Article | Open

Charcoal evidence that rising atmospheric oxygen terminated Early Jurassic ocean anoxia

  • Nature Communications 8, Article number: 15018 (2017)
  • doi:10.1038/ncomms15018
  • Download Citation
Received:
Accepted:
Published online:

Abstract

The Toarcian Oceanic Anoxic Event (T-OAE) was characterized by a major disturbance to the global carbon(C)-cycle, and depleted oxygen in Earth’s oceans resulting in marine mass extinction. Numerical models predict that increased organic carbon burial should drive a rise in atmospheric oxygen (pO2) leading to termination of an OAE after 1 Myr. Wildfire is highly responsive to changes in pO2 implying that fire-activity should vary across OAEs. Here we test this hypothesis by tracing variations in the abundance of fossil charcoal across the T-OAE. We report a sustained 800 kyr enhancement of fire-activity beginning 1 Myr after the onset of the T-OAE and peaking during its termination. This major enhancement of fire occurred across the timescale of predicted pO2 variations, and we argue this was primarily driven by increased pO2. Our study provides the first fossil-based evidence suggesting that fire-feedbacks to rising pO2 may have aided in terminating the T-OAE.

Introduction

It has been suggested that projections of anthropogenic C-emissions likely exceed levels that have initiated Oceanic Anoxic Events (OAEs) in Earth’s past1,2, implying that anthropogenic forcing of the Earth System may cause a future OAE, with implications for food security and for the oceans as a net C sink. OAEs are identified in the rock record by globally traceable organic-rich sediments and excursions within the δ13C record3,4, representing periods of major disturbance to the global C-cycle4. The study of OAEs therefore provides a geological test bed for understanding the functioning of global biogeochemical cycles under extreme conditions and rapid shifts in C-emissions.

Burial of organic carbon (C(org)) and reduced sulfur (pyrite) burial generate long-term build-up of oxygen to Earth’s atmosphere5,6,7,8,9,10. It has thus been predicted that during an OAE, where increased burial of Corg and pyrite11 occur, that pO2 concentrations should have risen12 (Fig. 1). Wildfire responds strongly to pO2 (refs 13, 14, 15) and has been implicated in providing an essential long-term negative feedback, counteracting rising pO2 throughout geological time (for example, see refs 5, 12, 16). We therefore hypothesize that fire-activity should track projected pO2 changes across an OAE (Fig. 1).

Figure 1: Summary of published data collected across the early Toarcian oceanic anoxic event.
Figure 1

(a) Carbonate carbon isotope profile from Peniche and the organic carbon isotope profile from Yorkshire illustrating the step-wise nature of the negative excursion, and postulated pulses of light carbon release from Kemp et al.25 Plotted alongside are the osmium isotope profile from Mochras and total organic carbon content from the Yorkshire section. (b) Handoh and Lenton’s12 hypothesized model changes in atmospheric oxygen and wildfire frequency across an oceanic anoxic event, with period of modelled peak oxygen and wildfire frequency highlighted.

Variation in the occurrence and abundance of charcoal throughout Earth history is taken to represent changes in fire-activity and appears to correlate with broad trends in the abundance of pO2 (refs 13, 17). A few studies have looked at the fossil-charcoal record within Devonian marine black shales and related them to changes in pO2 and fire-feedbacks18,19. However, fossil charcoal has not been studied across events such as OAEs in order to test the hypothesis that fire-feedbacks to pO2 may have acted together to rebalance the Earth system during these events9,12. Here we test this hypothesis by assessing the charcoal content of sediments from two sites deposited in the southern Laurasian Seaway, at Mochras in Wales, UK and Peniche, Portugal.

In this study, we find that charcoal abundances and therefore inferred wildfire-activity at both study locations are enhanced 1 Myr after the onset of the T-OAE. The enhancement of fire-activity is sustained for 800 kyr and peaks during the OAE termination. Variations in pO2 are anticipated to occur over Myr timescales6,16,20 due to the long residence time of oxygen within the ocean-atmosphere system12,20. The major enhancement of fire-activity occurring 1 Myr after the start of the T-OAE and lasting over 800 kyr is strikingly similar to the Myr timescale required for predicted global pO2 variations. Our findings therefore provide the first fossil-based evidence to support the postulation that OAEs are terminated by a rise in pO2 levels.

Results

Palaeo-wildfire

We find background charcoal abundances range between 22,000 and 75,000 particles per 10 g rock at Mochras, and 37,000 and 122,000 at Peniche prior to the T-OAE. Charcoal abundance rises briefly above background levels during the onset of the T-OAE, evidenced by 950,000 particles at Peniche (10.4 m log height) and 133,000 at Mochras (842 m depth), the start of which is widely identified in the rock record by a shift towards negative δ13C values at the culmination of a positive δ13C trend3 (Fig. 2). Charcoal abundances then decline to background values during the period of the negative carbon isotope excursion (CIE). Abundances remain at/below background levels until the final stages of the OAE (22.4 m at Peniche and 809 m at Mochras), where abundances increase to 293,000 particles at Peniche and 350,000 at Mochras. Although there appears to be variability within the charcoal abundance data, at both study locations abundances remain above background levels for 9.6 m at Peniche (between log heights 22.4 m and 32 m); and 23 m at Mochras (between core depths 809 m and 786 m), with the exception of one point at 803 m at Mochras, where abundances decline to 45,000 particles per 10 g of rock. Once the T-OAE has terminated, identified by the δ13C values returning to towards pre-excursion levels, abundances return to background levels as evidenced at Peniche from a mean of 411,000 particles between log heights 22.20 m and 32 m to a mean of 62,000 particles between 32 m and 38.2 m; and at Mochras from a mean charcoal abundance of 307,000 particles between core depths 809–786 m to a mean of 113,000 particles between depths of 785 m and 771 m.

Figure 2: Charcoal and Phytoclast abundances across the T-OAE.
Figure 2

Charcoal and phytoclast data collected in this study, plotted against published wood and carbonate carbon isotope profiles from Peniche and Mochras, and calculated cyclostratigraphic timescale from the Peniche section by ref. 24, 24. δ13Cwood and δ13Ccarb profiles for Peniche are from ref. 3. The δ13C carb for Mochras is from ref. 51 and correlated to the Peniche sequence using ref. 28.

Palynofacies

The reported variations in charcoal abundance do not appear to be an artefact of preservation or changes in terrestrial organic delivery across the OAE, because variations in preserved phytoclasts (comprising terrestrial vegetal matter including charcoal, plant cuticles, pollen and spores and coalified material), show little correlation with the variations in charcoal abundance at either site (Fig. 2). This is further statistically supported by higher than 0.05 P values of P=0.384 for the Mochras section (where Pearsons R equalled −0.0186), and P=0.195 for Peniche (where R equalled −0.2153), indicating that the correlation between charcoal abundance and phytoclast abundance throughout the sections is not significant.

Discussion

Fluctuations in the abundance of terrestrial phytoclasts have been used to indicate shifts in proximal palaeo-shoreline distance from the depositional site, as well as changes in preservation, for example, due to a switch from anoxic to an oxic environment21. At Mochras, the depositional site is anticipated to have gradually deepened, beginning at the OAE initiation and continuing throughout the falciferum ammonite zone into the bifrons ammonite zone beyond the studied section22. Interestingly, phytoclast abundances do not appear to reflect this deepening trend, suggesting that the site may have continued to experience a similar influx of terrestrial material throughout the OAE and beyond. Therefore this deepening is unlikely to explain enhanced charcoal abundance towards the end of the OAE; if anything deepening might be expected to decrease the amount of charcoal reaching the depositional environment at this site. Furthermore the lack of correspondence between variations in phytoclast abundance and charcoal abundance, implies that the enhanced number of fossil-charcoal particles that occur during the final stages of the OAE are unlikely to be due to a change in organic preservation, and therefore most likely reflect a real change in fire-activity. The charcoal is further unlikely to have been reworked up-section as there is no evidence of reworking in the biostratigraphic record of the sites, nor evidence for enhanced bioturbation at the onset of this phase of the OAE. Because charcoal abundance is limited below this point, reworking of the older sediments appears an unlikely source for the abundant charcoal that appears in the final phases of the OAE.

Published astronomically calibrated timescales for the Peniche section23,24, estimate a total duration of between 900 kyrs and 1.7 Myrs for the T-OAE, respectively. These timescales have previously been compared and correlated with Toarcian sediments exposed in Yorkshire, UK, which also illustrates a strong astronomical forcing within the δ13Corg record25. The section we have studied at Mochras provides twice the thickness and is considered to be stratigraphically more complete than that exposed in Yorkshire26,27. For the purpose of this study, we have used the most up-to-date published correlation of the Peniche and Mochras section,28 plotted alongside the most up-to-date published cyclostratigraphically calibrated timescale from the Peniche section24.

Using the published timescale, we estimate that background charcoal abundances persisted for the duration of 600 kyrs (ref. 24) prior to the initiation of the OAE. The sustained increase in charcoal abundances at 22.4 m at Peniche and 809 m at Mochras, occurs at an estimated 1 Myrs after the OAE onset (Fig. 2), remaining elevated for an estimated 800 kyrs–1 Myrs before declining towards background abundances after the OAE termination. The major change in inferred wildfire-activity estimated at 1 Myrs after the OAE onset appears to corroborate the hypothesis of Handoh and Lenton12, suggesting that a rise in pO2 may have assisted in terminating the T-OAE by ventilating the ocean. However, while Handoh and Lenton12 predict that pO2 and thus fire-activity should be at a minimum at the start of the OAE and gradually rise throughout (Fig. 1), our analysis reveals a brief rise in fire-activity during the T-OAE initiation at both study sites, although albeit a much smaller rise in abundances at the Mochras site. Calculation of the Z scores for this brief rise in charcoal abundances (Z=10.43 at Peniche and Z=3.39 at Mochras) indicates that this increase in charcoal abundance at the onset, is statistically significant (larger than the critical Z value of 1.645) when compared to the background counts at both study sites. While, this observation is based on only one data-point in each section and requires corroboration, the brief rise in charcoal abundance occurs at the culmination of a positive δ13C trend. This could imply that the positive δ13C trend is indicative of an earlier prolonged increase in C(org) burial, and therefore that pO2 began rising before the OAE.

Fire responses to rising pO2 are non-linear (see Fig. 4 in ref. 29); therefore, depending on the timing of the onset of C(org) burial and the abundance of pO2 prior to the OAE, the fire responses could be variable throughout the OAE29. The pO2 estimates for 183 Ma range between 16 and 21% (ref. 17). If background pO2 were 19%, and the onset of C(org) burial were capable of leading to a rapid 1% rise in pO2 by the start of the OAE, there would be a rapid rise in fire-activity as pO2 transitioned between 19 and 21% (ref. 29). Beyond 21% the fire response would slow but still continue to rise throughout the OAE with rising C(org) burial and pO2, reaching a peak towards the end. However, most models estimate baseline pO2 at 20% (refs 16, 30), which would generate a slower fire response at the onset of enhanced C(org) burial, with fire-activity gradually rising throughout and peaking at the end of the OAE. Therefore the initial peak in fire-activity would require a different explanation.

A study by McElwain et al.31 on a T-OAE section at Bornholm, Denmark, reveals that during the initiation, significant climatic changes occurred. Although, this sequence31 preserves only the lower part of the negative CIE, and was conducted at a higher resolution than that captured here, a rise in global temperatures and drying of the regional climate is inferred due to increased abundance of thermophilic plant taxa immediately before the first negative δ13C shift. Past Mesozoic global warming events have been shown to enhance fire activity15 and warm, dry periods are commonly linked with increased fire probability and large fire events32,33, which tend to be enhanced when dry periods succeed wetter periods that are favourable to fuel accumulation. Thus the brief enhancement of fire-activity may have been influenced by climatic changes occurring over timescales of a few hundred to thousand years close to the onset of the OAE; either driven directly by the climate change or from a resulting change in vegetation, the fuel for fires.

Following the brief rise in fire-activity, charcoal diminishes to near background levels, rather than rising gradually throughout the OAE. During the negative CIE, pulses of isotopically light C suggest enhanced input of CO2 into the atmosphere from volcanic sources25 leading to increased global temperatures34, sufficient to provoke methane (CH4)-hydrate dissociation3. This combined with an increase in terrestrial methanogenesis and a potential positive feedback associated with the decomposition of plant litter enabling further release of CO2 and CH4 from terrestrial sources (for example, refs 35, 36), thus created the large negative CIE and enhanced CH4 driven global warming. Coupled ocean-atmosphere models suggest an increase in global precipitation rates of +9 cm per year driven by the subsequent rises in CO2 (ref. 37). Increased continental weathering rates of up to 3 times larger than before the excursion38, have also been suggested based on a positive excursion in 187Os/188Os within the Jet Rock beds of Yorkshire and at Mochras38 (Fig. 1). These imply a warmer but wetter world; an expected feedback response to greenhouse induced warming31. Hence suppression of the rise in fire-activity throughout the negative CIE may be due to a significantly wetter climate, damping any pO2-fire response. Of significance however, is the ability of fire-activity to continue at background levels, which may indicate rising pO2 enabling fuels with higher moisture contents to continue to burn at a similar level to before the event13,14,15.

Towards the end of the T-OAE the δ13C record rises to more positive values again. At the same time, charcoal abundances at both sites increase, and remain elevated until the point of the T-OAE’s termination. This synchronous rise begins at an estimated 1 Myr (ref. 24) after the start of anoxia, with charcoal abundances remaining elevated for an inferred 800 kyr (ref. 24), before returning to near background values (Fig. 2).

Following the negative CIE, palaeoclimatic conditions are hypothesized to have gradually cooled and dried, continuing well beyond the point of the T-OAE termination34,39. Climatic drying will have likely aided any pO2 driven enhancement of fire-activity, removing the suppression of fire under the wetter conditions of the CIE. Importantly however, beyond the OAE termination, charcoal abundances no longer track the inferred climate changes and instead decline despite the hypothesized climate continuing to dry and cool. Instead, after an inferred 800 kyr (ref. 24) of enhanced fire-activity the system appears to return to near background functioning, evidenced by the decline in charcoal at Peniche between 33.2m and 38.2 m, and at Mochras between 785m and 771 m.

Variations in pO2 are anticipated to occur over Myr timescales6,16,20, due to the long residence time of oxygen within the ocean-atmosphere system12,20, which is set by the large reservoir of oxygen in the atmosphere,3.7 × 1019 mol (ref. 20), divided by the relatively small flux of oxygen from C(org) burial 18 × 1012 mol oxygen per year1,20 (and corresponding removal largely by oxidative weathering). The major enhancement of fire-activity for 800 kyr is strikingly similar to the Myr timescale required for hypothesized global pO2 reservoir variations12,20. In the model of Handoh and Lenton12, increased C(org) burial across the OAE should lead to a gradual rise in pO2 and an increase in fire-activity, which leads to suppression of vegetation and a decline in chemical weathering rate (particularly of phosphorous) towards the end of the OAE (ref. 12). The latter prediction appears to be supported by the rapidly declining 187Os/186Os towards the end of the T-OAE (refs 38, 40). Some Earth system models (for example, COPSE (ref. 30)) depend on the sensitivity of fires to pO2 and the impact that fires have on vegetation biomass16,30 to regulate pO2. Fire is estimated to suppress Earth's present day vegetation biomass by 50% (ref. 41) at pO2 21%, yet fire cannot be sustained (and therefore cannot suppress vegetation) below pO2 15–17% (ref. 13). Even a modest increase in pO2 driven by enhanced C(org) burial during the T-OAE, from, for example, the base level of pO2 (20%) estimated for the Jurassic16,30 to 21%, could have led to a 5% increase in burn probability due to the rapid response of fire to pO2 around this baseline level13. This in turn could have significantly enhanced the suppression of vegetation by fire16 by the end of the T-OAE. The resulting fire suppression of plant-driven phosphorus weathering may have assisted in terminating the T-OAE by reducing the input of phosphorus to the ocean and therefore productivity and oxygen demand in the water column. This effect would have combined with the direct effect of rising pO2 re-oxygenating the ocean and in turn causing phosphorus to be more efficiently removed to sediments12. Specifically, as the ocean starts to re-oxygenate this is predicted12 to increase the removal of phosphorus adsorbed to iron oxide minerals (Fe–P)42 and that preserved in organic matter (Org-P)43,44, lowering the ocean PO4 concentration and thus lowering oxygen demand in the water column—a strong positive feedback amplifying the re-oxygenation of the ocean. The data presented here provides the first fossil evidence that pO2 driven fire-feedbacks may have played a significant role in terminating ocean anoxia. We note that further work at additional study site(s) away from the Tethys region would be required to provide evidence that this fire response to rising pO2 was global in extent.

In conclusion, the observed increase in abundance of fossil charcoal, taken as a proxy for fire-activity occurring towards the end of the T-OAE is hypothesized to be primarily driven by increased pO2, providing the first fossil-based evidence to support the postulation that OAEs are terminated by a rise in pO2 levels. Thus the response of fire to Earth system perturbations across the T-OAE appears to capture a geologically rapid enhancement of pO2 implying that relatively small but significant changes in this key atmospheric gas may be possible over the timescale of an OAE. Such rapid C-cycle driven changes to pO2 suggest that new higher time-resolution models of pO2 over Earth's history may be required to explore the relationship between changes in C-cycling and Earth system functioning. This is critical because it appears that oxygen-fire feedbacks have the ability to regulate key processes that help re-oxygenate the ocean during perturbations to C-cycling and return the Earth system to background functioning. Given that the modern ocean is ‘on the edge of anoxia’12 and observations that the Earth system may take millions of years to regain background function if the ocean is tipped into an anoxic state, it will be critical to manage anthropogenic disruption to the C-cycle and maintain the natural functioning of wildfire-activity in order to regulate the Earth system within habitable bounds.

Methods

Study locations

Two sites were studied that record the T-OAE, deposited within the southern Laurasian Seaway; Peniche in Portugal and Mochras in the UK (Fig. 3). At Peniche, the Pliensbachian-Toarcian carbonate ramp succession is particularly well exposed, including the Toarcian GSSP (for example, see ref. 45). The deepest part of the ramp (200 m), represented by the Praia do Abalo sample locality, was bounded by the high-relief Berlenga–Farilhões horst, which provided terrestrial material to the sample site46. The site is unlikely to be influenced by a rise in sea level, as the horst would not have become more distal from the depositional area3. In Wales, UK, the Llanbedr (Mochras Farm) core, referred to as Mochras, drilled in 1967–1969, provides a complete section of mostly Early Jurassic sediments dating from the Late Rhaetian to Late Toarcian47,48. The sediments were deposited within a basinal marine setting, which became deeper during the initiation of the OAE, continuing throughout the falciferum zone into the bifrons zone (beyond the studied section)22 influenced by nearby terrigenous sources around the Cardigan Bay area48. Both sites are within the Laurasian Seaway (see Hesselbo and Pieńkowski49 and references therein), and are anticipated to capture regional signals of burning from the nearby emergent land.

Figure 3: Jurassic Palaeo-map of the sample localities and relative site stratigraphies for the Mochras and Peniche sections.
Figure 3

Palaeo-map and Peniche log were edited from ref. 3. Mochras log edited from ref. 26

Sample collection and processing

Rock samples were collected from the exposed cliff sections in Peniche, and from the Mochras core, stored at British Geological Survey, Keyworth. The samples were picked from marl units, characterized by minor lithological changes and are considered to have been deposited within relatively uniform palaeoenvironments, minimizing the distortion of any fire-signals observed. Fossil charcoal was extracted from the Peniche and Mochras rock samples (48 samples in total were processed and analysed) using standard palynological acid maceration techniques. The remaining organic particles were sieved using a 125 μm mesh, where both size fractions were collected. The >125 μm size fractions were analysed using a binocular microscope, where all charcoal particles in each 20 g sample were quantified. The <125 μm fraction retained was quantified by evenly dispersing the organic particles in a known quantity of water. A known volume was then pipetted and made into slides using standard palynological techniques. Two transects of each slide were quantified, and scaled up to the known quantity of the <125 μm sample50. Selected particles were studied using a scanning electron microscope (SEM) to confirm their identification as charcoal (Fig. 4). To ensure changes in fossil charcoal concentrations were not biased by a change in nature or abundance of terrestrial organic material, a palynofacies analysis of each sample was conducted, quantifying the abundance of pollen and spores; plant cuticle, amorphous organic matter and coalified particles (Supplementary Data 1).

Figure 4: SEM images of charcoal fragments from the Peniche section.
Figure 4

The fragments show the preservation of cellular anatomy and fused/homogenized cell walls—a key feature in charcoal identification.

Data availability

All data generated and analysed in this study are included in this published article and its supplementary information file.

Additional information

How to cite this article: Baker, S. J. et al. Charcoal evidence that rising atmospheric oxygen terminated Early Jurassic ocean anoxia. Nat. Commun. 8, 15018 doi: 10.1038/ncomms15018 (2017).

Publisher’s note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

References

  1. 1.

    & The impact of climate change on the World’s marine ecosystems. Science 328, 1523–1528 (2010).

  2. 2.

    , & Carbon sequestration activated by a volcanic CO2 pulse during Ocean Anoxic Event 2. Nat. Geosci. 3, 205–208 (2010).

  3. 3.

    , , & Carbon-isotope record of the Early Jurassic (Toarcian) Oceanic Anoxic Event from fossil wood and marine carbonate (Lusitanian Basin, Portugal). Earth Planet. Sci. Lett. 253, 455–470 (2007).

  4. 4.

    Geochemistry of oceanic anoxic events. Geochem. Geophys. Geosys. 11, 1–30 (2010).

  5. 5.

    Terrestrial feedback in atmospheric oxygen regulation by fire and phosphorus. Lett. Nat. 335, 152–154 (1988).

  6. 6.

    & Redfield revisited 2: what regulates the oxygen content of the atmosphere? Glob. Biogeochem. Cycles 14, 249–268 (2000).

  7. 7.

    & Coupling of the sedimentary sulfur and carbon-cycles-an improved model. Am. J. Sci. 284, 989–1007 (1984).

  8. 8.

    Atmospheric oxygen over Phanerozoic time. Proc. Natl Acad. Sci. 96, 10955–10957 (1999).

  9. 9.

    The Phanerozoic Carbon Cycle: CO2 and O2 150, Oxford University Press (2004).

  10. 10.

    The early history of atmospheric oxygen: homage to Robert M. Garrels. Earth Planet Sci. Lett. 33, 1–36 (2005).

  11. 11.

    , & A global perturbation to the sulfur cycle during the Toarcian Oceanic Anoxic Event. Earth Planet Sci. Lett. 312, 484–496 (2011).

  12. 12.

    & Periodic-Mid Cretaceous Oceanic anoxic events linked by oscillations of the phosphorous and oxygen biogeochemical cycles. Glob. Biogeochem. Cycles 17, 1–11 (2003).

  13. 13.

    & Limits for combustion in low O2 redefine paleoatmospheric predictions for the mesozoic. Science 321, 1197–1200 (2008).

  14. 14.

    Consequences for the biosphere of forest and grassland fires (PhD thesis, Department of Engineering and Cybernetics, University of Reading, 1978).

  15. 15.

    et al. Increased fire activity at the Triassic/Jurassic boundary in Greenland due to climate-driven floral change. Nat. Geosci. 3, 426–429 (2010).

  16. 16.

    in Fire Phenomena and the Earth System (ed. Belcher, C. M.) 288–308Wiley-Blackwell Press (2013).

  17. 17.

    & Phanerozoic concentrations of atmospheric oxygen constructed from sedimentary charcoal. Lett. Nat. Geosci. 3, 627–630 (2010).

  18. 18.

    et al. A forest fire and soil erosion event during the Late Devonian mass extinction. Palaeogeog. Palaeoclim. Palaeoecol. 392, 272–280 (2013).

  19. 19.

    , , & The rise of fire: fossil charcoal in late Devonian marine shales as an indicator of expanding terrestrial ecosystems, fire, and atmospheric change. Am. J. Sci. 315, 713–733 (2015).

  20. 20.

    & How Earth’s atmosphere evolved to an oxic state: a status report. Earth Planet. Sci. Lett. 237, 1–20 (2005).

  21. 21.

    , & Depositional palaeoenvironment and hydrocarbon source potential of the Oligocene Dabaa Formation, north Western Desert, Egypt: a palynofacies approach. Geosphere 12, 346–353 (2016).

  22. 22.

    The Paleoecology of the Liassic Benthic Foraminifera of Great Britain (PhD. dissertation, Rutgers University, 1990).

  23. 23.

    et al. Duration for the Early Toarcian carbon isotope excursion deduced from spectral analysis: consequence for its possible causes. Earth Planet. Sci. Lett. 267, 666–679 (2008).

  24. 24.

    & Pacing of the Toarcian Oceanic Anoxic Event (Early Jurassic) from astronomical correlation of marine sections. Gondwana Res. 25, 1–8 (2014).

  25. 25.

    , , & Astronomical forcing and chronology of the early Toarcian (Early Jurassic) oceanic anoxic event in Yorkshire, UK. Paleoceanography 26, PA4210 (2011).

  26. 26.

    et al. Mochras borehole revisited: a new global standard for Early Jurassic earth history. Sci. Drill no. 16, 81–91 (2013).

  27. 27.

    et al. Astronomical constraints on the duration of the Early Jurassic Pliensbachian Stage and global climatic fluctuations. Earth Planet. Sci. Lett. 455, 149–165 (2016).

  28. 28.

    , , , & Carbon isotope evidence for sedimentary discontinuities in the lower Toarcian of the Lusitanian Basin (Portugal): Sea level change at the onset of the Oceanic Anoxic Event. Sed. Geol. 303, 1–14 (2014).

  29. 29.

    , , , & Baseline intrinsic flammability of Earth’s ecosystems estimated from paleoatmospheric oxygen over the past 350 million years. Proc. Natl Acad. Sci. 107, 22448–22453 (2010).

  30. 30.

    , & COPSE: a new model of biogeochemical cycling over Phanerozoic time. Am. J. Sci. 304, 397–437 (2004).

  31. 31.

    , & Changes in carbon dioxide during an oceanic anoxic event linked to intrusion into Gondwana Coals. Lett. Nat. 35, 479–482 (2005).

  32. 32.

    Fire and climate change during the last 750 Yr in Northwestern Minnesota. Ecol. Mono. 60, 135–159 (1990).

  33. 33.

    et al. Climate change and forest disturbances. Bioscience 51, 723–734 (2001).

  34. 34.

    et al. Jurassic climate mode governed by ocean gateway. Nat. Commun. 6, 1–7 (2015).

  35. 35.

    et al. High-resolution carbon isotope records of the Toarcian Oceanic Anoxic Event (Early Jurassic) from North America and implications for the global drivers of the Toarcian carbon cycle. Earth Planet. Sci. Lett. 459, 118–126 (2017).

  36. 36.

    , & Fungal decomposition of terrestrial organic matter accelerated Early Jurassic climate warming. Sci. Rep. 6, 31930 (2016).

  37. 37.

    & Modeling evidence for global warming, Arctic seawater freshening, and sluggish oceanic circulation during the Early Toarcian anoxic event. Paleoceanography 27, 1–15 (2016).

  38. 38.

    et al. Osmium isotope evidence for two pulses of increased continental weathering linked to Early Jurassic volcanism and climate change. Geology 44, 759–762 (2016).

  39. 39.

    et al. Distribution of clay minerals in Early Jurassic Peritethyan seas: palaeoclimatic significance inferred from multiproxy comparisons. Palaeogeogr. Palaeoclimatol. Palaeoecol. 271, 39–51 (2009).

  40. 40.

    , , & Osmium isotope evidence for the regulation of atmospheric CO2 by continental weathering. Geology 32, 157–160 (2004).

  41. 41.

    , & in Terrestrial Global Productivity, Chapter: Predicting the Future Productivity and Distribution of Global Terrestrial Vegetation (eds Roy, J., Saugier, B. & Mooney, H. A.) 521–541 (Academic Press, 2001).

  42. 42.

    & in Marine Authigenesis: from global to microbial, Chapter: The global diagenetic flux of phosphorus from marine sediments to the oceans: redox sensitivity and the control of atmospheric oxygen levels (eds Glenn, C. R., Prévôt, L. & Lucas, P.) 53–75 (Society for Sedimentary Geology, 2000).

  43. 43.

    & Benthic phosphorus regeneration, net primary production, and ocean anoxia: a model of the coupled marine biogeochemical cycles of carbon and phosphorus. Paleoceanography 9, 677–692 (1994).

  44. 44.

    & Redox stabilization of the atmosphere and oceans by phosphorus‐limited marine productivity. Science 271, 493–496 (1996).

  45. 45.

    et al. Toarcian Stage of Lower Jurassic defined by the Global Boundary Stratotype Section and Point (GSSP) at the Peniche section (Portugal). Episodes 39, 460–481 (2016).

  46. 46.

    In The Peniche Section (Portugal). Contributions to the definition of the Toarcian GSSP (ed. Rocha, R .B.) 17–23 (International Subcommission of Jurassic Stratigraphy, 2007).

  47. 47.

    The Llanbedr (Mochras Farm) Borehole. Report No. 71/18 115 (Institute of Geological Sciences, 1971).

  48. 48.

    & The geology of Cardigan Bay. Proc. Geol. Ass. 98, 331–353 (1987).

  49. 49.

    & Stepwise atmospheric carbon-isotope excursion during the Toarcian Oceanic Anoxic Event (Early Jurassic, Polish Basin). Earth Planet. Sci. Lett. 301, 365–372 (2011).

  50. 50.

    , & Constraints on the thermal energy released from the Chicxulub impactor: new evidence from multi-method charcoal analysis. J. Geol. Soc. Lond. 162, 591–602 (2005).

  51. 51.

    & Lower Jurassic epicontinental carbonates and mudstones from England and Wales: chemostratigraphic signals and the early Toarcian anoxic event. Sedimentology 44, 687–706 (1997).

Download references

Acknowledgements

We thank the Natural Environment Research Council for funding through a studentship grant NE/L501669/1 to S.J.B. C.M.B. acknowledges funding via an ERC Starter Grant ERC-2013-StG-335891-ECOFLAM. S.P.H., T.M.L. and C.M.B. acknowledge funding from the NERC ‘JET’ grant NE/N018508/1, as well as a Royal Society Wolfson Research Merit Award supporting T.M.L. We thank Amir Abbasi for his assistance in the field at Peniche and Mark Grosvenor for his assistance in the lab and J.B. Riding for help at the BGS core store. Two anonymous reviewers and J. Owens are thanked for their useful comments on the manuscript.

Author information

Affiliations

  1. wildFIRE Lab, Hatherly Laboratories, University of Exeter, Prince of Wales Road, England, Exeter EX4 4PS, UK

    • Sarah J. Baker
    •  & Claire M. Belcher
  2. Deep time global change research group, Camborne School of Mines and Environment and Sustainability Institute, University of Exeter, Penryn Campus, Penryn, England, Cornwall TR10 9FE, UK

    • Stephen P. Hesselbo
  3. Earth System Science Group, Laver Building, (Level 7), University of Exeter, North Park Road, England, Exeter EX4 4QE, UK

    • Timothy M. Lenton
  4. MARE, Marine and Environmental Sciences Centre, Department of Earth Sciences, University of Coimbra, 3000-370 Coimbra, Portugal

    • Luís V. Duarte

Authors

  1. Search for Sarah J. Baker in:

  2. Search for Stephen P. Hesselbo in:

  3. Search for Timothy M. Lenton in:

  4. Search for Luís V. Duarte in:

  5. Search for Claire M. Belcher in:

Contributions

C.M.B. designed the study with input from T.M.L. and S.P.H. S.P.H. collected 11 of the rock samples used in this study from the field in Peniche. S.J.B. collected the remaining rock samples in the field from Peniche with the assistance of L.V.D. and from the Mochras core stored at the BGS with the assistance of S.P.H. S.J.B. prepared the samples for charcoal identification, using acid maceration and palynofacies preparation techniques. S.J.B. analysed the samples and the data. S.J.B. wrote the manuscript with contributions from all authors.

Competing interests

The authors declare no competing financial interests.

Corresponding author

Correspondence to Sarah J. Baker.

Supplementary information

Excel files

  1. 1.

    Supplementary Data 1

    Summary of raw data collected

Comments

By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.

Creative Commons BYThis work is licensed under a Creative Commons Attribution 4.0 International License. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in the credit line; if the material is not included under the Creative Commons license, users will need to obtain permission from the license holder to reproduce the material. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/