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amafic serpentinizing systems can support both biotic and abiotic formation of organic matter (McCollom and Seewald, 2006, 2007; Bradley et al., 2009). The potential for long-term organi: vation in subsurface serpentine and hydrothermal systems is presently not well understood although Walter (1996) identifies several promising examples. 1, moderate; n/a, not available. rly constrained estimates; require improved knowledge of erosional processes and timescales. TABLE 4. SUMMARY OF EARLY MARS VOLCANIC AND HYDROTHERMAL ENVIRONMENTS, THEIR ABILITY TO SUPPORT SYNTHESIS, CONCENTRATION AND PRESERVATION OF ORGANIC MATTER (OM), AND THEIR DETECTABILITY BY REMOTE SENSING AND THE MSL INSTRUMENT PACKAGE

Table 4 amafic serpentinizing systems can support both biotic and abiotic formation of organic matter (McCollom and Seewald, 2006, 2007; Bradley et al., 2009). The potential for long-term organi: vation in subsurface serpentine and hydrothermal systems is presently not well understood although Walter (1996) identifies several promising examples. 1, moderate; n/a, not available. rly constrained estimates; require improved knowledge of erosional processes and timescales. TABLE 4. SUMMARY OF EARLY MARS VOLCANIC AND HYDROTHERMAL ENVIRONMENTS, THEIR ABILITY TO SUPPORT SYNTHESIS, CONCENTRATION AND PRESERVATION OF ORGANIC MATTER (OM), AND THEIR DETECTABILITY BY REMOTE SENSING AND THE MSL INSTRUMENT PACKAGE

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mod, moderate; n/a, not available. *Poorly constrained estimates; require improved knowledge of erosional processes and timescales. TABLE 3. SUMMARY OF EARLY MARS SEDIMENTARY ENVIRONMENTS THAT COULD BE ENCOUNTERED BY MSL WITH AN ASSESSMENT OF THEIR POTENTIA) SUPPORT ORGANIC MATTER (OM) FORMATION THROUGH BIOTIC AND ABIOTIC PROCESSES, THEIR CAPACITY TO CONCENTRATE AND PRESERVE OM AND Our ABILITY TO DETECT BY REMOTE SENSING AND MSL
mod, moderate; n/a, not available. *Poorly constrained estimates; require improved knowledge of erosional processes and timescales. TABLE 3. SUMMARY OF EARLY MARS SEDIMENTARY ENVIRONMENTS THAT COULD BE ENCOUNTERED BY MSL WITH AN ASSESSMENT OF THEIR POTENTIA) SUPPORT ORGANIC MATTER (OM) FORMATION THROUGH BIOTIC AND ABIOTIC PROCESSES, THEIR CAPACITY TO CONCENTRATE AND PRESERVE OM AND Our ABILITY TO DETECT BY REMOTE SENSING AND MSL
TABLE 6. As FOR TABLE 5, BUT APPLIED TO SEDIMENTARY ENVIRONMENTS AND PROCESSES Only fluvial floodplain, deltaic, lacustrine (perennial and evaporitic) environments are considered. *By measuring carbon abundances, SAM and APXS can address concentration processes.
TABLE 6. As FOR TABLE 5, BUT APPLIED TO SEDIMENTARY ENVIRONMENTS AND PROCESSES Only fluvial floodplain, deltaic, lacustrine (perennial and evaporitic) environments are considered. *By measuring carbon abundances, SAM and APXS can address concentration processes.
TABLE 7. SUMMARY OF PAYLOAD ELEMENTS THAT CAN BE USED TO CONFIRM ENVIRONMENTAL FEATURES THAT ARE RELEVANT TO INTERPRETATION OF STABLE ISOTOPIC COMPOSITIONS IN HyDROTHERMAL ENVIRONMENTS
TABLE 7. SUMMARY OF PAYLOAD ELEMENTS THAT CAN BE USED TO CONFIRM ENVIRONMENTAL FEATURES THAT ARE RELEVANT TO INTERPRETATION OF STABLE ISOTOPIC COMPOSITIONS IN HyDROTHERMAL ENVIRONMENTS
TABLE 8. SUMMARY OF PAYLOAD ELEMENTS THAT CAN BE USED TO CONFIRM ENVIRONMENTAL FEATURES THAT ARE RELEVANT TO INTERPRETATION OF STABLE ISOTOPIC COMPOSITIONS IN SEDIMENTARY ENVIRONMENTS they could be included in a regular sampling scheme. Detec: tion and quantification of atmospheric methane by MSL would provide an important verification of the Earth-based and orbital spectroscopic detections of methane per-billion levels (Formisano et al., 2004, Krasnopols at part y et al. 2004; Mumma et al., 2009). Temporal variations in methane concentration would be detectable by MSL and could poten: tially distinguish between episodic release of subsurface methane or methane destruction from photolytic, oxidative, o1 dust reactions in the modern environment (Atreya et al., 2006) Spatial variations in methane concentration are not expected to be observable unless MSL is proximal to a subsurface hy- drothermal, volcanic, or unstable hydrate point source. Using C-isotopic data to constrain the origins of atmospheric meth- ane on Mars, however, presents a formidable problem. Abiogenic methane production associated with serpentiniza- tion, that is, aqueous alteration of olivine- or pyroxene-rich rocks, or both, is a process that was likely prevalent early in Mars’ history and, feasibly, continues to the present day (Oze and Sharma, 2005). Multiple carbon and hydrogen isotopic
TABLE 8. SUMMARY OF PAYLOAD ELEMENTS THAT CAN BE USED TO CONFIRM ENVIRONMENTAL FEATURES THAT ARE RELEVANT TO INTERPRETATION OF STABLE ISOTOPIC COMPOSITIONS IN SEDIMENTARY ENVIRONMENTS they could be included in a regular sampling scheme. Detec: tion and quantification of atmospheric methane by MSL would provide an important verification of the Earth-based and orbital spectroscopic detections of methane per-billion levels (Formisano et al., 2004, Krasnopols at part y et al. 2004; Mumma et al., 2009). Temporal variations in methane concentration would be detectable by MSL and could poten: tially distinguish between episodic release of subsurface methane or methane destruction from photolytic, oxidative, o1 dust reactions in the modern environment (Atreya et al., 2006) Spatial variations in methane concentration are not expected to be observable unless MSL is proximal to a subsurface hy- drothermal, volcanic, or unstable hydrate point source. Using C-isotopic data to constrain the origins of atmospheric meth- ane on Mars, however, presents a formidable problem. Abiogenic methane production associated with serpentiniza- tion, that is, aqueous alteration of olivine- or pyroxene-rich rocks, or both, is a process that was likely prevalent early in Mars’ history and, feasibly, continues to the present day (Oze and Sharma, 2005). Multiple carbon and hydrogen isotopic
TABLE 9. AN ASSESSMENT OF IDENTIFIABLE TEXTURAL FEATURES, AND THEIR CORRESPONDING PRESERVATION WINDows, THAT May BE ENCOUNTERED IN MARS’ HYDROTHERMAL ENVIRONMENTS
TABLE 9. AN ASSESSMENT OF IDENTIFIABLE TEXTURAL FEATURES, AND THEIR CORRESPONDING PRESERVATION WINDows, THAT May BE ENCOUNTERED IN MARS’ HYDROTHERMAL ENVIRONMENTS
TABLE 10. AN ASSESSMENT OF IDENTIFIABLE TEXTURAL FEATURES, AND THEIR CORRESPONDING PRESERVATION WINDOWS THAT May BE ENCOUNTERED IN Mars’ SEDIMENTARY ENVIRONMENTS
TABLE 10. AN ASSESSMENT OF IDENTIFIABLE TEXTURAL FEATURES, AND THEIR CORRESPONDING PRESERVATION WINDOWS THAT May BE ENCOUNTERED IN Mars’ SEDIMENTARY ENVIRONMENTS
TABLE 11. FEATURES RELEVANT TO BIOSIGNATURE PRESERVATION IN HYDROTHERMAL ENVIRONMENTS ON EARLY MARS
TABLE 11. FEATURES RELEVANT TO BIOSIGNATURE PRESERVATION IN HYDROTHERMAL ENVIRONMENTS ON EARLY MARS
TABLE 12. SUMMARY OF MINERALOGICAL FEATURES RELEVANT TO BIOSIGNATURE PRESERVATION IN SEDIMENTARY ENVIRONMENTS ON EARLY Mars
TABLE 12. SUMMARY OF MINERALOGICAL FEATURES RELEVANT TO BIOSIGNATURE PRESERVATION IN SEDIMENTARY ENVIRONMENTS ON EARLY Mars
FIG 1. Earth’s biogeochemical carbon cycle, showing principal carbon reservoirs (boxes) in the mantle, crust, oceans and atmosphere, and showing the processes (arrows) that unite these reservoirs. The range of each of these reservoir boxes along the horizontal axis gives a visual estimate of typical 5'°C values for each reservoir. The vertical bars at right indicate the timeframes within which C typically completely traverses each of the four subcycles. For example, carbon can traverse the hydrosphere-atmosphere-biosphere subcycle typically in the timescale between 0 and 1000 years. See Des Marais, 2001 for detailed discussion.
FIG 1. Earth’s biogeochemical carbon cycle, showing principal carbon reservoirs (boxes) in the mantle, crust, oceans and atmosphere, and showing the processes (arrows) that unite these reservoirs. The range of each of these reservoir boxes along the horizontal axis gives a visual estimate of typical 5'°C values for each reservoir. The vertical bars at right indicate the timeframes within which C typically completely traverses each of the four subcycles. For example, carbon can traverse the hydrosphere-atmosphere-biosphere subcycle typically in the timescale between 0 and 1000 years. See Des Marais, 2001 for detailed discussion.
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GeologyGeochemistryMicrobial MatMars Science LaboratoryAtmospheric GasesGeological Processes
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