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Investigating the biological potential of galactic cosmic ray-induced radiation-driven chemical disequilibrium in the Martian subsurface environment

Abstract

There is growing evidence suggesting the presence of aqueous environment on ancient Mars, raising the question of the possibility of life in such an environment. Subsequently, with the erosion of the Martian atmosphere resulting in drastic changes in its climate, surface water disappeared, shrinking habitable spaces on the planet, with only a limited amount of water remaining near the surface in form of brines and water–ice deposits. Life, if it ever existed, would have had to adapt to harsh modern conditions, which includes low temperatures and surface pressure, and high radiation dose. Presently, there is no evidence of any biological activity on the planet’s surface, however, the subsurface environment, which is yet to be explored, is less harsh, has traces of water in form of water–ice and brines, and undergoes radiation-driven redox chemistry. I hypothesize that Galactic Cosmic Ray (GCR)-induced radiation-driven chemical disequilibrium can be used for metabolic energy by extant life, and host organisms using mechanisms seen in similar chemical and radiation environments on Earth. I propose a GCR-induced radiolytic zone, and discuss the prospects of finding such life with Rosalind Franklin rover of the ExoMars mission.

Introduction

The Viking mission, which included two landers, Viking 1 (1976–1982) and Viking 2 (1976–1980), was tasked with detecting possible biosignatures on the Martian surface. Although the mission generated excitement initially, it failed to detect any biological activity from samples collected from the surface. Although, recently upon reexamination of results from the Label Release experiment it has been argued that the possibility of extant life cannot be ruled out based on Viking results1. With our current understanding of the planet, a high level of radiation dose prohibits the survival of any stable ecosystem on the planet’s surface. Based on studies of geological features over the years, it is generally believed that Mars had abundant liquid water, and habitable conditions could have existed during the early to middle Noachian (4.1 to 3.7 billion years ago). Dramatic climate change resulted in drying of water bodies, and eventually shrinking of habitable spaces available on the planet. On present day Mars, there is evidence of only trace amounts of water in the form of brines, polar caps, hydrated minerals, and large deposits of water ice in the shallow subsurface environment2. The chemical environment also seems hostile to life. Oxidant species and perchlorates have been detected on the surface, and if heat activated, have the capability to destroy potential biomolecules and chemical biosignatures.

Although the Martian subsurface environment is yet to be directly probed, measurements from surface rovers, and satellite observations have provided reliable data to characterize it. Satellite observations of exposed water ice provides evidence of the existence of water below the surface. Ice deposits occur at a depth as shallow as 1 m below the surface, extending down to several kilometers in depth2. The Martian surface is bombarded by Galactic Cosmic Rays (GCRs), which are energetic charged particles and are able to penetrate a few meters below the surface3. Theoretical modeling of radiation propagation informs us about the energy deposition rate below the surface3,4,5. As discussed later, this continuous supply of energy leads to the formation of a number of chemical species, some of which may be potentially useful for metabolic chemistry. This is an additional source of energy along with radionuclides present in the Martian regolith.

Based on the results of radiation chemistry experiments, and observations of interstellar ices and comets, it is highly likely that prebiotic molecules are present below the surface. The degradation of potential subsurface organic molecules, resulting from GCR penetration occurs on timescales of millions of years4,5. This degradation effect is therefore negligible if an active ecosystem currently exists on Mars, since microbes have much smaller cell turnover times. Although, we do not understand how chemistry transforms itself into biology, we do understand basic properties of life, and minimum physicochemical environmental conditions required for life as we know it. The main aim of the manuscript is to estimate the likelihood of extremophile survivability in the Martian subsurface environment, which is planned to be explored with Rosalind Franklin rover of the ExoMars mission6. One of the objectives of the ExoMars mission is to search for biomarkers; find evidence of present or extinct life on the planet6. In this manuscript, I investigate the plausibility of radiation-induced chemical disequilibrium as a source of metabolic energy for potential Martian biota. In the following section, I will investigate how the Martian subsurface environment can be suitable for life, and whether it can be detected with Rosalind Franklin (ExoMars) rover.

Subsurface environment

For life to potentially survive on Mars, five basic requirements have to be satisfied: (1) Presence of organics to supply biological hardware, (2) a source chemical disequilibrium to supply energy for metabolic activity, (3) a medium for nutrient transport, such as water, (4) the ability to transform “harmful” chemical species to benign products, and (5) a radiation damage repair mechanism. I focus on the top 2 m of the subsurface environment, which is also the subject of a planned investigation by Rosalind Franklin rover6 (ExoMars mission). Since there is no in-situ measurement of the subsurface region, estimates can only be made based on a combination of numerical modeling of radiation penetration, laboratory radiation chemistry experiments, data from satellites and rovers. The subsurface radiation environment is dominated by GCR-induced secondary particles3,4,5. The interaction between GCR-induced radiation with the Martian soil is the main driver of chemistry in the region. Mars is extremely dry, but small pockets of water–ice, hydrated salts, and other chemicals (discussed later) upon interaction with radiation could potentially be able to provide chemical energy to sustain independent ecosystems.

Numerical modeling

We use the GEANT4 numerical model7 to calculate the energy deposition rate in the Martian subsurface. The model simulates charged particle propagation with matter, and can be used to model particle interactions in planetary atmospheres and surfaces. GEANT4 simulations have been found consistent with measurements by the RAD instrument8 on board MSL on the Martian surface. We follow the GEANT4 configuration described in Matthia et al. and calculate GCR propagation in the Martian atmosphere and regolith. GCR spectrum was obtained from the BON10 model9 which consists of 87% protons, 12% alpha particles, and 1% Iron nuclei which acts as a substitute for heavier particles. The Martian atmospheric properties were obtained from the Mars Climate Database (MCD)10, which compiles data from a number of instruments and is used widely in the Mars community. We validated our numerical approach with measurements of the background flux of GCRs made by RAD. We obtained a background dose rate of 0.59 mSv/day, which is consistent with 0.64 ± 12 mSv/day11 within instrumental uncertainties of RAD. Solar Proton Events (SPEs) can temporarily enhance the subsurface energy flux for a period of up to several hours in the top layer of the Martian subsurface. The energy of typical SPE protons entering the Martian atmosphere is a few 100 MeV, which can go up to 10 GeV in extreme cases12. Pavlov et al.5 calculated the subsurface energy deposition using the averaged proton flux of 33 protons cm−2 s−1 and found the top 20 cm layer impacted by SPEs and found it to be 2 × 108 eVg−1 s−1 on an average. However, a typical event of a total proton fluence of 109 protons cm−2 on Earth would translate to a flux of ~ 5 × 103 protons cm−2 s−1 on Mars (SPE assumed to be lasting for 24 h13), or about 150 times the average flux of 33 protons cm−2 s−1. This would result in a temporary enhancement in radiation dose over the background dose from GCRs in the top 20 cm of the subsurface, and might be damaging to potential lifeforms.

The energy deposition rate obtained from numerical modeling ranges between 105–107 eVg−1 s−1 in the top 2 m depth of the Martian subsurface as shown in Fig. 1. For comparison, deep subsurface ecosystems on Earth survive on ~ 106 eVg−1 s−1 14 which, as shown in Fig. 1 exists at a depth of 1–2 m. Geological evidence suggests a thicker Martian atmosphere in the past, which would reduce the GCR-induced energy deposition in the subsurface, making the proposed mechanism less relevant. GCR flux is also anti-correlated with solar wind activity, and a higher wind strength in the ancient past15 would have resulted in a lower GCR flux. A combination of these two factors makes this mechanism relevant on Mars later during its evolution into a planet with a thin atmosphere.

Subsurface organics

The presence of organics on the Martian surface has been established based on data from robotic missions16,17. They are either delivered through meteorites, or photo- and radio-chemically produced in the atmosphere, or through geological sources16. Organics can make their way below the surface through gardening. It has also been proposed that they can be produced in-situ from charged particle-induced chemistry (charged particle-ice interaction), similar to the way they are produced in interstellar ices and comets3. Radiation chemistry produces low-energy secondary electrons, which may result in reaction pathways not possible in photochemistry18. Radiolysis can also yield the formation of a number of biological useful molecules, as reported in some experiments18,19. It can also assist in carbon and nitrogen fixation, as seen in other cases20,21. Charged particle-induced reactions can produce complex organics such as amino acid precursors19, Complex Organic Molecules (COMs), which are organic molecules of six or more atoms, in cometary ice22, and abiotic ribose synthesis in interstellar ice analog experiments23.

One should expect similar chemical products to be detected in the top Martian subsurface with the Rosalind Franklin rover. Subsurface organics are shielded from high dose of surface UV, but are exposed to GCR-induced secondary particles. Their rate of degradation below the surface has been calculated using numerical models, which occurs over a timescale of millions of years4,5. However, organics can be preserved, if they are a part of a biological system since it will likely have a repair mechanism, and also, the degradation rate would be negligible on shorter timescales expected from biological processes.

Yield of organics can be calculated based on laboratory experiments studying organics production from proton irradiation in ice mixtures and Mars-analog conditions. Kobayashi et al. irradiated a mixture of CO2, CO, N2 and H2O and studied the formation of amino acid precursors, formaldehyde and HCN24. Amino acids were formed after hydrolysis of radiolytic products. The yield of glycine was found to be 0.02/100 eV, which at peak rate assuming 100% efficiency would yield a maximum of 1.26 × 1011 molecules/g annually. Other experiments have shown the G-value of formaldehyde, H2CO3 to be 0.2/100 eV25 which would yield 1.26 × 1012 molecules/g annually. Miyakawa (2002) with a CO2–N2–H2O atmosphere found the yield of the Uracil to be 1.6 × 10–7 molecules/eV26 or ~ 108 molecules/g annually.

GCR-induced chemical disequilibrium

As shown in Fig. 1, numerical models suggest that 106 to 107 eVg−1 s−1 of energy is potentially available for redox chemistry3. However, not all energy will be utilized for metabolic activity, and this energy deposition rate represents the upper limit of energy availability. Next, we discuss possible mechanisms which can be used for metabolic activity.

1. a)

GCR-induced H2 production

One of the main modes of chemical energy is abiotic hydrogen production, which is vital for some deep-subsurface ecosystems that thrive independent of photosynthesis. Hydrogen is a great source of fuel where photosynthesis is not viable. Radiolysis from radioactive substances is known to produce hydrogen and has been known as a source of energy for subsurface life on Earth14 and has been proposed as an energy source on Mars30,31. In deep-subsurface ecosystems, H2 is used for both hydrocarbon synthesis, and as a source of metabolic energy14,32,33. H2 is a source of energy for a number of electron acceptors and is important for Fischer–Tropsch (F–T) synthesis of organics. F–T synthesis is a reaction which catalytically converts CO and H2 to hydrocarbons33.

$$\left( {{\text{2n}} + {1}} \right){\text{ H}}_{{2}} + {\text{ n CO }} \to {\text{ C}}_{{\text{n}}} {\text{H}}_{{({\text{2n}} + {2})}} + {\text{ n H}}_{{2}} {\text{O}}$$

H2 is also produced by a number of chemical processes such as serpentinization, which is hydrolysis of ferrous silicates. In addition to radioactive substances, I propose that subsurface ice would be exposed to GCR secondaries, where H2O gets dissociated into a number of products, ultimately producing H2, O2 and H2O2, and H218 could be used for metabolic purposes32. Water–ice radiolysis is a well understood phenomenon, and O2 and H2O2 are also found in the interstellar medium18. Methanogens are known to use H2 and CO2 to produce CH4, both of which are available on Mars34. Methanogens are also found in permafrost, which are Earth-analogs to Martian subsurface. Methane had been detected at the Gale crater35 and a source is yet to be identified but detection or lack thereof from the Martian orbit remains controversial36. One possible source of methane production could be from potential Martian methanogens in the subsurface using GCR-induced radiolysis products to power their metabolism. Metabolic energy can also be obtained by H2 reacting with electron acceptors such as Fe3+ or SO42−.

2. b)

GCR-induced sulfate reduction

Desulforudis audaxviator is known to survive in a radiation environment dominated by energetic alpha, beta and gamma radiation, away from solar photons, deriving metabolic energy from sulfate reduction, aided by the presence of radioactive rocks in a 2.8 km deep gold mine37.

$${\text{4H}}_{{2}} + {\text{ H}}^{ + } + {\text{ SO}}_{{4}}^{{{2} - }} \to {\text{ HS}}^{ - } + {\text{ 4H}}_{{2}} {\text{O}}$$

Radionuclide-induced sulfate reduction has been suggested as a potential source of metabolic energy on Europa38. I propose that sulfate reduction aided by GCR-induced radiation chemistry could be another possible mechanism in the Martian subsurface where the GCR flux is substantial (Figs. 1 and 2). Aiding this mechanism is water ice, which is also available on Mars and discussed in detail later. The production rate of ATP molecules was estimated by multiplying the ATP yield39 with the maximum energy deposition rate, which turns out to be ~ 1.9 × 1014 molecules/g annually assuming 100% efficiency.

Other forms of disequilibrium

Chlorates and perchlorates are abundant on Mars. Perchlorates, if heat activated, can be harmful to organics, and some organisms. For example, they are found as water soluble contaminants that are harmful to human health. However, the presence of perchlorate does not exclude the possibility of life. Life, if evolved in this environment will develop capabilities to transform harmful chemicals to benign products. Some microbes have the capability to reduce chlorate and perchlorate, whose high reduction potential makes them efficient electron acceptors, and can be used for microbial metabolism40. Reduction of perchlorate to chlorate, chlorite and chloride has also been seen in some plants. One example of a perchlorate-reducing microbe is Dechloromonas aromatica, which in addition to perchlorate reduction, is also used for the bioremediative treatment of radionuclide contamination40. The key enzyme that enables the reaction is chlorite dismutase which converts ClO2− to Cl and O2 in presence of acetate which acts as a reducing agent. It is debatable whether or not microbes can use perchlorate reduction as an energy source to survive on Mars, but it is certain that the presence of perchlorates does not rule out the possibility of microbial communities powering their metabolism using alternate mechanisms.

Liquid medium

The presence of at least trace amounts of water is a basic requirement for life as we know it. The average Martian temperature is 210 K and the diurnal range is between 184 and 242 K. The summer temperature can rise up to 293 K. Life is known to survive in temperatures down to 77 K. The presence of salts on Mars has been reported over the years, which lowers the freezing point of water and absorbs atmospheric moisture. Magnesium perchlorate, magnesium chlorate and sodium perchlorate have been detected on the surface. Hydrated calcium perchlorate has been detected on the Gale crater. Water’s freezing point can be lowered to 40 K in the presence of sodium perchlorate and to 70 K in the presence of magnesium perchlorate. More recently, spectral evidence of flowing hydrated salts (Recurring Slope Linea or RSL) on the Martian surface was reported41. The detection of RSL supports the idea that briny solutions can flow on Mars although it is not an evidence of liquid water. It is plausible that life could be embedded in these briny solutions since halophilic organisms, such as Salinibacter ruber are known to thrive in such high salt environments. Some such microbes are known to survive in salt brines with concentrations up to 11%. Subsurface water–ice sheets have been observed up to 1–2 m below the surface and extend several tens of meters in depth2. An ice layer can also act as an insulator and can aid in maintaining more moderate temperatures below the surface.

Protection from potentially harmful chemicals

One of the fundamental properties of life is the ability to control its chemical environment. For example, a cell wall provides protection but also enables the exchange of chemicals through osmosis. On Mars, potential organisms can use similar mechanisms to maintain a favorable chemical environment. One possibility could be a habitat in porous rocks which can act as a protective shield but also allows for chemical exchange. This mechanism would enable organisms to survive in the presence of oxidants such as hydrogen peroxide, metal oxides such as Fe2O3 and FeO2−442, and perchlorates (if they are indeed dangerous to Martian biology). Low temperature would assist in maintaining disequilibrium in such conditions since the natural rate of reactions would be extremely low, and reactions can only occur with the help of catalysts for metabolic purposes.

One of the most important requirements for any organism to survive in high radiation conditions is to be able to effectively repair radiation-induced damage. A number of extremophiles are known to have capabilities to survive in high radiation environments. Deinococcus radiodurans is able to withstand radiation exposure up to 105 Sv, which is several orders of magnitude higher than the Martian subsurface43. Desulforudis audaxviator is able to thrive despite prolonged permanent exposure to radiation, likely by developing a damage repair mechanism which needs to be studied. Given a comparable dose environment in the 1–2 m depth in the Martian subsurface3 as shown in Fig. 1, it is highly plausible that extant life might have developed mechanisms to deal with radiation.

Discussion

In absence of a theory of the origin of life, it is not possible to determine whether life could have originated on ancient Mars when the environment was more hospitable to life as we know it. There is growing evidence that radiation-induced chemistry is capable of producing prebiotic compounds in a number of extraterrestrial scenarios and could have assisted with the potential origin of life on Mars3,18,19. However, with a thicker atmosphere of ancient Mars, the subsurface energy deposition from GCRs would be much lower making this mechanism less relevant. Later, when the planet lost much of its atmosphere, such potential ecosystem(s) can be sustained with radiation-driven chemical disequilibrium proposed in the paper (see below). So far, there is no known mechanism to understand how the formation of prebiotic compounds can lead to the origin of life. However, if life did exist on ancient Mars, there is a possibility of survival, which can be estimated based on our knowledge of extremophiles that are known to survive in comparably harsh environments on Earth. Such microbial life could have either originated on Mars, or transported from elsewhere, including from the Earth. Deep subsurface ecosystems are the only proxies for potentially extant subsurface Martian life. Desulforudis audaxviator, found in a 2.8 km deep South African mine is possibly the best such example. It is a sulfate reducing bacterium capable of thriving in a radioactive environment away from solar photons37. The bacterium is capable of using radiation-induced sulfate reduction for metabolic purposes and has developed damage repair mechanisms, which are crucial for survival in a high radiation environment37. As we have discussed, it has properties which are key to survival in the Martian subsurface. Deinococcus radiodurans is yet another extremophile, which is capable of withstanding radiation dose several orders of magnitude higher than that on Mars44. Some other well-known examples of extremophiles, among many, with properties required for survival in such an environment are Dechloromonas aromatica, which is a perchlorate-reducing bacterium40, Salinibacter ruber, a halophilic bacterium, and Methanosarcina barkeri, a methanogen.

Here is a summary of GCR-induced processes in the Martian subsurface environment:

• A source of chemical disequilibrium

• Energy deposition rate ~ 106–107 eVg−1 s−1

• Enhanced electron production

The Rosalind Franklin rover (ExoMars) is well suited to detect extant microbial life proposed in the manuscript. It is a rover on board the ExoMars mission (ESA and Roscosmos), designed to detect biosignatures on Mars, scheduled to be launched in summer 2022. The most important tool on the rover is the Subsurface drill, which is capable of penetrating and obtaining samples up to 2 m below the Martian surface6. The top 2 m of Martian subsurface at the Oxia Planum a clay-laden landing site, which is thought to have had a standing body of water in the past would be investigated for its exobiological potential6. There are a number of instruments on board the rover designed to identify and characterize possible biosignatures, and signs of extinct or extant life as described in details by Vago et al.6. The Mars Organic Molecule Analyzer (MOMA) for the study of organic molecules and possible chemical biosignatures. The close-up imager (CLUPI) for high-resolution color images with a resolution of up to 8 μm/pixel. The MicroOmega instrument for imaging crushed sample material with a resolution of 20 μm/pixel. The ADRON neutron and gamma ray detector to measure the subsurface hydrogen content up to a depth of 1 m. The Raman Laser Spectrometer (RLS) for the detection of organic functional groups. These instruments would assist in detecting signs of possible microbial life and/or chemical biosignatures. If radiation-induced biology as proposed in the manuscript is detected, one might also consider the possibility of a GCR-induced radiolytic zone, which is a range of depth below the planetary surface at which radiation is optimum for biologically useful redox chemistry. As shown in Fig. 2, up to ~ 107 eVg−1 s−1 of energy is available on the top 3 m of Mars where biology would be able to utilize radiation-induced products for metabolic purposes while also being able to repair damage. The proposed mechanism would be applicable on planetary objects with a thin or no atmosphere at all, such as on Europa, Moon, comets etc. provided that the other key features required for life are satisfied, as discussed earlier, and should be detectable with future planetary missions.

References

1. 1.

Levin, G. V. & Straat, P. A. The case for extant life on mars and its possible detection by the viking labeled release experiment. Astrobiology 16, 798–810. https://doi.org/10.1089/ast.2015.1464 (2016).

2. 2.

Dundas, C. M. et al. Exposed subsurface ice sheets in the Martian mid-latitudes. Science 359, 199–201 (2018).

3. 3.

Atri, D. On the possibility of galactic cosmic ray-induced radiolysis-powered life in subsurface environments in the Universe. J. R. Soc. Interface 13, 20160459 (2016).

4. 4.

Dartnell, L. R., Desorgher, L., Ward, J. M. & Coates, A. J. Modelling the surface and subsurface Martian radiation environment: Implications for astrobiology. Geophys. Res. Lett. https://doi.org/10.1029/2006gl027494 (2007).

5. 5.

Pavlov, A. A., Vasilyev, G., Ostryakov, V. M., Pavlov, A. K. & Mahaffy, P. Degradation of the organic molecules in the shallow subsurface of Mars due to irradiation by cosmic rays. Geophys. Res. Lett. https://doi.org/10.1029/2012gl052166 (2012).

6. 6.

Vago, J. L. et al. Habitability on early mars and the search for biosignatures with the ExoMars rover. Astrobiology 17, 471–510. https://doi.org/10.1089/ast.2016.1533 (2017).

7. 7.

Agostinelli, S. et al. GEANT4—a simulation toolkit. Nucl. Instrum. Methods Phys. Res. Sect. A 506, 250–303 (2003).

8. 8.

Hassler, D. M. et al. The radiation assessment detector (RAD) investigation. Space Sci. Rev. 170, 503–558 (2012).

9. 9.

O’Neill, P. M. Badhwar–O’Neill 2010 galactic cosmic ray flux model—Revised. IEEE Trans. Nucl. Sci. 57, 3148–3153 (2010).

10. 10.

10Millour, E. et al. in European Planetary Science Congress. 2015–2438.

11. 11.

Matthiä, D. et al. The Martian surface radiation environment—a comparison of models and MSL/RAD measurements. J. Sp. Wea. Sp. Clim. 6, A13 (2016).

12. 12.

Atri, D. Modelling stellar proton event-induced particle radiation dose on close-in exoplanets. Monthly Notices R. Astron. Soc. Lett. 465, L34–L38 (2017).

13. 13.

Atri, D. Stellar Proton Event-induced surface radiation dose as a constraint on the habitability of terrestrial exoplanets. Monthly Notices R. Astron. Soc. Lett. 492, L28–L33 (2020).

14. 14.

Lin, L. H. et al. Radiolytic H-2 in continental crust: Nuclear power for deep subsurface microbial communities. Geochem. Geophys. Geosyst. https://doi.org/10.1029/2004gc000907 (2005).

15. 15.

Wood, B. E., Müller, H.-R., Zank, G. P., Linsky, J. L. & Redfield, S. New mass-loss measurements from astrospheric Lyα absorption. Astrophys. J. Lett. 628, L143 (2005).

16. 16.

Freissinet, C. et al. Organic molecules in the Sheepbed Mudstone, Gale Crater, Mars. J. Geophys. Res. Planet 120, 495–514. https://doi.org/10.1002/2014je004737 (2015).

17. 17.

Eigenbrode, J. L. et al. Organic matter preserved in 3-billion-year-old mudstones at Gale crater, Mars. Science 360, 1096–1100. https://doi.org/10.1126/science.aas9185 (2018).

18. 18.

Arumainayagam, C. R. et al. Extraterrestrial prebiotic molecules: photochemistry vs radiation chemistry of interstellar ices. Chem. Soc. Rev. 48, 2293–2314. https://doi.org/10.1039/c7cs00443e (2019).

19. 19.

Kobayashi, K. in Astrobiology (ed Kakegawa T. Yamagishi A., Usui T.) (Springer, Singapore, 2019).

20. 20.

Gao, K. S. et al. Solar UV radiation drives CO2 fixation in marine phytoplankton: A double-edged sword. Plant Physiol. 144, 54–59. https://doi.org/10.1104/pp.107.098491 (2007).

21. 21.

Bickley, R. I. & Vishwanathan, V. Photocatalytically induced fixation of molecular nitrogen by near Uv-radiation. Nature 280, 306–308. https://doi.org/10.1038/280306a0 (1979).

22. 22.

Garrod, R. T. Simulations of ice chemistry in cometary nuclei. Astrophys. J. https://doi.org/10.3847/1538-4357/ab418e (2019).

23. 23.

Meinert, C. et al. Ribose and related sugars from ultraviolet irradiation of interstellar ice analogs. Science 352, 208–212 (2016).

24. 24.

Kobayashi, K. et al. Possible complex organic compounds on Mars. Adv. Space Res. 19, 1067–1076 (1997).

25. 25.

Gerakines, P., Moore, M. H. & Hudson, R. L. Carbonic acid production in H2O: CO2 ices. UV photolysis vs. proton bombardment. Astron. Astrophys. 357, 793–800 (2000).

26. 26.

Miyakawa, S., Yamanashi, H., Kobayashi, K., Cleaves, H. J. & Miller, S. L. Prebiotic synthesis from CO atmospheres: Implications for the origins of life. Proc. Natl. Acad. Sci. 99, 14628–14631 (2002).

27. 27.

Loeffler, M. J., Raut, U., Vidal, R. A., Baragiola, R. A. & Carlson, R. W. Synthesis of hydrogen peroxide in water ice by ion irradiation. Icarus 180, 265–273. https://doi.org/10.1016/j.icarus.2005.08.001 (2006).

28. 28.

Zolotov, M. Y. & Shock, E. L. A model for low-temperature biogeochemistry of sulfur, carbon, and iron on Europa. J. Geophys. Res. Planets 109, 1 (2004).

29. 29.

Clark, B. C. Surviving the limits to life at the surface of Mars. J. Geophys. Res. Planets 103, 28545–28555 (1998).

30. 30.

Tarnas, J. et al. Radiolytic H2 production on Noachian Mars: Implications for habitability and atmospheric warming. Earth Planet. Sci. Lett. 502, 133–145 (2018).

31. 31.

Dzaugis, M., Spivack, A. J. & D’Hondt, S. Radiolytic H2 production in Martian environments. Astrobiology 18, 1137–1146. https://doi.org/10.1089/ast.2017.1654 (2018).

32. 32.

Blair, C. C., D’Hondt, S., Spivack, A. J. & Kingsley, R. H. Radiolytic hydrogen and microbial respiration in subsurface sediments. Astrobiology 7, 951–970. https://doi.org/10.1089/ast.2007.0150 (2007).

33. 33.

Schulz, H. Short history and present trends of Fischer-Tropsch synthesis. Appl. Catal. A 186, 3–12 (1999).

34. 34.

Onstott, T. C. et al. Martian CH4: sources, flux, and detection. Astrobiology 6, 377–395 (2006).

35. 35.

Giuranna, M. et al. Independent confirmation of a methane spike on Mars and a source region east of Gale Crater. Nat. Geosci. 12, 326–332 (2019).

36. 36.

Korablev, O. et al. No detection of methane on Mars from early ExoMars trace Gas Orbiter observations. Nature 568, 517–520 (2019).

37. 37.

Chivian, D. et al. Environmental genomics reveals a single-species ecosystem deep within earth. Science 322, 275–278. https://doi.org/10.1126/science.1155495 (2008).

38. 38.

Altair, T., de Avellar, M. G. B., Rodrigues, F. & Galante, D. Microbial habitability of Europa sustained by radioactive sources. Sci Rep-Uk. https://doi.org/10.1038/s41598-017-18470-z (2018).

39. 39.

Schulze-Makuch, D. & Irwin, L. N. Life in the Universe (Springer, Berlin, 2004).

40. 40.

Coates, J. D. & Achenbach, L. A. Microbial perchlorate reduction: rocket-fuelled metabolism. Nat. Rev. Microbiol. 2, 569 (2004).

41. 41.

Ojha, L. et al. Spectral evidence for hydrated salts in recurring slope lineae on Mars. Nat. Geosci. 8, 829 (2015).

42. 42.

Lasne, J. et al. Oxidants at the surface of Mars: a review in light of recent exploration results. Astrobiology 16, 977–996 (2016).

43. 43.

Battista, J. R., Earl, A. M. & Park, M. J. Why is Deinococcus radiodurans so resistant to ionizing radiation?. Trends Microbiol 7, 362–365. https://doi.org/10.1016/S0966-842x(99)01566-8 (1999).

44. 44.

Daly, M. J. OPINION A new perspective on radiation resistance based on Deinococcus radiodurans. Nat. Rev. Microbiol. 7, 237–245. https://doi.org/10.1038/nrmicro2073 (2009).

Acknowledgements

I thank the three reviewers for their feedback which helped in improving the manuscript. This work is supported by the New York University Abu Dhabi (NYUAD) Institute research grant G1502.

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Atri, D. Investigating the biological potential of galactic cosmic ray-induced radiation-driven chemical disequilibrium in the Martian subsurface environment. Sci Rep 10, 11646 (2020). https://doi.org/10.1038/s41598-020-68715-7

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