Global hydrogen reservoirs in basement and basins
© The Author(s) 2017
Received: 12 January 2017
Accepted: 14 March 2017
Published: 20 March 2017
Hydrogen is known to occur in the groundwaters of some ancient cratons. Where associated gases have been dated, their age extends up to a billion years, and the hydrogen is assumed also to be very old. These observations are interpreted to represent the radiolysis of water and hydration reactions and migration of hydrogen into fracture systems. A hitherto untested implication is that the overwhelming bulk of the ancient low-permeability basement, which is not adjacent to cross-cutting fractures, constitutes a reservoir for hydrogen.
New data obtained from cold crushing to liberate volatiles from fluid inclusions confirm that granites and gneiss of Archean and Palaeoproterozoic (>1600 Ma) age typically contain an order of magnitude greater hydrogen in their entrained fluid than very young (<200 Ma) granites. Sedimentary rocks containing clasts of old basement also include a greater proportion of hydrogen than the young granites.
The data support the case for a global reservoir of hydrogen in both the ancient basement and in the extensive derived sediments. These reservoirs are susceptible to the release of hydrogen through a variety of mechanisms, including deformation, attrition to reduce grain size and diagenetic alteration, thereby contributing to the hydrogen required by chemolithoautotrophs in the deep biosphere.
Measurements of groundwaters in Precambrian cratons show that they consistently contain hydrogen (data reviewed in [1–3]). The hydrogen is attributed to the long-term radiolysis of water due to natural radioactivity  and hydration reactions, including serpentinization and oxidation of ferrous iron . Evidence from noble gas composition shows that gases may have been trapped in the crust for up to a billion years [5–7], and although hydrogen is not dated directly, longevity is implied by the association with dated gases , and the genetic link between radiolysis and dated radiogenic helium.
The measurement of hydrogen has focussed on crystalline basement, rather than in sedimentary basins. Yet sedimentary basins are dominated by siliciclastic sediment, that sediment is dominated by the mineral quartz, and most quartz is derived from granites. More generally, siliciclastic sediment ultimately has a basement source, albeit recycled through phases of sedimentary deposition and erosion. An implication of the derivation from crystalline basement is that a signature of hydrogen in the basement could be conferred to the sediment. The ultimate provenance of sediment is evident from the dating of detrital zircon grains. Both modern sand, and sandstone in the geological record, contains a substantial proportion of grains derived from basement sources of early-mid Proterozoic age [8, 9]. This reflects an episode of anomalous crustal growth with globally extensive granite emplacement [10, 11]. We therefore might expect the sediment to carry the heritage of the hydrogen-rich Precambrian basement. A significant proportion of the hydrogen generated by radiolysis in basement rocks, possibly two-thirds , is resident in fluid inclusions, and these inclusions survive in the derived sediment particles.
If the hydrogen occurs widely in the entrapped fluid in old basement rocks, as implied by the gas released from Precambrian cratons.
If the importance of age can be demonstrated by comparison with data in young basement rocks.
If hydrogen also occurs in the derived sediment, as we predict here.
Most water in granitic basement is in post-magmatic secondary fluid inclusions, with only a comparatively minor component originating from the granite melt and forming glassy melt inclusions or rare primary aqueous fluid inclusions . The secondary aqueous fluid inclusions in granites represent hydrothermal fluid from a range of origins, including fractionation of the original melt, convection systems driven by the hot magma, and later fluids focussed on the granite because it has become a structural/topographic high [16, 17]. The entrapped fluid in granitic basement is, therefore, a good record of its post-emplacement history.
The cold crush method involves analysis by mass spectrometry conducted in high vacuum as described in [12–14]. Each session was preceded and followed by analysis of one microlitre capillary tubes for calibration. Atmosphere was also introduced to verify the calibration using 100–200 acquisitions for both the sample and atmosphere standard. A match head sized sample (about 250 microns) is crushed incrementally under a vacuum of ~10−8 Torr, producing 6–10 successive bursts, which remained in the vacuum chamber for 8–10 analyser scans (~2 s) before removal by the vacuum pump. This method does not require a carrier gas and volatiles are not separated from each other but released simultaneously into the chamber. The act of incremental crushing may open a single inclusion or multiple fluid inclusions. The data acquisition is performed by means of two Pfeiffer Prisma quadrupole mass spectrometers operating in fast-scan, peak-hopping mode. Routinely the system analyzes for the following gaseous species including H2, He, CH4, H2O, N2, O2, Ar, and CO2. The volatiles are reported in mol%. The instrument is calibrated using Scott Gas Mini-mix gas mixtures (with 2% uncertainty), capillary tubes filled with gas mixtures (with 1% uncertainty), and three in-house fluid inclusion gas standards. The amount of each species is calculated by matrix multiplication  to provide a quantitative analysis. The 2-sigma detection limit for most inorganic species is about 0.2 ppm for aqueous fluid inclusions. Instrumental blanks were also analyzed routinely to assess if gases were produced during the crushing process. The mass spectra remained at background during crushing of blanks indicating that gases released are not sourced from the crushers or hardware. Linearity of the mass spectrometer was confirmed up to nitrogen partial pressures of 10−6 Torr, which is orders of magnitude higher than routine operating pressures. The error across the linear range of the mass spectrometer is estimated from the standard deviation for capillary tube measurements of the N2/Ar ratio. This covers the noise and the area under the peak curve. The measurements indicate a maximum error of 1%. Precision and accuracy vary between species. The amount of each species was calculated by matrix methods to provide a quantitative analysis, which is corrected for the instrumental background. Nine capillary tubes with encapsulated atmosphere were analyzed and yielded N2/Ar ratios of 83.2 with a standard deviation of 1.4, within error of the atmospheric N2/Ar ratio of 83.6. This translates into 0.5% accuracy for artificial inclusions made under laboratory conditions. Precision using natural inclusions for the major gas species measured is generally 2–5%, these being dependent on summed errors derived from instrument noise, linearity of the mass spectrometer, uncertainty of standards, blanks, interferences, and measurement of sensitivity factors. Before analysis, the crushing area and the bellows of the crusher were cleaned using potassium hydroxide. The apparatus is also routinely cleaned with isopropanol. Thereafter, the crushing chamber is baked at about 150–200 °C for 72 h before loading and analysing the samples at room temperature the next day. The crushing area is isolated from the main chamber so that the main chamber can be baked out every evening.
The hydrogen data is converted to the proportion of the non-aqueous component, to avoid misleading inferences from variations in the abundance of aqueous fluid inclusions, which dominate the entrained fluid.
Contents of H2, He, and mols of gas measured in samples of old and young basement, and sediments with old and young provenance
H2 (% non-water)
JP210 Devon Is
1.4 * −09
JP212 White Sea, Karelia
6.1 * −10
JP219 Chiobino, Karelia
6.4 * −11
3.3 * −10
JP201 South Harris gneiss
1.9 * −10
JP147 Creighton, Sudbury
5.4 * −11
JP177 North Uist gneiss
3.1 * −11
JP92 Devon Is
2.5 * −09
5.7 * −10
JP139 Moeda Fm
5.5 * −10
3.1 * −10
9293 Shaw batholith (Aus)
9.3 * −11
9299 Mt Edgar batholith (Aus)
8.3 * −11
9298 Swaziland Ngwane gneiss
1.2 * −10
9300 MSC105 Acasta TTG
1.7 * −10
9301 MSC110 Acasta TTG
3.0 * −10
JP221 Gawler Craton (Aus)
2.0 * −10
JP224 Cullen (Aus)
3.0 * −10
JP233 Bass Lake Ontario
1.8 * −10
KV3 Kaap Valley pluton SA
8.4 * −11
JP236 Rhinns Complex
1.1 * −10
JP246 Nuuk, Greenland
1.1 * −10
JP249 Gairloch Pier
2.4 * −10
JP262 Nanortalik, Greenland
1.4 * −10
KCL19 Liangchen, N China
7.1 * −11
7.1 * −10
2.9 * −10
1.5 * −10
1.4 * −10
3.7 * −10
2.0 * −09
6.8 * −09
1.1 * −10
3.1 * −10
9292 Chuqui, Chile
5.1 * −10
9305 New Mexico Sugar Loaf
6.7 * −11
1.3 * −10
4.9 * −11
8.2 * −11
3.0 * −10
1.1 * −10
NB New Mexico Questa
1.7 * −10
9291 El Abra Chile
Granodiorite (U minztn)
2.3 * −10
Sediments with old provenance
JP247 Gairloch Pier
2.6 * −10
1.6 * −10
2.4 * −10
Sediments with young provenance
JP242A Red Cuillin, Skye
5.8 * −11
JP244 Bloody Bridge
3.9 * −10
JP245 Glen Sannox
4.4 * −09
The database confirms previous theory [1, 2] that there is a global reservoir of hydrogen in crystalline basement and clarifies that it is resident particularly in old basement. The greater concentrations of hydrogen in the older rocks can be explained by the greater accumulated radioactivity, and hence radiolysis. A major proportion of the radioactivity is from potassium. In a coarse-grained rock like granite, beta-irradiation from potassium is more likely to penetrate beyond grain boundaries into intergranular fluid than shorter-range alpha irradiation from uranium, and potassium is also more pervasively distributed than the uranium in granite, so contributes more widely to radiolysis. Potassium is as abundant in the young basement as it is in the Precambrian basement (Fig. 2), showing that it is age rather than composition that is the control on hydrogen content. The hydrogen contents measured in modern sediments show that the gas signature of the basement rocks is conferred to the derived clasts. The more hydrogen-rich Precambrian basement is reflected in greater hydrogen contents in sediment derived from Precambrian basement than in sediment derived from Cenozoic basement. There are other mineral alteration mechanisms by which hydrogen can be generated in sediments on relatively short time scales (e.g. ), but the correlation of sediment provenance with hydrogen content shows that radiolysis is a major contributor.
The hydrogen entrained in basement and derived sediment is available for release by a variety of mechanisms, including solid state diffusion, strain deformation, fault movement and a range of surface erosion processes such as glacial grinding. Many of these mechanisms would involve decrepitation of the fluid inclusions, as is widely observed . The availability of hydrogen in the subsurface in particular is important as a potential fuel for a deep biosphere [3, 21, 22]. Hydrogen may be the predominant source of energy for microbial activity in the subsurface, with a record back to the earliest life on Earth .
The signatures in old sediments will be a mixture of hydrogen generated in the provenance basement, and hydrogen generated by radiolysis since sediment deposition. As long as there is still a source of radioactivity, including potassium, radiolysis will continue, especially in fine-grained sediments where a greater proportion of the shorter range alpha irradiation may interact with pore waters . This is conspicuously evident in the Oklo uranium deposits, Gabon, where fluid inclusions in sandstone contain discrete oxygen and hydrogen generated by radiolysis [25, 26]. Where basement and derived sediment must differ in hydrogen generation is in the case of mineralogically mature sands consisting almost exclusively of quartz, where the potassium-bearing phases (especially feldspars) have been eliminated and the potassium becomes concentrated in clay/silt-sized minerals that are deposited under different hydrodynamic conditions. However the quartz may still retain hydrogen generated from adjacent mineral phases before basement and sediment erosion.
The availability of hydrogen in sedimentary basins may be as relevant, if not more so, to supporting a subsurface biosphere, than the availability of hydrogen in the parent basement. In contrast to basement rocks, in which deformation is episodic and spatially focussed, deformation in compacting basins proceeds relatively continuously and widely. Microfractures develop in compacting sands, even before they are fully lithified, and are rapidly re-healed as micron-scale planes containing entrapped fluid, extensively evident in cathodoluminescence images [27, 28]. However, there is evidence for low level availability of hydrogen in shallow sediment, where it is oxidized by microbes, but it is assumed that the hydrogen they process is derived from overlying atmosphere [29, 30]. Microbes also utilize hydrogen where it is available from deep sediment  and subsurface crystalline sources, especially through interaction of Fe(II) and water [4, 32–34]. These communities show that where hydrogen is available it is likely to be utilized and this will include hydrogen released from reservoirs in sedimentary rocks.
There is an implication for other rocky planets, which may similarly contain a subsurface reservoir of hydrogen derived from radiolysis, and thereby could support subsurface life. Notably, such life would not require surface water, and so would not be constrained by the ‘Goldilocks Zone’ commonly used to define the limits of habitability .
Precambrian basement consistently contains entrained hydrogen, at levels an order of magnitude greater than in young (<200 Ma) basement.
Modern sediment derived from old and young basement retains the signature of more or less hydrogen, respectively.
The high proportion of particles of early-mid Proterozoic age in modern sediments implies that relatively high levels of entrained hydrogen are held in much of that sediment.
These data show that reservoirs of hydrogen occur in both basement and sediment, available to support subsurface microbial activity.
JP instigated the project. NB undertook the measurements. Both authors prepared the final manuscript. Both authors read and approved the final manuscript.
The authors are grateful to the Science and Technology Facilities Council (STFC) for funding, through Grant NE/G00322X/1. Samples were kindly contributed by K. Condie, M.J. Hole, and D. Muirhead. We are grateful to reviewers for their criticism.
The authors declare that they have no competing interests.
Availability of data and materials
The datasets supporting the conclusions of this article are included within the article. Data are also available from Dr. Nigel Blamey (email@example.com).
Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The Creative Commons Public Domain Dedication waiver (http://creativecommons.org/publicdomain/zero/1.0/) applies to the data made available in this article, unless otherwise stated.
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