Metasedimentary rocks from Isua, West Greenland (over 3,700 million years old) contain 13C-depleted carbonaceous compounds, with isotopic ratios that are compatible with a biogenic origin1,2,3. Metamorphic garnet crystals in these rocks contain trails of carbonaceous inclusions that are contiguous with carbon-rich sedimentary beds in the host rock, where carbon is fully graphitized. Previous studies4,5 have not been able to document other elements of life (mainly hydrogen, oxygen, nitrogen and phosphorus) structurally bound to this carbonaceous material. Here we study carbonaceous inclusions armoured within garnet porphyroblasts, by in situ infrared absorption on approximately 10−21 m3 domains within these inclusions. We show that the absorption spectra are consistent with carbon bonded to nitrogen and oxygen, and probably also to phosphate. The levels of C–H or O–H bonds were found to be low. These results are consistent with biogenic organic material isolated for billions of years and thermally matured at temperatures of around 500 °C. They therefore provide spatial characterization for potentially the oldest biogenic carbon relics in Earth’s geological record. The preservation of Eoarchean organic residues within sedimentary material corroborates earlier claims2,6 for the biogenic origins of carbon in Isua metasediments.
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The research was supported by the Danish National Research Foundation (DNRF; fund number DNRF53) to Nordic Center for Earth Evolution. The research was supported by the NanoGeoScience group. We are grateful to E. Mathez, S. L. S. Stipp, J. Generosi and K. Bechgaard for inspiring discussions and J. Andersen for establishing contact. We also wish to thank D. Buti for assistance with the Raman spectroscopy.
The authors declare no competing financial interests.
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Extended data figures and tables
a, Geological map of the Isua Supracrustal Belt (ISB) in West Greenland. The samples were extracted from the area framed by the black rectangle. b, Bouma sequence alternating pelagic shales and turbiditic psamites. The iron-rich lithologies of this study have been sampled at approximately 4 m along strike from this outcrop from the bottom (left-hand) part of the sequence. c, MgO/FeO (wt%) ratio along a traverse across a garnet porphyroblast. This profile and the MnO profile in d are consistent with a single garnet growth event during prograde metamorphic heating. d, MnO (wt%) along a traverse across a garnet porphyroblast, showing a typical bell curve. The values along the x axis represent sequential automated EMP analytical points separated by 10 μm. Points intersecting inclusions and not representing pure garnet have been replaced by the average of the garnet values on either side. e, Table showing the stable isotopic composition of reduced carbon from inclusion bearing garnets (GNT 1–4) and two bulk rock samples of the garnet–biotite–epidote schist samples (030048 1–4 and 460531 1–4). The total reduced carbon (TOC) values found in the samples are given in relative numbers in column 2. The garnets and therefore all inclusions examined in this study were from the 030048 samples. Data obtained by Service d’Analyse des Roches et des Mineraux, CNRS, CRPG, Université de Lorraine.
a, These inclusions were imaged immediately after the garnets were opened and contain what appears to be liquid (white arrows indicate some examples). b, Inclusions containing more solid material.
a–c, Optical (a), SEM (b) and EDXS (c) intensity maps for carbon for the inclusion shown in Fig. 3. The white frames in b and c indicate the outline of AFM images shown in Fig. 3. EDXS is not surface-sensitive so thin layers of carbonaceous material will be dwarfed by other phases in the EDXS map. Nevertheless, the EDXS map confirms that the dark spots observed in the SEM image are carbon-rich material. In the inclusion studied (Fig. 3), we can confirm that we have carbon-rich material consistent with our AFM-IR results.
(This is not the inclusion shown in Fig. 3.) a, b, Optical images of the freshly cleaved garnet surface with carbonaceous inclusions. The white frame in a marks the size and position of the image shown in b. The white frame in b indicates the approximate position and size of the AFM-IR deflection mode image (c) and the corresponding IR maps shown in e and f. d, IR absorption spectra from 900 to 2,235 cm−1 at 12 different spots where the positions of S1 to S9 are equally spaced along a line across the inclusion, while S10, S11 and S12 are inside the inclusion at random positions. e, f, A map of the intensity of absorption at 2,230 cm−1 (e) and a map of the intensity of absorption at 1,836 cm−1 (f) across the area shown in c. g, IR absorption spectra from 2,500 to 3,600 cm−1 at a central spot in the inclusion.
Spectra on inclusion shown in Extended Data Fig. 4 and mapping across a neighbouring inclusion. a, The outline of the map is marked by the black frame. b, The peak position of the G-band across the inclusion. The G-band is usually found at around 1,575 cm−1, but in our experiments, there was a downward offset in the position of approximately 10 cm−1 attributed to laser heating35. The shift in the G-band peak position to higher wavenumbers is usually attributed to an increase in carrier concentration36; here, the higher value for the G-band on the rim suggests that the graphite contains other components, increasing in concentration towards the rim. We observe a 10 cm−1 shift between the centre and the rim of the inclusion, which is consistent with a 5–10 cm−1 upward shift in the G-band observed in graphite that has been functionalized with oxygen and nitrogen37. c, Map of the variation in the ratio between the D-band and G-band intensity. It varies between 0.13 (ratio for the peaks shown above) and 0.24. This corresponds to crystal size around 15 nm on average along the direction of the graphite plane11, and according to the RSCM thermometer method25 this corresponds to a peak metamorphic temperature of up to 600 °C. d, Raman spectroscopy of the inclusion studied by AFM-IR at the position marked by red arrow in the optical picture in a. The three distinct bands characteristic for graphite (G-band), D-band and 2D-band (arrows with values) are visible in the spectrum. A second spectrum was recorded on the garnet surface at the position indicated by the blue arrow next to the inclusions. For this spectrum, no specific bands for graphite were visible. e, Peak position of the G-band along the cross-section marked in the map shown in b by a black bar. f, Cross-section of the D-band and G-band corresponding to the black bar marked in c.
Extended Data Figure 6 Raman spectroscopy of an unexposed micro-inclusion inside a garnet in a polished thin section.
a, b, A reflected light image (a) and a transmitted light image (b) of a garnet in thin section. The bands of carbonaceous material can be clearly observed as dark bands in the transmitted light image shown in b, but are less obvious in the reflected light image (a). The Raman-equipped microscope was focused a few micrometres below the surface at the red arrow, so that the Raman signal came mainly from the carbonaceous material below the surface. c, The Raman spectra from the encapsulated carbonaceous material (position indicated by the red arrow) is shown as the red plot, and a Raman spectra from the pure garnet at the surface of the thin section (position indicated by the blue arrow) is shown as the blue plot. The three distinct bands characteristic for the G-band, D-band and 2D-band (arrows with values) are visible in the spectrum from the inclusions. The position of the bands along with the ratio between the D-band and G-band match those found for the exposed inclusion shown in Extended Data Fig. 5. The Raman spectra obtained from the uncleaned surface of this polished thin section display organic contamination with the broad signal from 1,200 cm−1 to 1,600 cm−1 and again from 2,800 cm−1 to 3,000 cm−1 (C–H).
IR absorption spectra (in the range in which hydrogen-bond absorption would occur) from various spots in the inclusion shown in Fig. 3. a, The deflection mode AFM image (as in Fig. 3). b, AFM-IR absorption in the range from 2,500 to 3,600 cm−1 at four points inside the inclusion indicated in a with boxes of corresponding colour (red, green, purple and blue). C–H stretches have a strong adsorption between 2,850 and 3,100 cm−1, depending on whether the C–H bond is aliphatic (lower wavenumbers) or aromatic (higher wavenumbers) hydrocarbon. No such bands could be detected in our inclusions. Similarly, no evidence for O–H was observed. The pulsed laser power used here was the same as for the lower range 900–2,230 cm−1.
Extended Data Figure 8 AFM-IR on kerogen on a grain of sand from a core plug extracted from an oil reservoir.
a, An AFM topography image on part of the sand grain surface. In the right part of the image, a 1 × 1 μm2 square part of the surface was scraped clean of kerogen by applying high force (GPa) with the AFM tip while scanning the area. This causes a build-up of kerogen around the cleaned area. A height profile (the blue line in a) across the surface and into the scraped area is shown in b). Using the same settings for the AFM-IR and the same type of tip as used on the inclusions we recorded three spectra shown in c from 2,500 to 3,600 cm−1. The positions at which we recorded these spectra are marked with blue, red and green boxes in a, with the corresponding arrows in b. The position marked by green was inside the scraped area. The kerogen is only a few nanometres thick and the C–H absorption is therefore very low, but barely detectable. At the blue and red positions the kerogen is 20–40 nm thick and the absorption for the C–H and O–H stretch can be clearly detected. The laser power in the AFM-IR was the same as used for the inclusions.
a, The AFM image (deflection mode) inside the inclusion a few hours after the inclusion was opened. b, The same area after analysis in the SEM. c, The height profile along the blue and red lines shown in a and b across the internal part of the inclusion. The difference between the blue and red lines shows up to 500 nm thick material was lost because of beam damage during the analysis in the SEM.
a–c, Molecular modelling of the free energy for transforming the dipeptide dileucine (a) into an aromatic amine (blue) (b) and an aromatic nitrile (red) (c). d, The modelling predicts that the free energy for the reactions favour formation of aromatic groups and loss of hydrogen and water above approximately 250 °C. On the basis of the calculated reaction free energy, the nitrile is favoured above 700 °C, while the amine is favoured between 250 and 700 °C. If hydrogen is removed from the inclusion via diffusion into the surrounding garnet, the shift in equilibrium can still lead to nitrile formation instead of amines, even at temperatures below 700 °C, as discussed in the main text and Supplementary Information.
This file contains information on geological context broken down into protolith, age, metamorphism, and deformation and also includes an analysis of the molecular modelling. The file also contains supplementary table 3 which shows the IR absorption assignment. (PDF 236 kb)
This file contains supplementary table 1 which shows the major elements in the metasedimentary rock. The inclusions studied are from 30048. (XLSX 33 kb)
This file contains supplementary table 2 which shows composition data in biotite and garnets at various positions close to the inclusions studied. Also shown is the estimated temperature using a calibration by Ferry and Spear. (XLSX 48 kb)
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Hassenkam, T., Andersson, M., Dalby, K. et al. Elements of Eoarchean life trapped in mineral inclusions. Nature 548, 78–81 (2017). https://doi.org/10.1038/nature23261
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