Chemolithotrophy on the Noachian Martian breccia NWA 7034 via experimental microbial biotransformation

Multiple lines of evidence indicate an active hydrogeological history of Mars and chemolithoautotrophy-suited environments within its Noachian terrains. As a result, one of the primary aims of upcoming missions to Mars is to search for signs of ancient life. Here we report on laboratory-scaled microbially assisted chemolithoautotrophic biotransformation of the Noachian Martian breccia Northwest Africa (NWA) 7034 composed of ancient (~4.5 Gyr old) crustal materials from Mars. Nanoanalytical hyperspectral analysis provides clues for the trafficking and distribution of meteorite inorganic constituents in the microbial cell. We decipher biomineralization patterns associated with the biotransformation and reveal microbial nanometer-sized lithologies located inside the cell and on its outer surface layer. These investigations provide an opportunity to trace the putative bioalteration processes of the Martian crust and to assess the potential biogenicity of Martian materials. Terrestrial chemolithotrophic microbes living on Martian crustal material produce distinct biosignatures which could be detected by future missions searching for evidence of past life, according to experiments on a Noachian Martian meteorite.

R ecent works heightened interest in the search for biologically driven alterations on Mars and its potential as a habitat for past or present life [1][2][3][4] . Along with an active hydrogeological history of Mars, past chemolithoautotrophybased habitability was suggested for lacustrine sediments at Gale crater 1,2 , many instances of phyllosilicate-containing mineral deposits have been reported [5][6][7][8][9][10] , and eventually, a thermal habitability window of the early Mars crust was also featured 11 . A primary aim of the upcoming Mars exploration missions (Mars 2020 and ExoMars) is to search for signs of ancient life. Rovers specifically equipped and well suited to search for signs of life will traverse and explore the surface of Mars, focusing on the Noachian terrains with moisture-rich ancient geological history and mineral springs that could have been colonized by microorganisms. While a range of environments that would have been well suited to support a potential Martian chemolithoautotrophy have been proposed 1,2,12-14 , our understanding of putative biosignatures to be targeted in Martian materials is still poor. In this connection, a valuable source of information can be extracted from microbial fingerprints of chemolithotrophic life based on Martian materials. Chemolithoautotrophy, as the ancient metabolic form of life 15,16 , is thought to have enabled the transition of geochemistry into geobiochemistry and served as a biochemical link between the mineral world and the last universal common ancestor 15,[17][18][19] . Chemolithoautotrophic microorganisms employ an astonishing number of metabolic pathways to extract energy from diverse inorganic electron donors and acceptors 20 , shaping global biogeochemical cycles. Chemolithoautotrophs that thrive in geothermal springs metabolize inorganic chemicals, a source of energy that provided the most likely habitable niches for life on early Mars. Hydrothermal settings were widespread during the early geologic history of Mars 21,22 and continued into the late Amazonian period [23][24][25] . The tectono-magmatic complexes Tharsis and Elysium have long been known as late Noachian-early Hesperian hydrothermal environments on Mars 21,22 . Recently, a deep-water hydrothermal environment on ancient Mars (>3.8 Ga (billion years ago)) has been interpreted for Eridania basin based on massive clay-, carbonate-, and sulfide-bearing deposits 26 . Hydrothermal spring deposits of opaline silica sinter and the case for ancient hot springs in Gusev crater have also recently been reported 27,28 . Additionally, evidences of past hydrothermal activity in the Martian crust have been derived from the analysis of Martian meteorites 29,30 . As environmental conditions with hot spring settings were similar on early Earth and early Mars 31 , thermophilic chemolithoautotrophs are under the scope of particular interest 32 . Moreover, a number of studies have suggested thermophilicity of the last universal common ancestor, implying that life on Earth may have evolved from heat-loving organisms 33,34 .
Only a few works have been carried out for probing microbial interactions with astromaterials in relation to the study of Martian soil as a possible habitat for microorganisms. Single laboratory investigations on meteorites and Mars regolith analogs have been performed, demonstrating that some iron-oxidizing chemolithotrophs (e.g., Leptospirillum ferrooxidans, Acidithiobacillus ferrooxidans) could colonize metal-bearing astromaterials and use them as energy sources [35][36][37] . The microbial communities, which in situ colonize stony meteorites upon their fall to Earth, have been recently accessed 38 . Micrometer/nanometer-scale patterns and morphologies at the meteorite surfaces have also been previously investigated in connection with biogenicity criteria for the identification of fossil extraterrestrial life 39,40 . Using a chondrite meteorite with relatively high iron abundance, we have recently reported chemical analysis of the meteorite-microbial interface at nanometer-scale spatial resolution 41 Fig. 1 and Fig. 1) and investigated microbial-meteorite interactions at nanometer scale. The compositional variety of the polymictic regolith breccia NWA 7034 closely corresponds to the estimated bulk-crust composition of Mars 29,47,48 and to visible-infrared reflectance spectra of the Martian surface measured from orbit 29,49 . This brecciated regolith sample represents the Fig. 1 Images of various lithologic components in the NWA 7034 fragment used in this study. a The high-angle annular dark-field (HAADF) scanning transmission electron microscopy (STEM) image of the focused ion beam (FIB) section extracted for STEM analysis from the NWA 7034 fragment used in this study. b False-color energy-dispersive X-ray spectroscopy (EDS) composite image of NWA 7034 (Si-magenta, P-red, Syellow, Ca-white, Ti-cyan, Fe-blue). The full list of detected mineral phases is presented in Supplementary Table 1. The P signal in the region of the Pt layer deposited during FIB sample preparation is due to the overlap of the P-Kα and Pt-Mα peaks in the EDS spectra. The EDS spectra acquired in STEM mode from both regions are presented in Supplementary Fig. 12. oldest known Martian crust of the ancient crystallization ages (~4.5 Ga) 29,45,46 , with predominant plagioclase feldspar (38.0 ± 1.2%), low-Ca pyroxene (25.4 ± 8.1%), clinopyroxenes (18.2 ± 4.0%), iron-oxides (9.7 ± 1.3%), alkali feldspars (4.9 ± 1.3%), apatite (3.7 ± 2.6%), and to a lesser amount, chromite and ironsulfides 47 .

Results and discussion
Growth, elemental ultrastructural, and nanoanalytical spectroscopy analyses. M. sedula was cultivated on the Noachian Martian regolith breccia NWA 7034 ( Supplementary Fig. 1). The major lithologies of NWA 7034 used in the study were examined by nanometer-scale point analysis of the NWA 7034 thin section using energy-dispersive X-ray spectroscopy (EDS) in scanning transmission electron microscopy (STEM) mode and high-resolution scanning transmission electron microscopy (HR-STEM) techniques. Representative images and corresponding EDS elemental maps ( Fig. 1 and Supplementary Fig. 2 Fig. 2). Cl-, P-, and Ca-rich apatite grains 26 that exhibit amorphous textures and rounded morphologies were also present ( Fig. 1, Supplementary Fig. 2, and Supplementary Table 1). M. sedula was capable of chemolithoautotrophic growth on NWA 7034, breaking down its mineral material and solubilizing metals into the leachate solution ( Supplementary Fig. 3). Examination of the metal-mobilizing capacities of M. sedula by means of inductively coupled plasma mass spectrometry (ICP-MS) analysis showed a release of sulfur (S), along with a leaching of Na, Mg, P, K, and Ca as major elements released from NWA 7034 ( Supplementary  Fig. 3a). The mobilization of other minor and trace elements (B, Ni, Mo, Li, Rb, Sr, Sb, Cs, and W) was also detected ( Supplementary  Fig. 3b, c). Viewed from the bioenergetic perspective, pyrite(FeS 2 )rich domains within the proto-breccia clast of NWA 7034 29 can provide reduced sulfur and iron species as an energy source for M. sedula. Other Fe 2+ -bearing minerals (e.g., ilmenite FeTiO 3 ; magnetite Fe 2+ Fe 2 3+ O 4 2− ; pyroxene and plagioclase with Fe 2+ contributing to the total iron budget) can potentially satisfy the energy demand for M. sedula respiration needs, offering the metal ions of a suitable redox potential (Fe 2+ ) for its biooxidative metabolic activity. Resulting microbially produced Fe 3+ species promote further meteorite oxidation and enable the mobilization of metals (including abundant meteoritic Fe 3+ species) from the solid meteorite matrix into the solution. Such a joint microbially produced and abiotic Fe 3+ pull acts effectively as an oxidizing agent and facilitate the further process of metal mobilization, thus destroying the meteorite structure. Moreover, manganese biooxidation could also implement in NWA 7034 elemental dissolution mediated by M.  Table 2) did not reveal the presence of similar cellular assemblages.
Further HR-STEM analysis of M. sedula grown on NWA 7034 revealed that encrusted outer layer has a crystalline microstructure with lattice parameters close to different phosphate assemblages: Fe phosphates, Mn phosphates, and Al phosphates (Fig. 3a, b and Supplementary Table 3; see Supplementary  Table 4 for the inter-atomic spacing d-values). Closely related to M. sedula species Sulfolobus acidocaldarius also forms Fe phosphates on the cell surface, followed by complete encrustation with Fe phosphates upon incubation in the Fe-rich medium 50 . Mn, Si, and Zn primarily localize intracellularly in M. sedula ( Supplementary Fig. 4), while N, O, Fe, Na, Mg, S, Cr, and As are evenly dispersed through the cell (Fig. 2 Table 5). The As content has been reported in the meteorite NWA 7533 (paired with NWA 7034) 51 . Cells of M. sedula were capable of forming budding vesicles ( Fig. 4 and Supplementary Fig. 5), similar to the vesicular blebs which we previously observed during the growth of this archaeon on terrestrial minerals 43,52 . We have also previously observed the formation of M. sedula vesicles during growth on the ordinary chondrite NWA 1172 41 53 . Such vesicles are biogeochemically active and contain a functional protein machinery involved in iron oxidation, metal release, DNA compaction, and attachment to mineral surface 53 . Our STEM-EDS analysis detected Fe, Mn, S, Zn, Cr, Na, and As inside the vesicles ( Supplementary Fig. 5), indicating vesicular ability to immobilize metals from NWA 7034. Additionally, intensive vesiculation of M. sedula cells can function as an efficient mechanism of extracellular metal sequestration by binding with chelating agents (non-specific vesicular proteinaceous material and specific enzymatic detoxification of the metal to a less toxic form) 53 .
Intracellular nanocrystalline deposits. The NWA 7034-grown cells at the initial stages of biomineralization showed the accumulation of the blade-shaped structures protruding inwards from the cell wall to the cellular interior (Fig. 3c, d and Supplementary  Fig. 4a-d). HR-STEM imaging revealed that these blades are associated with nanometer-sized near-spherical aggregates, mainly comprised of Fe, O, Si, and Mn as suggested by STEM-EDS analysis (Fig. 3e, f). These structural nanoassemblages were rather of amorphous nature at the early stages of biomineralization ( Supplementary Fig. 4d), most likely representing an initial period of new mineral phase formation. At the late biomineralization stages of cell encrustation (Fig. 4), the cellular interior had heterogeneous, rugged, and coarse character ( Fig. 4a and Supplementary Fig. 5), and these metal-bearing nanoassemblages were converted into intracellular crystalline deposits of  Table 4), which requires further thorough clarification by synchrotron-assisted crystallography investigations.
It is noteworthy that the patterns of metal acquisition of this archaeon grown on the genuine Martian mineral material differ substantially from our recently reported observations of its growth on the ordinary chondrite NWA 1172 41 . Encrustation with the thick Fe(Mn, Al)/P-outer layer with P solely represented in this layer, intracellular formation of crystalline phases of Fe, Mn oxides, and mixed Mn silicates are distinguishable features of growth on the Noachian Martian breccia. In the case of NWA 1172, our TEM observations showed that the encrusted cell remnants and iron-bearing accumulations on the cell surface of M. sedula have an amorphous structure, with a mixture of different amorphous iron-oxides/hydroxides 41 . A similar encrustation of the cell surface, but of a simpler, homogenous and not complex nature, was observed earlier for M. sedula cultivated on metal-containing terrestrial materials 43,52 . When cells of M. sedula are grown on terrestrial minerals (e.g., tungsten mineral scheelite), then they are prone to encapsulation with homogenous crystalline tungsten-harboring nanolayers deposited over the microbial cell surface 43  Organometallic fingerprints. Further geochemical analysis of the biologically mediated alteration of the meteorite material was performed by investigating microbial fingerprints left on the Noachian breccia NWA 7034. Electron paramagnetic resonance (EPR) measurements were implemented to identify paramagnetic species of transition metal ions (e.g., Fe) in the NWA 7034 sample and to investigate the impact of M. sedula on their paramagnetic centers, as well as to identify possible newly formed paramagnetic complexes and reactive intermediates in the biologically processed NWA 7034. The EPR spectra obtained from raw, abiotic, and biogenic NWA 7034 samples were characterized by a signal with a broad linewidth ( Supplementary Fig. 11), which might refer to multiple ionic paramagnetic species. Biotransformation of the Noachian breccia NWA 7034 after the exposure to M. sedula resulted in a shifted g-value 2.93 at 273 K, compared to the raw and abiotically treated NWA 7034 material (g-values = 3.58/3.24, Supplementary Fig. 11). Low-spin ferric heme EPR resonances with highly specific g-values~2.9 are assigned to heme ligated axially by an imidazole ligand of the proximal histidine, bound to the iron with Fe-N distances in respiratory enzymes such as cytochromes 58,59 . A group of microbial heme-containing enzymes are characterized by this distinctive spectral feature of g-values = 2.93 [58][59][60][61][62] . These enzymes have been indicated as playing a role in electron transfer linked to energy-yielding processes in various chemolithotrophs, including M. sedula 44,56,57 , and most likely their heme prosthetic group contributes to a broad signal at g = 2.93 detectable solely after biotransformation of NWA 7034 ( Supplementary Fig. 11). Hemecontaining geoporphyrins can be resistant to degradation over long periods of time 63 , for instance, in geological context of 500 Ma-old oil shales 64 . Abiotically formed ancestors of heme-   65 . The extreme stability of certain heme-containing fossils (e.g., geoporphyrins) makes them attractive targets for the search of extinct life on Mars. However, care must be taken in distinguishing their biogenicity from abiotically formed hemecontaining compounds, e.g., abiotic porphyrins 66 . Fourier-transform infrared (FT-IR) spectroscopy data of the biotransformed NWA 7034 depicted several bands, which can be assigned to the vibration of functional S-containing aromatic organic groups 67,68 and contribute toward thiophene-bearing respiratory quinones in plasma membranes of M. sedula (Fig. 5). The unique C 30 isoprenoid quinones of sulfur metabolizing acidophilic chemolithotrophs of the archaeal order Sulfolobales (including M. sedula) are S-bearing aromatic derivatives of benzo-[b]-thiophen-4,7-quinone (see chemical formulas in Fig. 5), which function as electron carriers in the respiratory chains of these microorganisms 69,70 . These quinones comprise 0.28-0.38% of cell dry weight and represent ancestral biomarkers in terrestrial marine environments 71 . Notably, recent Sample Analysis at Mars (SAM) measurements onboard the Curiosity rover detected thiophenic organic sulfur in~3.5-Gyr (billion year)-old Murray formation, Gale crater 4 . These measurements did not reveal the exact source of thiophenic sulfur in the Murray formation. Both biogenic and abiotic origin could account for possible sources of S-bearing thiophenes on Mars. Apart from sulfurization of organic molecules over geological time, presence of S-bearing refractory organic matter in meteorite material, interplanetary dust particles, and abiotic organic constituents of igneous rocks, S-bearing respiratory quinones as metabolic fingerprints of M. sedula or similar archaea can also represent potential thiophene sources. Sulfurization appears to be a plausible mechanism to preserve Martian organic matter and to keep it detectable and stable under destructive environmental conditions in 3-Gyr-old mudstones at Gale crater 4 . S-bearing thiophenes of Sulfolobus quinones might be targeted as specific refractory organic biomarkers with a promising preservation potential. To enable detection by spacecraft instrumentation in a natural Martian environment, a non-destructive biomarker analysis should be considered in order to yield the fine chemical and structural features of potential biomarkers (e.g., long aliphatic side chains of S-bearing thiophenes from Sulfolobus quinones). This is an important part for assessing the biogenicity of identified organic compounds (e.g., pyrolysis-GC-MS-based destructive analysis cannot yield intact molecules of thiophene-bearing quinones, but only residual thiophenes).
The presented investigations on Martian meteorite biogeochemistry motivate further experimental and theoretical work to build a detailed understanding of the full functional setup of  21,72,73 . Several additional factors influence biosignature preservation in the rock record over geological time, e.g., rapidity of burial and mineral encapsulation of microbial cell 74,75 . When cells are rapidly encrusted in massive mineral precipitates (Figs. 2, 3 and Supplementary Figs. 4, 5) and subsequently rapidly buried in mineral sediments, they may form lithified biological materials, which are long-lived in geological environments. These structures form textural or morphologic biosignatures that can be preserved in the geologic record 74,75 . Furthermore, in Mars paleoenvironments anoxic conditions have been maintained 76 that restrict the oxidative destruction of organic matter and permit its preservation in the rock record at subsurface depth below the reach of other long-term harsh oxidizing factors, such as cosmic radiation 74,75,77 . If life evolved on Mars, the traces of fossil evidence of the earliest Martian biosphere may be well accessible in subsurface sediments. This has important implications for the exploration of past Martian habitability and potential Martian returned samples. The heavily Fe n Mn x Al y P z -encrusted cells with intracellular crystalline deposits of cubic Fe 3 O 4 , tetragonal Mn 3 O 4 , and mixed Mn x Si y O z phases, described in the present study, may constitute relevant putative biosignatures to be explored in the Martian geological record, if they persist destructive environmental conditions in reference to geologic timescales. We propose further focus on microbial nano-lithologies and metalloorganic signatures of the chemolithotrophs, including nanoscale metal-microbial interfaces and S-bearing specific organic biomarkers (thiophenes from Sulfolobales quinones). The present study considers thermoacidophilc microbial fingerprints on Martian mineral material which are relevant for potential hydrothermal spring settings on Mars. Further work should be conducted with Martian relevant mineral materials (e.g., Martian meteorites and Mars regolith analogs) for a wide variety of other chemolithotrophs, as other niches for the origin of life on Mars (e.g., psychrophilic ancestral phenotype relevant for low-temperature lacustrine settings) may certainly not be excluded. The nanoscale interfaces of chemolithotrophs grown on Martian materials should be further comprehensively investigated with advanced synchrotron-assisted spectroscopic techniques. These investigations may provide a guiding point for in situ measurements to analyze collected Mars samples. Furthermore, the performed studies may pave the way to the efficient nanoanalytical spectroscopy of collected and returned Mars samples in order to assess their potential biogenicity. Logistics Group GmbH, Meckenheim, Germany) in order to control agitation and temperature. The bioreactors were equipped with three 5 mL graduated glass pipettes, permitting carbon dioxide and air gassing and sampling of culture, respectively. The graduated pipettes used for gassing were attached by silicon tubing to sterile 0.2 µm filters (Millex-FG Vent filter unit, Millipore, Billerica, USA). A Luer-lock system was attached to the sampling graduated pipettes to operate sampling with sterile syringes (Soft-Ject, Henke Sass Wolf, Tuttlingen, Germany). A water-cooled condenser (Carl Roth, Karlsruhe, Germany) was used to force the off-gas to exit. Electronic thermocouple was used to control the temperature inside the bioreactors during the cultivations of M. sedula at 73°C. For chemolithoautotrophic growth, cultures were supplemented with 1 g/L of the Noachian breccia NWA 7034 (Mile High Meteorites Collection, 2.4 g fragment, non-covered with fusion crust, provided by Matt Morgan, Colorado Geological Survey). The meteorite sample (2.4 g, Supplementary Fig. 1) was ground and temperature sterilized at 180°C in a heating chamber for a minimum of 24 h prior to autoclavation at 121°C for 20 min. Abiotic controls comprised of culture media supplemented with sterilized NWA 7034, but without M. sedula cells, were included in all experiments. Growth of cells was observed by means of phase contrast/epifluorescence microscopy and release of soluble metal ions. To visualize cells wiggling on solid particles, a modified "DAPI" (4′-6′-Diamidino-2-phenylindole) procedure 37,41,43,52,78 was used for cell staining. The stained cells were observed and recorded with ProgRes ® MF cool camera (Jenoptik) mounted on Nikon eclipse 50i microscope, equipped with F36-500 Bandpass Filter Set (ex, 377/ 50 nm; em, 447/60 nm).

Methods
Scanning transmission electron microscopy. Cells of M. sedula were collected at stationary phase and primary fixed as described earlier 41 at 4°C in a 1 M Na-Cacodylate buffer supplemented with 2.5% glutaraldehyde. Followed by primary fixation, cells were post-fixed for 2 h in 1% OsO 4 . After thorough washing (three times with 2 × 0.1 M Na-cacodylate, 1x dH 2 O) and subsequent dehydration by a gradual ethanol series (30%, 50%, 70%, 90%, abs., each step with an incubation time of 30 min), cells were centrifuged after each dehydration step for 30 min and ; spectral intensities at 1454 cm -1 and from 2800 to 3000 cm -1 (CH 2 of lipids, isoprenoid chains of thiopheno-benzo-quinones). Spectra analysis was performed using reference database 67,68 and online database tool (http:// www.chem.msu.su/rus/teaching/tarasevich/Tarasevich_IR_tables_29-02-2012.pdf. resuspended for the subsequent ethanol treatment. Resulting samples were embedded in Spurr Low Viscosity Resin (Electron Microscopy Sciences, USA) and polymerized at 60°C for a minimum of 48 h. Semi-and ultrathin sectioning was conducted by means of a Reichert-Jung Ultracut E ultramicrotome, with 50-70 nm ultrathin sections, followed by their staining using uranyl-acetate (15 min), and deposited on 200 copper grid mesh coated with formvar/carbon (Agar Scientific, UK). Sample preparation of NWA 7034 for transmission electron microscopy has been performed by focused ion beam (FIB) sputtering using a FEI Quanta 3D FEG instrument, equipped with an electron column hosting a field-emission electron source and an ion column hosting a Ga-liquid metal ion source (LMIS). Sputtering progress has been monitored by electron beam (EB) induced secondary electron (SE) imaging at EB settings of 5 keV accelerating voltage. Before sputtering, a Pt layer (length × width × height = 8 μm × 3 μm × 3 μm) was deposited onto the NWA 7034 surface by applying FIB Pt deposition at 16 kV IB acceleration voltage. The deposited nanocrystalline Pt served as protection layer during subsequent preparation steps.
HR-STEM investigations were performed on a probe-corrected FEI Titan G2 60-300 (S/TEM) microscope with an X-FEG Schottky field-emission electron source operated at 60 and 300 kV (current of 150 pA, beam diameter below 1 Å in STEM mode). The microscope is equipped with a Super-X detector (Chemi-STEM technology, Thermo Fisher Scientific), comprised of a Dual EELS -Gatan Imaging Filter (GIF) Quantum and four separate silicon drift detectors. Two different highangle annular dark-field detectors (HAADF) and one annular dark-field (ADF) detector were applied to acquire the scanning transmission micrographs. Analytical investigations were performed using EDS and EELS carried out with a 19.7 and 20.5 mrad convergence and collection semiangles, respectively, [79][80][81] . Spectrum images were collected for different areas/locations of M. sedula cells. For each investigated spot, elemental maps were extracted from EELS and EDS spectrum images 41,43,52 . Afterwards, EELS and EDS spectra from investigated areas on the cell surface and inside of the cells were acquired/extracted. The acquired images and EELS spectra were processed via Gatan's Digital Micrograph being corrected for dark current and gain variations. EDS spectrum images were acquired and processed by using the VELOX software (Thermo Fisher Scientific).
The high-resolution STEM (HR-STEM) micrographs were processed by fast fourier transformation (FFT) in order to measure the hkl distances in a certain orientation of the polycrystalline structures. The transmitted and the diffracted electrons passing through a specimen and satisfying the Bragg condition, are focused at the back focal plane of the objective lens and form the electron diffraction pattern. In this plane, the space where the electron diffraction pattern can be observed is called the reciprocal space, which is mathematically given by the Fourier transform of the real space. The Fourier transform of an image is therefore its frequency-domain representation 82 . The interplanar distances in a certain orientation of a crystal are specific for each crystal with given lattice parameters. The hkl-d-values are directly measured on the HR-STEM images or using the FFT images which display the frequencies spots corresponding to the inverse of the interplanar distance. The advantage of using this method is the identification of even nanocrystals of dimensions smaller than 5 nm or atomic clusters of 2-3 nm (if ordered). The FFT measured d-values (hkl) have then been compared with the possible phases extracted from the ICSD database (https://icsd.fiz-karlsruhe.de) and their calculated d-values (hkl) [83][84][85][86][87][88][89][90][91][92][93][94][95][96] .
Infrared (IR) spectroscopy. IR spectra were recorded on a freeze-dried mineralcell pellet, obtained from the liquid culture, using a FT-IR spectrometer (Bruker Optik GmbH) equipped with an MCT-detector (32 scans, resolution 4 cm -1 ). Spectra analysis was performed using reference database 67,68 .
Electron paramagnetic resonance spectroscopy. The EPR spectra were measured as described earlier 34 on an X-Band Bruker Elexsys-II E500 CW-EPR spectrometer (Bruker Biospin GmbH, Rheinstetten, Germany) at 90 ± 1 and 293 ± 1 K using a high-sensitivity cavity (SHQE1119). Solid-state EPR measurements were conducted using microwave frequency settled to 9 GHz, center field to 6000 G, modulation frequency to 100 kHz, sweep width to 12,000 G, sweep time to 335.5 s, microwave power to 15 mW, modulation amplitude to 20.37 G, resolution to 4096 points, and conversion time to 81.92 ms. The samples were loaded in EPR quartz tubes (Wilmad-LabGlass, Vineland, NJ, USA) and scanning was performed three times, resulting to the average which was used for analysis. The spectrum of an empty control tube was subtracted from all sample spectra. The analysis of all spectra was performed using the Bruker Xepr software.
Metal analysis. To determine the extracellular concentrations of soluble metal ions mobilized from NWA 7034 meteoritic material, culture samples were preclarified by centrifugation. Resulting pre-clarified samples of the culture supernatants were filtered via 0.44 µm pore size filters and subsequently analyzed by ICP-MS, Perkin Elmer ELAN 6100.