Kerogen

Kerogen is solid, insoluble organic matter in sedimentary rocks. It consists of a variety of organic materials, including dead plants, algae, and other microorganisms, that have been compressed and heated by geological processes. Altogether kerogen is estimated to contain 1016 tons of carbon. This makes it the most abundant source of organic compounds on earth, exceeding the total organic content of living matter 10,000-fold.[1]

Not to be confused with Kerosene.

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The type of kerogen present in a particular rock formation depends the type of organic material that was originally present. Kerogen can be classified by these origins: lacustrine (e.g., algal), marine (e.g., planktonic), and terrestrial (e.g., pollen and spores). The type of kerogen depends also on the degree of heat and pressure it has been subjected to, and the length of time the geological processes ran. The result is that a complex mixture of organic compounds reside in sedimentary rocks, serving as the precursor for the formation of hydrocarbons such as oil and gas. In short, kerogen amounts to fossilized organic matter that has been buried and subjected to high temperatures and pressures over millions of years, resulting in various chemical reactions and transformations.

Kerogen is insoluble in normal organic solvents and it does not have a specific chemical formula. Upon heating, kerogen converts in part to liquid and gaseous hydrocarbons. Petroleum and natural gas form from kerogen.[2] The name "kerogen" was introduced by the Scottish organic chemist Alexander Crum Brown in 1906,[3][4][5][6] derived from the Greek for "wax birth" (Greek: κηρός "wax" and -gen, γένεση "birth").

The increased production of hydrocarbons from shale has motivated a revival of research into the composition, structure, and properties of kerogen. Many studies have documented dramatic and systematic changes in kerogen composition across the range of thermal maturity relevant to the oil and gas industry. Analyses of kerogen are generally performed on samples prepared by acid demineralization with critical point drying, which isolates kerogen from the rock matrix without altering its chemical composition or microstructure.[7]

Formation

Kerogen is formed during sedimentary diagenesis from the degradation of living matter. The original organic matter can comprise lacustrine and marine algae and plankton and terrestrial higher-order plants. During diagenesis, large biopolymers from, e.g., proteins, lipids, and carbohydrates in the original organic matter, decompose partially or completely. This breakdown process can be viewed as the reverse of photosynthesis.[8] These resulting units can then polycondense to form geopolymers. The formation of geopolymers in this way accounts for the large molecular weights and diverse chemical compositions associated with kerogen. The smallest units are the fulvic acids, the medium units are the humic acids, and the largest units are the humins. This polymerization usually happens alongside the formation and/or sedimentation of one or more mineral components resulting in a sedimentary rock like oil shale.

When kerogen is contemporaneously deposited with geologic material, subsequent sedimentation and progressive burial or overburden provide elevated pressure and temperature owing to lithostatic and geothermal gradients in Earth's crust. Resulting changes in the burial temperatures and pressures lead to further changes in kerogen composition including loss of hydrogen, oxygen, nitrogen, sulfur, and their associated functional groups, and subsequent isomerization and aromatization Such changes are indicative of the thermal maturity state of kerogen. Aromatization allows for molecular stacking in sheets, which in turn drives changes in physical characteristics of kerogen, such as increasing molecular density, vitrinite reflectance, and spore coloration (yellow to orange to brown to black with increasing depth/thermal maturity).

During the process of thermal maturation, kerogen breaks down in high-temperature pyrolysis reactions to form lower-molecular-weight products including bitumen, oil, and gas. The extent of thermal maturation controls the nature of the product, with lower thermal maturities yielding mainly bitumen/oil and higher thermal maturities yielding gas. These generated species are partially expelled from the kerogen-rich source rock and in some cases can charge into a reservoir rock. Kerogen takes on additional importance in unconventional resources, particularly shale. In these formations, oil and gas are produced directly from the kerogen-rich source rock (i.e. the source rock is also the reservoir rock). Much of the porosity in these shales is found to be hosted within the kerogen, rather than between mineral grains as occurs in conventional reservoir rocks.[9][10] Thus, kerogen controls much of the storage and transport of oil and gas in shale.[9]

Another possible method of formation is that vanabin-containing organisms cleave the core out of chlorin-based compounds such as the magnesium in chlorophyll and replace it with their vanadium center in order to attach and harvest energy via light-harvesting complexes. It is theorized that the bacteria contained in worm castings, Rhodopseudomonas palustris, do this during its photoautotrophism mode of metabolism. Over time colonies of light harvesting bacteria solidify, forming kerogen .

Composition
Structure of a vanadium porphyrin compound (left) extracted from petroleum by Alfred E. Treibs, father of organic geochemistry. The close structural similarity of this molecule and chlorophyll a (right) helped establish that petroleum was derived from plants.[11]

Kerogen is a complex mixture of organic chemical compounds that make up the most abundant fraction of organic matter in sedimentary rocks.[12] As kerogen is a mixture of organic materials, it is not defined by a single chemical formula. Its chemical composition varies substantially between and even within sedimentary formations. For example, kerogen from the Green River Formation oil shale deposit of western North America contains elements in the proportions carbon 215 : hydrogen 330 : oxygen 12 : nitrogen 5 : sulfur 1.[13]

Kerogen is insoluble in normal organic solvents in part because of the high molecular weight of its component compounds. The soluble portion is known as bitumen. When heated to the right temperatures in the earth's crust, (oil window c. 50–150 °C, gas window c. 150–200 °C, both depending on how quickly the source rock is heated) some types of kerogen release crude oil or natural gas, collectively known as hydrocarbons (fossil fuels). When such kerogens are present in high concentration in rocks such as organic-rich mudrocks shale, they form possible source rocks. Shales that are rich in kerogen but have not been heated to required temperature to generate hydrocarbons instead may form oil shale deposits.

The chemical composition of kerogen has been analyzed by several forms of solid state spectroscopy. These experiments typically measure the speciations (bonding environments) of different types of atoms in kerogen. One technique is 13C NMR spectroscopy, which measures carbon speciation. NMR experiments have found that carbon in kerogen can range from almost entirely aliphatic (sp3 hybridized) to almost entirely aromatic (sp2 hybridized), with kerogens of higher thermal maturity typically having higher abundance of aromatic carbon.[14] Another technique is Raman spectroscopy. Raman scattering is characteristic of, and can be used to identify, specific vibrational modes and symmetries of molecular bonds. The first-order Raman spectra of kerogen comprises two principal peaks;[15] a so-called G band ("graphitic") attributed to in-plane vibrational modes of well-ordered sp2 carbon and a so-called D band ("disordered") from symmetric vibrational modes of sp2 carbon associated with lattice defects and discontinuities. The relative spectral position (Raman shift) and intensity of these carbon species is shown to correlate to thermal maturity,[16][17][18][19][20][21] with kerogens of higher thermal maturity having higher abundance of graphitic/ordered aromatic carbons. Complementary and consistent results have been obtained with infrared (IR) spectroscopy, which show that kerogen has higher fraction of aromatic carbon and shorter lengths of aliphatic chains at higher thermal maturities.[22][23] These results can be explained by the preferential removal of aliphatic carbons by cracking reactions during pyrolysis, where the cracking typically occurs at weak C–C bonds beta to aromatic rings and results in the replacement of a long aliphatic chain with a methyl group. At higher maturities, when all labile aliphatic carbons have already been removed—in other words, when the kerogen has no remaining oil-generation potential—further increase in aromaticity can occur from the conversion of aliphatic bonds (such as alicyclic rings) to aromatic bonds.

IR spectroscopy is sensitive to carbon-oxygen bonds such as quinones, ketones, and esters, so the technique can also be used to investigate oxygen speciation. It is found that the oxygen content of kerogen decreases during thermal maturation (as has also been observed by elemental analysis), with relatively little observable change in oxygen speciation.[22] Similarly, sulfur speciation can be investigated with X-ray absorption near edge structure (XANES) spectroscopy, which is sensitive to sulfur-containing functional groups such as sulfides, thiophenes, and sulfoxides. Sulfur content in kerogen generally decreases with thermal maturity, and sulfur speciation includes a mix of sulfides and thiophenes at low thermal maturities and is further enriched in thiophenes at high maturities.[24][25]

Overall, changes in kerogen composition with respect to heteroatom chemistry occur predominantly at low thermal maturities (bitumen and oil windows), while changes with respect to carbon chemistry occur predominantly at high thermal maturities (oil and gas windows).

Microstructure

The microstructure of kerogen also evolves during thermal maturation, as has been inferred by scanning electron microscopy (SEM) imaging showing the presence of abundant internal pore networks within the lattice of thermally mature kerogen.[9][26] Analysis by gas sorption demonstrated that the internal specific surface area of kerogen increases by an order of magnitude (~ 40 to 400 m2/g) during thermal maturation.[27][28] X-ray and neutron diffraction studies have examined the spacing between carbon atoms in kerogen, revealing during thermal maturation a shortening of carbon-carbon distances in covalently bonded carbons (related to the transition from primarily aliphatic to primarily aromatic bonding) but a lengthening of carbon-carbon distances in carbons at greater bond separations (related to the formation of kerogen-hosted porosity).[29] This evolution is attributed to the formation of kerogen-hosted pores left behind as segments of the kerogen molecule are cracked off during thermal maturation.

Physical properties

These changes in composition and microstructure result in changes in the properties of kerogen. For example, the skeletal density of kerogen increases from approximately 1.1 g/ml at low thermal maturity to 1.7 g/ml at high thermal maturity.[30][31][32] This evolution is consistent with the change in carbon speciation from predominantly aliphatic (similar to wax, density < 1 g/ml) to predominantly aromatic (similar to graphite, density > 2 g/ml) with increasing thermal maturity.

Spatial heterogeneity

Additional studies have explored the spatial heterogeneity of kerogen at small length scales. Individual particles of kerogen arising from different inputs are identified and assigned as different macerals. This variation in starting material may lead to variations in composition between different kerogen particles, leading to spatial heterogeneity in kerogen composition at the micron length scale. Heterogeneity between kerogen particles may also arise from local variations in catalysis of pyrolysis reactions due to the nature of the minerals surrounding different particles. Measurements performed with atomic force microscopy coupled to infrared spectroscopy (AFM-IR) and correlated with organic petrography have analyzed the evolution of the chemical composition and mechanical properties of individual macerals of kerogen with thermal maturation at the nanoscale.[33] These results indicate that all macerals decrease in oxygen content and increase in aromaticity (decrease in aliphalicity) during thermal maturation, but some macerals undergo large changes while other macerals undergo relatively small changes. In addition, macerals that are richer in aromatic carbon are mechanically stiffer than macerals that are richer in aliphatic carbon, as expected because highly aromatic forms of carbon (such as graphite) are stiffer than highly aliphatic forms of carbon (such as wax).

Types

Labile kerogen breaks down to generate principally liquid hydrocarbons (i.e., oil), refractory kerogen breaks down to generate principally gaseous hydrocarbons, and inert kerogen generates no hydrocarbons but forms graphite.

In organic petrography, the different components of kerogen can be identified by microscopic inspection and are classified as macerals. This classification was developed originally for coal (a sedimentary rock that is rich in organic matter of terrestrial origin) but is now applied to the study of other kerogen-rich sedimentary deposits.

The Van Krevelen diagram is one method of classifying kerogen by "types", where kerogens form distinct groups when the ratios of hydrogen to carbon and oxygen to carbon are compared.[34]

Type I: algal/sapropelic

Type I kerogens are characterized by high initial hydrogen-to-carbon (H/C) ratios and low initial oxygen-to-carbon (O/C) ratios. This kerogen is rich in lipid-derived material and is commonly, but not always, from algal organic matter in lacustrine (freshwater) environments. On a mass basis, rocks containing type I kerogen yield the largest quantity of hydrocarbons upon pyrolysis. Hence, from the theoretical view, shales containing type I kerogen are the most promising deposits in terms of conventional oil retorting.[35]

Type II: planktonic

Type II kerogens are characterized by intermediate initial H/C ratios and intermediate initial O/C ratios. Type II kerogen is principally derived from marine organic materials, which are deposited in reducing sedimentary environments. The sulfur content of type II kerogen is generally higher than in other kerogen types, and sulfur is found in substantial amounts in the associated bitumen. Although pyrolysis of type II kerogen yields less oil than type I, the amount yielded is still sufficient for type II-bearing sedimentary deposits to be petroleum source rocks.

  • Hydrogen:carbon atomic ratio < 1.25
  • Oxygen:carbon atomic ratio 0.03–0.18
  • Derived principally from marine plankton and algae
  • Produces a mixture oil and gas under heating

Type II-S: sulfurous

Similar to type II but with high sulfur content.

Type III: humic

Type III kerogens are characterized by low initial H/C ratios and high initial O/C ratios. Type III kerogens are derived from terrestrial plant matter, specifically from precursor compounds including cellulose, lignin (a non-carbohydrate polymer formed from phenyl-propane units that binds the strings of cellulose together); terpenes and phenols. Coal is an organic-rich sedimentary rock that is composed predominantly of this kerogen type. On a mass basis, type III kerogens generate the lowest oil yield of principal kerogen types.

  • Hydrogen:carbon atomic ratio < 1
  • Oxygen:carbon atomic ratio 0.03–0.3
  • Has low hydrogen content because of abundant aromatic carbon structures
  • Derived from terrestrial (land) plants
  • Tends to produce gas under heating (recent research has shown that type III kerogens can actually produce oil under extreme conditions)[36]

Type IV: inert/residual

Type IV kerogen comprises mostly inert organic matter in the form of polycyclic aromatic hydrocarbons. They have no potential to produce hydrocarbons.[37]

  • Hydrogen:carbon atomic ratio < 0.5

Kerogen cycle
Kerogen cycle[38]

The diagram on the right shows the organic carbon cycle with the flow of kerogen (black solid lines) and the flow of biospheric carbon (green solid lines), showing both the fixation of atmospheric CO2 by terrestrial and marine primary productivity. The combined flux of reworked kerogen and biospheric carbon into ocean sediments constitutes total organic carbon burial entering the endogenous kerogen pool.[38][39]

Extra-terrestrial

Carbonaceous chondrite meteorites contain kerogen-like components.[40] Such material is thought to have formed the terrestrial planets. Kerogenous materials have been detected also in interstellar clouds and dust around stars.[41]

The Curiosity rover has detected organic deposits similar to kerogen in mudstone samples in Gale Crater on Mars using a revised drilling technique. The presence of benzene and propane also indicates the possible presence of kerogen-like materials, from which hydrocarbons are derived.[42][43][44][45][46][47][48][49][50]

See also
  • Asphaltene – Heavy organic molecular substances that are found in crude oil
  • Oil shale geology – Branch of geology
  • Petroleum geology – Study of the origin, occurrence, movement, accumulation, and exploration of hydrocarbon fuels
  • Tholin – Class of molecules formed by ultraviolet irradiation of organic compounds

References
  1. Horsfield, Brian (4 September 2019). "Oil and Gas Shales". Hydrocarbons, Oils and Lipids: Diversity, Origin, Chemistry and Fate. Springer Link. pp. 1–34. doi:10.1007/978-3-319-54529-5_18-1. ISBN 978-3-319-54529-5. S2CID 134257943. Archived from the original on 26 November 2022. Retrieved 26 November 2022.{{cite book}}: CS1 maint: bot: original URL status unknown (link)
  2. Vandenbroucke, M.,Largeau, C. (2007). "Kerogen origin, evolution and structure". Organic Geochemistry. 38 (5): 719–833. doi:10.1016/j.orggeochem.2007.01.001.{{cite journal}}: CS1 maint: multiple names: authors list (link)
  3. Oxford English Dictionary 3rd Ed. (2003)
  4. Cane, R.F. (1976). "The origin and formation of oil shale". In Teh Fu Yen; Chilingar, G.V. (eds.). Oil Shale. Amsterdam: Elsevier. p. 27. ISBN 978-0-444-41408-3. Retrieved 31 May 2009.
  5. Hutton, A.C.; Bharati, S.; Robl, T. (1994). "Chemical and Petrographic Classification of Kerogen/Macerals". Energy Fuels. 8 (6): 1478–1488. doi:10.1021/ef00048a038.
  6. Steuart, D.R., in Cadell, H.M. et al. Oil-Shales of Lothians iii. 142 (1906) "We are indebted to Professor Crum Brown, F.R.S., for suggesting the term Kerogen to express the carbonaceous matter in shale that gives rise to crude oil in distillation."
  7. Suleimenova, A.; et al. (2014). "Acid demineralization with critical point drying: A method for kerogen isolation that preserves microstructure". Fuel. 135: 492–497. doi:10.1016/j.fuel.2014.07.005.
  8. Tucker M.E. (1988) Sedimentary Petrology, An Introduction, Blackwell, London. p197. ISBN 0-632-00074-0
  9. Richardson, E.J.; Montenari, M. (2020). "Assessing shale gas reservoir potential using multi-scaled SEM pore network characterizations and quantifications: The Ciñera-Matallana pull-apart basin, NW Spain". Stratigraphy & Timescales. 5: 677–755. doi:10.1016/bs.sats.2020.07.001. ISBN 9780128209912. S2CID 229217907 – via Elsevier Science Direct.
  10. Loucks, R.; et al. (2009). "Morphology, genesis, and distribution of nanometer-scale pores in siliceous mudstones of the Mississippian Barnett Shale". Journal of Sedimentary Research. 79 (12): 848–861. Bibcode:2009JSedR..79..848L. doi:10.2110/jsr.2009.092. S2CID 59400824.
  11. Kvenvolden, K.A. (2006). "Organic geochemistry – A retrospective of its first 70 years". Org. Geochem. 37: 1–11. doi:10.1016/j.orggeochem.2005.09.001. S2CID 95305299.
  12. "Kerogen". Oilfield Glossary. Schlumberger.
  13. Robinson, W.E. (1976). "Origin and characteristics of Green River oil shale". In Teh Fu Yen; Chilingar, George V. (eds.). Oil Shale. Amsterdam: Elsevier. pp. 61–80. ISBN 978-0-444-41408-3.
  14. Kelemen, S.; et al. (2007). "Direct characterization of kerogen by X-ray and solid-state 13C nuclear magnetic resonance methods". Energy & Fuels. 21 (3): 1548–1561. doi:10.1021/ef060321h.
  15. Ferrari, A.C. (2007). "Raman spectroscopy of graphene and graphite: Disorder, electron–phonon coupling, doping and nonadiabatic effects". Solid State Communications. 143 (1–2): 42–52. Bibcode:2007SSCom.143...47F. doi:10.1016/j.ssc.2007.03.052.
  16. Spötl, C.; et al. (1998). "Kerogen maturation and incipient graphitization of hydrocarbon source rocks in the Arkoma Basin, Oklahoma and Arkansas: a combined petrographic and Raman spectrometric study". Organic Geochemistry. 28 (9–10): 535–542. doi:10.1016/S0146-6380(98)00021-7.
  17. Kelemen, S.; Fang, H.L. (2001). "Maturity trends in Raman spectra from kerogen and coal". Energy & Fuels. 15 (3): 653–658. doi:10.1021/ef0002039.
  18. Beyssac, O.; et al. (2002). "Raman spectra of carbonaceous material in metasediments: a new geothermometer". Journal of Metamorphic Geology. 20 (9): 859–871. Bibcode:2002JMetG..20..859B. doi:10.1046/j.1525-1314.2002.00408.x. S2CID 129891723.
  19. Liu, D.; et al. (2013). "Sample maturation calculated using Raman spectroscopic parameters for solid organics: methodology and geological applications". Chinese Science Bulletin. 58 (11): 1285–1298. Bibcode:2013ChSBu..58.1285L. doi:10.1007/s11434-012-5535-y.
  20. Schmidt Mumm, A.; Inan, S. (2016). "Microscale organic maturity determination of graptolites using Raman spectroscopy". International Journal of Coal Geology. 162: 96–107. doi:10.1016/j.coal.2016.05.002.
  21. Sauerer, B.; et al. (2017). "Fast and accurate shale maturity determination by Raman spectroscopy measurement with minimal sample preparation". International Journal of Coal Geology. 173 (9–10): 150–157. doi:10.1016/S0146-6380(98)00021-7.
  22. Craddock, P.R.; et al. (2015). "Evolution of Kerogen and Bitumen during Thermal Maturation via Semi-Open Pyrolysis Investigated by Infrared Spectroscopy". Energy & Fuels. 29 (4): 2197–2210. doi:10.1021/ef5027532.
  23. Craddock, P.R.; et al. (2018). "Chemical, Molecular, and Microstructural Evolution of Kerogen during Thermal Maturation: Case Study from the Woodford Shale of Oklahoma". Energy & Fuels. 32 (4): 4859–4872. doi:10.1021/ef5027532.
  24. Kelemen, S.; et al. (2007). "Direct Characterization of Kerogen by X-ray and Solid-State 13C Nuclear Magnetic Resonance Methods". Energy & Fuels. 21 (3): 1548–1561. doi:10.1021/ef060321h.
  25. Pomerantz, A.E.; et al. (2014). "Sulfur speciation in kerogen and bitumen from gas and oil shales". Organic Geochemistry. 68: 5–12. doi:10.1016/j.orggeochem.2013.12.011.
  26. Loucks, R.; et al. (2009). "Morphology, genesis, and distribution of nanometer-scale pores in siliceous mudstones of the Mississippian Barnett Shale". Journal of Sedimentary Research. 79 (12): 848–861. Bibcode:2009JSedR..79..848L. doi:10.2110/jsr.2009.092. S2CID 59400824.
  27. Cheshire, S.; et al. (2017). "Assessing thermal maturity beyond the reaches of vitrinite reflectance and Rock-Eval pyrolysis: A case study from the Silurian Qusaiba formation". International Journal of Coal Geology. 180: 29–45. doi:10.1016/j.coal.2017.07.006.
  28. Craddock, P.R.; et al. (2018). "Chemical, Molecular, and Microstructural Evolution of Kerogen during Thermal Maturation: Case Study from the Woodford Shale of Oklahoma". Energy & Fuels. 32 (4): 4859–4872. doi:10.1021/ef5027532.
  29. Bousige C.; et al. (2016). "Realistic molecular model of kerogen's nanostructure". Nature Materials. 15 (5): 576–582. Bibcode:2016NatMa..15..576B. doi:10.1038/nmat4541. PMID 26828313.
  30. Guidry, K. et al. (1995) Development of Laboratory and Petrophysical Techniques for Evaluating Shale Reservoirs, Final Report, Gas Research Institute Report GRI-95/0496.
  31. Alfred, D.; Vernik, L. (2013). "A new petrophysical model for organic shales". Petrophysics. 54 (3): 240–247.
  32. Craddock, P. R.; et al. (2018). "Matrix-adjusted shale porosity measured in horizontal wells". Petrophysics. 59 (3): 288–307. doi:10.30632/PJV59N3-2018a1.
  33. Yang, J.; et al. (2017). "Nanoscale geochemical and geomechanical characterization of organic matter in shale". Nature Communications. 8 (1): 2179. Bibcode:2017NatCo...8.2179Y. doi:10.1038/s41467-017-02254-0. PMC 5736702. PMID 29259150.
  34. Example of a Van Krevelen diagram.
  35. Tissot, B. P.; Welte, D. H. (1984). Petroleum Formation and Occurrence. doi:10.1007/978-3-642-87813-8. ISBN 978-3-642-87815-2.
  36. Krause F. F., 2009.
  37. Weber G., Green J. (1981) Guide to oil shale. NationalConference of State Legislatures. Washington D.C. USA. p. 21.
  38. Galy, Valier; Peucker-Ehrenbrink, Bernhard; Eglinton, Timothy (2015). "Global carbon export from the terrestrial biosphere controlled by erosion". Nature. 521 (7551): 204–207. Bibcode:2015Natur.521..204G. doi:10.1038/nature14400. PMID 25971513. S2CID 205243485.
  39. Hedges, J. I.; Oades, J. M. (1997). "Comparative organic geochemistries of soils and marine sediments". Organic Geochemistry. 27 (7–8): 319–361. doi:10.1016/S0146-6380(97)00056-9.
  40. Nakamura, T. (2005) "Post-hydration thermal metamorphism of carbonaceous chondrites", Journal of Mineralogical and Petrological Sciences, volume 100, page 268, (PDF) Retrieved 1 September 2007
  41. Papoular, R. (2001) "The use of kerogen data in understanding the properties and evolution of interstellar carbonaceous dust", Astronomy and Astrophysics, volume 378, pages 597–607, Archived 27 September 2007 at the Wayback Machine (PDF) Retrieved 1 September 2007
  42. "Ancient organic molecules found on Mars". C&E News. 7 June 2018.
  43. Brown, Dwayne; Wendel, JoAnna; Steigerwald, Bill; Jones, Nancy; Good, Andrew (7 June 2018). "Release 18-050 – NASA Finds Ancient Organic Material, Mysterious Methane on Mars". NASA. Retrieved 7 June 2018.
  44. Archived at Ghostarchive and the Wayback Machine: NASA (7 June 2018). "Ancient Organics Discovered on Mars – video (03:17)". NASA. Retrieved 7 June 2018.
  45. Wall, Mike (7 June 2018). "Curiosity Rover Finds Ancient 'Building Blocks for Life' on Mars". Space.com. Retrieved 7 June 2018.
  46. Chang, K. (7 June 2018). "Life on Mars? Rover's Latest Discovery Puts It 'On the Table' – The identification of organic molecules in rocks on the red planet does not necessarily point to life there, past or present, but does indicate that some of the building blocks were present". The New York Times. Retrieved 8 June 2018.
  47. Voosen, Paul (7 June 2018). "NASA rover hits organic pay dirt on Mars". Science. doi:10.1126/science.aau3992. S2CID 115442477. Retrieved 7 June 2018.
  48. ten Kate, Inge Loes (8 June 2018). "Organic molecules on Mars". Science. 360 (6393): 1068–1069. Bibcode:2018Sci...360.1068T. doi:10.1126/science.aat2662. PMID 29880670. S2CID 46952468.
  49. Webster, Christopher R.; et al. (8 June 2018). "Background levels of methane in Mars' atmosphere show strong seasonal variations". Science. 360 (6393): 1093–1096. Bibcode:2018Sci...360.1093W. doi:10.1126/science.aaq0131. PMID 29880682.
  50. Eigenbrode, J.L.; et al. (8 June 2018). "Organic matter preserved in 3-billion-year-old mudstones at Gale crater, Mars". Science. 360 (6393): 1096–1101. Bibcode:2018Sci...360.1096E. doi:10.1126/science.aas9185. PMID 29880683.

Helgeson, H.C.et al. (2009). "A chemical and thermodynamic model of oil generation in hydrocarbon source rocks". Geochim. Cosmochim. Acta. 73, 594–695.[1]

Marakushev, S.A.; Belonogova, O.V. (2021), "An inorganic origin of the “oil-source” rocks carbon substance". Georesursy = Georesources. 23, 164–176.[2]

  1. Helgeson, Harold C.; Richard, Laurent; McKenzie, William F.; Norton, Denis L.; Schmitt, Alexandra (2009). "A chemical and thermodynamic model of oil generation in hydrocarbon source rocks". Geochimica et Cosmochimica Acta. 73 (3): 594–695. Bibcode:2009GeCoA..73..594H. doi:10.1016/j.gca.2008.03.004.
  2. 164–176. https://doi.org/10.18599/grs.2021.3.19
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