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Table 1. The organic components in the least metamorphosed carbonaceous chondrites: Cl (Ivuna-like), CM (Mighei-like), CR (Renazzo-like), and Tagish Lake Empty fields indicate unavailable data. Concentrations are based on chromatographic peak intensities and include compounds identified by reference standards and mass spectra. The CM data are from Murchison CM2 meteorite (updated from Botta and Bada (2002)), unless otherv noted. The abundances are in ug/g (ppm), except where indicated. Table is adapted and modified from Alexander et al. (2017). “Averages from Alexander et al. (2012). Averages for recovered IOM from Alexander et al. (2007; 2014). °Range of the abundances in Orgueil and Ivuna (Ehrenfreund et al., 2001; Burton ef al., 201 4a). Range of abundances in Y-791198 (Naraoka et al., 1988; Shimoyama and Ogasawara, 2002; Glavin et al., 2010; Burton et al., 2014b). °Range of abundances in EET 92042, GRA 95229, and GRO 95577 (Martins et al., 2007; Glavin et al., 2010). ‘Range for different lithologies of Tagish Lake (Glavin et al., 2012; Hilts et al., 2014). ®Abundances in GRA 95229 (Pizzarello et al., 2008; 2012). ®SOM from Tagish Lake Pizzarello et al. (2001). ‘Range of abundances (Yuen and Kvenvolden, 1973; Huang et al., 2004). jFrom Aponte et al. (2014; 2015). KT ower limit for glyceric acid in Murchison (Cooper et al., 2001).

Table 1 The organic components in the least metamorphosed carbonaceous chondrites: Cl (Ivuna-like), CM (Mighei-like), CR (Renazzo-like), and Tagish Lake Empty fields indicate unavailable data. Concentrations are based on chromatographic peak intensities and include compounds identified by reference standards and mass spectra. The CM data are from Murchison CM2 meteorite (updated from Botta and Bada (2002)), unless otherv noted. The abundances are in ug/g (ppm), except where indicated. Table is adapted and modified from Alexander et al. (2017). “Averages from Alexander et al. (2012). Averages for recovered IOM from Alexander et al. (2007; 2014). °Range of the abundances in Orgueil and Ivuna (Ehrenfreund et al., 2001; Burton ef al., 201 4a). Range of abundances in Y-791198 (Naraoka et al., 1988; Shimoyama and Ogasawara, 2002; Glavin et al., 2010; Burton et al., 2014b). °Range of abundances in EET 92042, GRA 95229, and GRO 95577 (Martins et al., 2007; Glavin et al., 2010). ‘Range for different lithologies of Tagish Lake (Glavin et al., 2012; Hilts et al., 2014). ®Abundances in GRA 95229 (Pizzarello et al., 2008; 2012). ®SOM from Tagish Lake Pizzarello et al. (2001). ‘Range of abundances (Yuen and Kvenvolden, 1973; Huang et al., 2004). jFrom Aponte et al. (2014; 2015). KT ower limit for glyceric acid in Murchison (Cooper et al., 2001).

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ee eee eee ee eee EeeeEEEeE———e—E—E—E—EO Eee oo Along the continuum of thermal maturation, characteristic changes occur. Behar and Vandenbroucke 1987) produced structural models showing the progressive alteration of kerogens during their matur- ation. Kerogens become increasingly aromatic while bitumens become more aliphatic in character Craddock et al., 2015). There are also characteristic variations in the ratios of hydrogen to carbon H/C) and oxygen to carbon (O/C). Van Krevelen (1961) used these elemental ratios to classify coal, but this method is now widely used in classifying kerogens and their products. Such plots are typically referred to as van Krevelen diagrams. Four kerogen types are recognized: Type I, generated from algal and bacterial remains (algal kerogens); Type II, generated from zoo- and phytoplankton planktonic kerogens); Type III, from vascular plants (humic kerogens) and Type IV (residual kero- gens). Types I and II often occur in shales. Type III kerogens commonly occur as varieties of coal which can, on occasion, be interlayered with Type I and II bearing shales. Type 4 kerogens are often found as degraded surface deposits associated with coal (Vandenbrouke, 2003; Walters, 2007; Lawniczak et al., 2020) (Fig. 1).
ee eee eee ee eee EeeeEEEeE———e—E—E—E—EO Eee oo Along the continuum of thermal maturation, characteristic changes occur. Behar and Vandenbroucke 1987) produced structural models showing the progressive alteration of kerogens during their matur- ation. Kerogens become increasingly aromatic while bitumens become more aliphatic in character Craddock et al., 2015). There are also characteristic variations in the ratios of hydrogen to carbon H/C) and oxygen to carbon (O/C). Van Krevelen (1961) used these elemental ratios to classify coal, but this method is now widely used in classifying kerogens and their products. Such plots are typically referred to as van Krevelen diagrams. Four kerogen types are recognized: Type I, generated from algal and bacterial remains (algal kerogens); Type II, generated from zoo- and phytoplankton planktonic kerogens); Type III, from vascular plants (humic kerogens) and Type IV (residual kero- gens). Types I and II often occur in shales. Type III kerogens commonly occur as varieties of coal which can, on occasion, be interlayered with Type I and II bearing shales. Type 4 kerogens are often found as degraded surface deposits associated with coal (Vandenbrouke, 2003; Walters, 2007; Lawniczak et al., 2020) (Fig. 1).
Mass Balances for the pyrolysis products are from Byrne et al. (2022). Table 2. Calculations of the proportion of mass that is extractable for food production (x, equation (2)) and the minimum / maximum expected biomass that is extractable from asteroid Bennu (b, equation (3))
Mass Balances for the pyrolysis products are from Byrne et al. (2022). Table 2. Calculations of the proportion of mass that is extractable for food production (x, equation (2)) and the minimum / maximum expected biomass that is extractable from asteroid Bennu (b, equation (3))
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