high-pressure condition, just like piezophiles. Deming and Baross mentioned that most of the hyperthermophilic archaea isolated from deep-sea hydrothermal vents are able to grow under conditions of high temperature and pressure, and in most cases their optimal pressure for growth was greater than the environmental pressure they were isolated from. It is possible that originally their native environment may have been deeper than the sea floor and that there had to be a deeper biosphere. This implication suggests that the deep-sea hydrothermal vents are the windows to a deep subsurface biosphere. A vast array of chemoautotrophic deep-sea animal communities have been found to exist in cold seep environments, and most of these animals are common with those found in hydrothermal vent environments. Thus, it is possible to consider that the cold seeps are also one of slit windows to a deep subsurface biosphere. We conclude that the deep-sea extremophiles are very closely related into the unseen majority in subsurface biosphere, and the subsurface biosphere probably concerns to consider the "exobiology".     

Possible origin of a membrane in the subsurface of the Earth

A location for the origin of life on Earth could have been an oil/water interface in the warm, subsurface environment of the Earth. The physico-chemical conditions of the subsurface would include elevated, but eventually cooling temperatures, anaerobic conditions, and protection from intense surface radiation. This type of subsurface oil/water environment may have been ideal for the assembly of the first simple membrane(s), where no enzyme catalysis was needed. Once a stable, simple, continuous closed membrane was formed, one central component of the first cell(s) would have been present; a semi-permeable open system that allowed the passage of both matter and energy in and out of the cell. Such an open system could also acquire novel functions, whereas a closed system would be unable to evolve.     

Crucial crises in biology: life in the deep biosphere.

The origin and evolution of life on Earth are the result of a series of crises that have taken place on the planet over about 4500 millions of years since it originated. Biopoiesis (origin of life), ecopoiesis (origin of ecosystems) and the first ecosystems (stromatolites and microbial mats), as well as eukaryopoiesis (origin of nucleated cells) are revised. The paper then focuses on the study of the deep biosphere, describing ecosystems never found before, which are independent of solar radiation and have changed previous assumptions about the requirements of life; even the concept of biosphere, as Vernadsky defined it, has increased its scope. Since the discovery, in 1987, of bacteria growing in the crevices of rocks at 500 m deep, in boreholes drilled near the Savanna River, Aiken, South Carolina, other bacteria have been found in the deep subsurface reaching depths of about 3 km (e.g., in the Columbia River Basalt Group, near Richland, Washington state), in an anaerobic, hot, high-pressure environment. Some kinds of microorganisms can thrive at such depths, living in many cases a geochemical existence, by using very specialized metabolisms, which depend on the local environments. The existence of organisms independent from photosynthetic production is the most outstanding, novel feature of the deep biosphere. Living beings might not need other energy and chemical sources than those which occur in the development of all planetary bodies. Life, therefore, could even be an ineluctable outcome of planetary evolution and, as a corollary, a natural continuation of the usual development of physical phenomena in the universe.     

The first living systems: a bioenergetic perspective.

The first systems of molecules having the properties of the living state presumably self-assembled from a mixture of organic compounds available on the prebiotic Earth. To carry out the polymer synthesis characteristic of all forms of life, such systems would require one or more sources of energy to activate monomers to be incorporated into polymers. Possible sources of energy for this process include heat, light energy, chemical energy, and ionic potentials across membranes. These energy sources are explored here, with a particular focus on mechanisms by which self-assembled molecular aggregates could capture the energy and use it to form chemical bonds in polymers. Based on available evidence, a reasonable conjecture is that membranous vesicles were present on the prebiotic Earth and that systems of replicating and catalytic macromolecules could become encapsulated in the vesicles. In the laboratory, this can be modeled by encapsulated polymerases prepared as liposomes. By an appropriate choice of lipids, the permeability properties of the liposomes can be adjusted so that ionic substrates permeate at a sufficient rate to provide a source of monomers for the enzymes, with the result that nucleic acids accumulate in the vesicles. Despite this progress, there is still no clear mechanism by which the free energy of light, ion gradients, or redox potential can be coupled to polymer bond formation in a protocellular structure.     

Geochemical constraints on chemolithoautotrophic reactions in hydrothermal systems

Thermodynamic calculations provide the means to quantify the chemical disequilibrium inherent in the mixing of redeuced hydrothermal fluids with seawater. The chemical energy available for metabolic processes in these environments can be evaluated by taking into account the pressure and temperature dependence of the apparent standard Gibbs free energies of reactions in the S-H₂-H₂O system together with geochemical constraints on pH, activities of aqueous sulfur species and fugacities of H₂ and/or O₂. Using present-day mixing of hydrothermal fluids and seawater as a starting point, it is shown that each mole of H₂S entering seawater from hydrothermal fluids represents about 200,000 calories of chemical energy for metabolic systems able to catalyze H₂S oxidation. Extrapolating to the early Earth, which was likely to have had an atmosphere more reduced than at present, shows that this chemical energy may have been a factor of two or so less. Nevertheless, mixing of hydrothermal fluids with seawater would have been an abundant source of chemical energy, and an inevitable consequence of the presence of an ocean on an initially hot Earth. The amount of energy available was more than enough for organic synthesis from CO₂ or CO, and/or polymer formation, indicating that the vicinity of hydrothermal systems at the sea floor was an ideal location for the emergence of the first chemolithoautotrophic metabolic systems.     

Biological energy requirements as quantitative boundary conditions for life in the subsurface

All life requires energy, which must be extracted from the environment. For all known life, free energy must be available at finite minimum levels in order to be usefully harnessed and must be delivered at finite minimum rates in order to support basic biochemical integrity and function. While seldom tested in the high energy light‐ and oxygen‐based metabolisms of the surface biosphere, the magnitude of these requirements – the biological energy quantum (BEQ) and maintenance energy (ME) requirements, respectively – is considerable with respect to the potential metabolisms and energy sources that characterize the deep subsurface realm. As such, they constitute a fundamental constraint on the possible nature, distribution, and activity of microbial life in that environment. Because the energy released in a chemical transformation can be equated to the concentrations of substrates and products, both the BEQ and ME requirements define the minimum substrate concentration and minimum substrate production rate that must be sustained by a given environment for it to be capable of supporting life. The magnitudes of the BEQ and ME requirements are sensitive to a range of environmental parameters that may vary significantly in the subsurface. Temperature exerts a particularly strong control and is among the most important parameters to be considered in evaluating the energetic habitability of subsurface environments.     

Hydrogen-driven subsurface lithoautotrophic microbial ecosystems (SLiMEs): do they exist and why should we care?

One of the keys to success of many anaerobic ecosystems is the process of syntrophic intercellular hydrogen transfer. This process facilitates the overall reaction by end-product removal, taking advantage of a wide variety of organisms that are able to use hydrogen directly as an energy source by uptake hydrogenases. Thus, the issue is not whether there are hydrogen-driven processes or communities but whether there are hydrogen-driven communities that exist and persist independently of the products of photosynthesis (so-called subsurface lithoautotrophic microbial ecosystems, or SLiMEs). It is the proof of long-term independence from photosynthesis and its products that is the most difficult issue to establish, and perhaps the most important one with regard to searching for SLiMEs both on and off our planet. Although the evidence is not yet unequivocal, a growing body of evidence supports the existence of SLiME-like communities: if they exist, the implications are immense with regard to understanding subsurface environments on Earth, looking for present day analogs of early Earth and the search for life in other worlds.     

Reduction and Activation of Phosphate on the Primitive Earth

Electrical discharges in water-saturated N₂ containing 1–10% CH₄ were shown earlier toreduce phosphate to phosphite. This mechanism was suggestedas a possible source of water-soluble phosphorus-containing compounds in volcanic environments on the prebiotic Earth.We have now extended our investigations to gas mixtures inwhich CO₂ and N₂ are the main components, and studied the effect of introducing smallamounts of H₂ and CO.We show that surprisingly high conversions to phosphite occurin reducing mixtures and thatseveral percent reduction of apatite occurs even in thepresence of as little as 1% each of H₂ and CO. We were also able to confirm a previous report ofpolyphosphate production as a result of heating the mineral apatite in the presence of other minerals.     

Review: microbial mechanisms of accessing insoluble Fe(III) as an energy source

Of all the terminal electron acceptors, Fe(III) is the most naturally abundant in many subsurface environments. Fe(III)-reducing microorganisms are phylogenetically diverse and have been isolated from a variety of sources. Unlike most electron acceptors, Fe(III) has a very low solubility and is usually present as insoluble oxides at neutral pH. The mechanisms by which microorganisms access and reduce insoluble Fe(III) are poorly understood. Initially, it was considered that microorganisms could only reduce insoluble Fe(III) through direct contact with the oxide. However, recent studies indicate that extracellular electron shuttling or Fe(III)-chelating compounds may alleviate the need for cell–oxide contact. These include microbially secreted compounds or exogenous electron shuttling agents, mainly from humic substances. Electron shuttling via humic substances is likely a significant process for Fe(III) reduction in subsurface environments. This paper reviews the various mechanisms by which Fe(III) reduction may be occurring in pure culture and in soils and sediments.     

Nitrogen Dioxide Sterilization in Low-Resource Environments: A Feasibility Study

Access to sterilization is a critical need for global healthcare, as it is one of the prerequisites for safe surgical care. Lack of sterilization capability has driven up healthcare infection rates as well as limited access to healthcare, especially in low-resource environments. Sterilization technology has for the most part been static and none of the established sterilization methods has been so far successfully adapted for use in low-resource environments on a large scale. It is evident that healthcare facilities in low-resource settings require reliable, deployable, durable, affordable, easily operable sterilization equipment that can operate independently of scarce resources. Recently commercialized nitrogen dioxide (NO₂) sterilization technology was analyzed and adapted into a form factor suitable for use in low-resource environments. Lab testing was conducted in microbiological testing facilities simulating low-resource environments and in accordance with the requirements of the international sterilization standard ANSI/AAMI/ISO 14937 to assess effectiveness of the device and process. The feasibility of a portable sterilizer based on nitrogen dioxide has been demonstrated, showing that sterilization of medical instruments can occur in a form factor suitable for use in low-resource environments. If developed and deployed, NO₂ sterilization technology will have the twin benefits of reducing healthcare acquired infections and limiting a major constraint for access to surgical care on a global scale. Additional benefits are achieved in reducing costs and biohazard waste generated by current health care initiatives that rely primarily on disposable kits, increasing the effectiveness and outreach of these initiatives.     

Planetary Organic Chemistry and the Origins of Biomolecules

Organic chemistry on a planetary scale is likely to have transformed carbon dioxide and reduced carbon species delivered to an accreting Earth. According to various models for the origin of life on Earth, biological molecules that jump-started Darwinian evolution arose via this planetary chemistry. The grandest of these models assumes that ribonucleic acid (RNA) arose prebiotically, together with components for compartments that held it and a primitive metabolism that nourished it. Unfortunately, it has been challenging to identify possible prebiotic chemistry that might have created RNA. Organic molecules, given energy, have a well-known propensity to form multiple products, sometimes referred to collectively as “tar” or “tholin.” These mixtures appear to be unsuited to support Darwinian processes, and certainly have never been observed to spontaneously yield a homochiral genetic polymer. To date, proposed solutions to this challenge either involve too much direct human intervention to satisfy many in the community, or generate molecules that are unreactive “dead ends” under standard conditions of temperature and pressure. Carbohydrates, organic species having carbon, hydrogen, and oxygen atoms in a ratio of 1:2:1 and an aldehyde or ketone group, conspicuously embody this challenge. They are components of RNA and their reactivity can support both interesting spontaneous chemistry as part of a “carbohydrate world,” but they also easily form mixtures, polymers and tars. We describe here the latest thoughts on how on this challenge, focusing on how it might be resolved using minerals containing borate, silicate, and molybdate, inter alia.Interesting organic chemistry occurs throughout the cosmos, including in presolar nebulae (see the article in this collection by Pascale Erhrenfreund), asteroidal bodies (see the article in this collection by Sandra Pizzarello) and icy bodies near the outer boundary of our solar system (Bernstein et al. 2002). Although organic molecules made in off-Earth locales almost certainly contributed to the reduced carbon inventory on Earth before life emerged, planetary processing on Earth undoubtedly also contributed to the inventory of prebiotic molecules that were available to life as it originated (assuming that Earth was the site of life''s origin). Indeed, in the RNA first model for the origin of life on Earth (Joyce and Orgel 1999)(Benner 2009), it is often proposed that terran-based chemistry produced RNA in oligomeric form to initiate Darwinian evolution.How are we to constrain models for planetary processing to converge on a model for what actually happened on Earth four billion years ago? Today, atmospheric dioxygen (O₂) readily converts organic materials to carbon dioxide, making it essentially impossible to observe such processing on the surface of Earth. Furthermore, the ubiquity of life on modern Earth means that any organic processing is more likely to reflect biology than prebiology. The closest we may come today to observe organic transformations absent biology on a planetary scale might be on Titan, a moon of Saturn whose atmosphere and surface is rich in reduced carbon.Nevertheless, it is possible to apply a general understanding of organic chemical reactivity to suggest chemical reactions that might have occurred on early Earth and the products that they might have produced. These suggestions are constrained by models for the atmosphere and mineralogy of early Earth, although these constraints might change as models improve.In this article, we assume that the atmosphere of early Earth was less oxidizing than today''s atmosphere, although not as rich in methane as the simulated atmosphere used in the classic experiments of Stanley Miller (Miller 1955). Further, we assume that the atmosphere on early Earth had access to many sources of energy. These include electrical discharge, ultraviolet and visible light (although the Sun was almost certainly dimmer then than now, a Titan-like haze may have prevented high energy photons from reacting the Earth''s surface), volcanism (providing not only heat but also reactive species and mixtures not at thermodynamic equilibrium), ionizing radiation, and impacts. (See Pizzarello and Shock 2010 for a discussion of such energy sources.)We also assume that life emerged after the planet underwent a geological fractionation in which heavier minerals and elemental iron sank towards the core, leaving lighter rocks to form the crust. Open questions concern the inventory of water relative to the surface of early Earth, an inventory that determined whether planetary organic transformations might have occurred on dry land or below water on a planetary surface that was totally submerged.     

Isolation of Thiomonas thermosulfatus Strain 51, a Species Capable of Coupling Biogenic Pyritization with Chemiosmotic Energy Transduction

The precipitation of iron sulfides potentially offers enough energy and reducing power to sustain life but organisms harnessing this reaction have not to our knowledge been previously described. We isolated a bacterial strain, capable of forming the iron sulfide minerals troilite (FeS), greigite (Fe₃S₄), and pyrite (FeS₂), from subsurface, microbial mats in Mangalia, Romania. This strain, most closely related to strains of Thiomonas sp., forms pyrite only if the redox conditions remain negative (< ?60 mV), sulfides are provided continually (≈1 mM), and the concentration of iron remains low (≤ 0.08 mM) but constant. Pyrite formation by this microbial strain is proposed as an example of biologically controlled mineralization because it is controlled by uncouplers of oxidative phosphorylation, it is larger in living than in dead cells, it is additive (controlled less by the amount of cell surfaces and more by reagents), and it results in the formation of ATP. This study indicates that precipitation and crystal formation can represent an energy resource for life and provides support for the “iron-sulfide world hypothesis” regarding the early evolution of life on Earth.     

Critically testing olivine‐hosted putative martian biosignatures in the Yamato 000593 meteorite—Geobiological implications

On rocky planets such as Earth and Mars the serpentinization of olivine in ultramafic crust produces hydrogen that can act as a potential energy source for life. Direct evidence of fluid–rock interaction on Mars comes from iddingsite alteration veins found in martian meteorites. In the Yamato 000593 meteorite, putative biosignatures have been reported from altered olivines in the form of microtextures and associated organic material that have been compared to tubular bioalteration textures found in terrestrial sub‐seafloor volcanic rocks. Here, we use a suite of correlative, high‐sensitivity, in situ chemical, and morphological analyses to characterize and re‐evaluate these microalteration textures in Yamato 000593, a clinopyroxenite from the shallow subsurface of Mars. We show that the altered olivine crystals have angular and micro‐brecciated margins and are also highly strained due to impact‐induced fracturing. The shape of the olivine microalteration textures is in no way comparable to microtunnels of inferred biological origin found in terrestrial volcanic glasses and dunites, and rather we argue that the Yamato 000593 microtextures are abiotic in origin. Vein filling iddingsite extends into the olivine microalteration textures and contains amorphous organic carbon occurring as bands and sub‐spherical concentrations <300 nm across. We propose that a martian impact event produced the micro‐brecciated olivine crystal margins that reacted with subsurface hydrothermal fluids to form iddingsite containing organic carbon derived from abiotic sources. These new data have implications for how we might seek potential biosignatures in ultramafic rocks and impact craters on both Mars and Earth.     

Energy Transduction Inside of Amphiphilic Vesicles: Encapsulation of Photochemically Active Semiconducting Particles

Amphiphilic bilayer membrane structures (vesicles) have been postulated to have been abiotically formed and spontaneously assemble on the prebiotic Earth, providing compartmentalization for the origin of life. These vesicles are similar to modern cellular membranes and can serve to contain water-soluble species, concentrate species, and have the potential to catalyze reactions. The origin of the use of photochemical energy in metabolism (i.e. energy transduction) is one of the central issues in the origin of life. This includes such questions as how energy transduction may have occurred before complex enzymatic systems, such as required by contemporary photosynthesis, had developed and how simple a photochemical system is possible. It has been postulated that vesicle structures developed the ability to capture and transduce light, providing energy for reactions. It has also been shown that pH gradients across the membrane surface can be photochemically created, but coupling these to drive chemical reactions has been difficult. Colloidal semiconducting mineral particles are known to photochemically drive redox chemistry. We propose that encapsulation of these particles has the potential to provide a source of energy transduction inside vesicles, and thereby drive protocellular chemistry, and represents a model system for early photosynthesis. In our experiments we show that TiO₂ particles, in the ~20 nm size range, can be incorporated into vesicles and retain their photoactivity through the dehydration/rehydration cycles that have been shown to concentrate species inside a vesicle.     

Mineralogical characterization of biosilicas versus geological analogs

Non-crystalline silica mineraloids are essential to life on Earth as they provide architectural structure to dominant primary producers, such as plants and phytoplankton, as well as to protists and sponges. Due to the difficulty in characterizing and quantifying the structure of highly disordered X-ray amorphous silica, relatively little has been done to understand the mineralogy of biogenic silica and how this may impact the material properties of biogenic silica, such as hardness and strength, or how biosilica might be identified and differentiated from its inorganic geological counterparts. Typically, geologically formed opal-A and hyalite opal-A_N are regarded as analogs to biogenic silica, however, some spectroscopic and imaging studies suggest that this might not be a reasonable assumption. In this study, we use a variety of techniques (X-ray diffraction, Raman spectroscopy, and scanning electron microscopy) to compare differences in structural disorder and bonding environments of geologically formed hydrous silicas (Opal-A, hyalite, geyserite) and silica glass versus biogenic silicas from an array of organisms. Our results indicate differences in the levels of structural disorder and the Raman-observed bonding environments of the SiO₂ network modes (D₁ mode) and the Q-species modes (~1015 cm⁻¹) between varieties of biogenic silicas and geologically formed silicas, which aligns with previous studies that suggest fundamental differences between biogenic and geologically formed silica. Biosilicas also differ structurally from one another by species of organism. Our mineralogical approach to characterizing biosilicas and differentiating them from other silicas may be expanded to future diagenesis studies, and potentially applied to astrobiology studies of Earth and other planets.     

Self-assembly of the first cells in a hydrophobic environment with hydrogen as the energy source.

Two fundamental questions in biology are how and where the first cell(s) self-assembled under anoxic conditions on the Earth. The possibility is explored that life first self-assembled in a hydrophobic environment in the subsurface protected from radiation with ubiquitous hydrogen as the likely universal energy source.