Barite in hydrothermal environments as a recorder of subseafloor processes: a multiple-isotope study from the Loki's Castle vent field.

Barite chimneys are known to form in hydrothermal systems where barium-enriched fluids generated by leaching of the oceanic basement are discharged and react with seawater sulfate. They also form at cold seeps along continental margins, where marine (or pelagic) barite in the sediments is remobilized because of subseafloor microbial sulfate reduction. We test the possibility of using multiple sulfur isotopes (δ34S, Δ33S, ∆36S) of barite to identify microbial sulfate reduction in a hydrothermal system. In addition to multiple sulfur isotopes, we present oxygen (δ18O) and strontium (87Sr/86Sr) isotopes for one of numerous barite chimneys in a low-temperature (~20 °C) venting area of the Loki's Castle black smoker field at the ultraslow-spreading Arctic Mid-Ocean Ridge (AMOR). The chemistry of the venting fluids in the barite field identifies a contribution of at least 10% of high-temperature black smoker fluid, which is corroborated by 87Sr/86 Sr ratios in the barite chimney that are less radiogenic than in seawater. In contrast, oxygen and multiple sulfur isotopes indicate that the fluid from which the barite precipitated contained residual sulfate that was affected by microbial sulfate reduction. A sulfate reduction zone at this site is further supported by the multiple sulfur isotopic composition of framboidal pyrite in the flow channel of the barite chimney and in the hydrothermal sediments in the barite field, as well as by low SO4 and elevated H2S concentrations in the venting fluids compared with conservative mixing values. We suggest that the mixing of ascending H2- and CH4-rich high-temperature fluids with percolating seawater fuels microbial sulfate reduction, which is subsequently recorded by barite formed at the seafloor in areas where the flow rate is sufficient. Thus, low-temperature precipitates in hydrothermal systems are promising sites to explore the interactions between the geosphere and biosphere in order to evaluate the microbial impact on these systems.

Variation of the intercalating proline in artificial peptides mimicking the DNA binding and bending IHF protein.

The integration host factor (IHF) is a protein which sequence specifically induces a bend of double-stranded DNA by more than 160°. Based on IHF as lead structure, a peptide mimic was introduced resembling the positively charged body of the protein by a lysine dendrimer and the minor groove recognition loop by a cyclopeptide. The proline located close to the tip of the recognition loop intercalates between the base pair plane. It was modified in order to evaluate the influence of the side chain residue with respect to size (1,2,3,4-tetrahydroisoquinoline-3-carboxylic acid), aromaticity (phenylalanine), conformation of the five-membered ring [(4R)-fluoroproline, (4S)-fluoroproline, 3,4-dehydroproline], and the peptide backbone conformation (α-methylproline) on binding dsDNA and bending the double strand. Binding and bending studies were carried out by fluorescence resonance energy transfer experiments and gel electrophoresis using DNA sequences prepared by PCR with the IHF binding site in central or terminal position. Whereas aromatic residues and α-methylproline were not tolerated as proline substitute, incorporation of (4S)-fluoroproline and 3,4-dehydroproline provided enhanced binding.

Mechanisms of microtunneling in rock substrates: distinguishing endolithic biosignatures from abiotic microtunnels.

Rock-dwelling, endolithic micro-organisms can create tubular microcavities (TMCs) by the dissolution of rock substrates. Microtunnels can also conceivably be formed by abiotic processes, and collectively, these structures are here termed tubular microcavities. A textural record of life in subseafloor environments is provided by biological TMCs, and it is imperative to distinguish these from abiological tunnels. To this end, the morphologies and petrographic context of tunnels formed by chemical solution, physical abrasion, and biological processes are here described. Biological TMCs in volcanic glass are restricted to sites that were connected to early fluid circulation. Their shapes, distribution, and the absence of intersections exclude an origin by chemical dissolution of pre-existing heterogeneities such as, radiation damage trails, gas-escape structures, or fluid inclusion trails. Rather their characteristics are best explained by microbial dissolution, involving perhaps, cellular extensions that provide a mechanism of localizing and directing microtunnel formation as observed in terrestrial soils. Biological TMCs are contrasted with ambient inclusion trails (AITs) found in cherts and authigenic minerals. These differ in exhibiting longitudinal striae, a constant diameter, and polygonal cross-section, sometimes with terminal inclusions. The origin(s) of AITs remain unclear but they are hypothesized to form by migration of crystalline or organic inclusions in sealed substrates, in contrast to biotic TMCs that form in open systems. We present diagnostic morphological and petrographic criteria for distinguishing these different types of TMCs. Moreover, we argue that AIT-type processes are not viable in volcanic glass because of the absence of crystalline millstones, localized chemical solution agents, and elevated fluid pressures, necessary to drive this process.