The timing of marine ecosystem recovery following the End Permian Mass Extinction (EPME) remains poorly constrained given the lack of radiometric ages. Here we develop a high-resolution carbonate carbon isotope (δ13Ccarb) record for 3.20 million years of the Olenekian in South China that defines the astronomical time-scale for the critical interval of major evolutionary and oceanic events in the Spathian. δ13Ccarb documents eccentricity modulation of carbon cycling through the period and a strong obliquity signal. A shift in phasing between short and long eccentricity modulation, and amplification of obliquity, is nearly coincident with a 2% decrease in seawater δ13CDIC, the last of a longer-term stepped decrease through the Spathian. The mid-Spathian shift in seawater δ13CDIC to typical thermocline values is interpreted to record a major oceanic reorganization with global climate amelioration. Coincidence of the phasing shift with the first occurrence of marine reptiles (248.81 Ma), suggests that their invasion into the sea and the onset of a complex ecosystem were facilitated by restoration of deep ocean ventilation linked mechanistically to a change in the response of the oceanic carbon reservoir to astronomical forcing. Together these records place the first constraints on the duration of the post-extinction recovery to 3.35 myr.
Previous studies have shown that post-extinction recovery from the EPME was delayed1,2,3,4 until Middle Triassic due to anomalous oceanic conditions during the Early Triassic, elevated CO2 and surface temperatures5,6,7, widespread anoxia8,9,10,11,12,13 and high primary productivity14,15. However, discovery of an Early Triassic (Griesbachian to Early Smithian) rapid recovery of benthic faunas including bivalves, gastropods, brachiopods, and ostracods in Oman and the South China Block argues against persistent widespread anoxia16,17 and challenge the delayed-recovery hypothesis. Rather, a later period of widespread benthic anoxia and hot tropical temperatures at the Smithian-Spathian boundary created a new biocrisis with slowed rate of recovery6,7, making the pattern of post-extinction recovery more complex. Notably, most prior studies of the biotic recovery have focused on invertebrate benthic marine faunas2,3,4,16,17. Mesozoic marine reptiles, such as ichthyopterygians and sauropterygians, first occurred in the Early Triassic as a part of the transition from the ‘Paleozoic Fauna’ to the ‘Modern Fauna’, and dominated the Mesozoic seas18,19. Our collection of more than 80 well-preserved and multi-clade mid-Spathian marine reptile specimens from the Majiashan Section, Chaohu, South China documents that predatory marine tetrapods diversified in the Early Triassic and were well adapted to life in the sea, indicating a habitable marine environment in the mid-Spathian at Chaohu, which is earlier then previously suggested. The diverse predators, including fish and marine reptiles, and abundant invertebrates such as bivalves, ammonoids and arthropods, form the Chaohu Fauna, represent a nearly complete ecosystem. The first appearance of abundant and multi-clade Mesozoic marine reptiles in Chaohu provides the first glimpse of recovering biotic structure reaching a high trophic level. The lack of geochronologic data, however, has precluded constraining the age of the Chaohu Fauna and thus the timing of post-extinction recovery remains poorly known.
Deep-sea δ13Ccarb records of mid-Cretaceous to Cenozoic age reveal a persistent long-eccentricity (405-kyr) cyclicity, which records astronomical pacing of carbon cycling among Earth’s surface reservoirs20,21,22,23,24. Astronomical cyclicity is also recognized following the EPME25,26,27, when potentially the largest carbon cycle perturbation of the Phanerozoic was followed by a series of disturbances throughout the Early Triassic interval of protracted marine ecosystem recovery2,28. Astronomical cycles in carbon cycling, however, have not yet been recognized leaving ambiguous the timing of the post-extinction recovery and the role of astronomical pacing of climate and carbon cycling through a significant portion of the biotic recovery phase. Furthermore, constraining the drivers of major carbon cycle perturbation is fundamental to understanding climate and biosphere dynamics throughout Earth history29,30.
The nature of the mechanistic link between post-extinction carbon cycle perturbations and the Early Triassic biotic recovery has been the focus of much research invoking wholesale changes in ocean oxygenation and water column stratification13,15. Major oceanic restructuring is inferred to have occurred in response to global warming, likely driven by episodic release of exogenic carbon from Siberian Trap volcanism6,31. Conversely, the role of internal mechanisms and feedbacks in the Earth’s climate system, including cycling through the surface carbon reservoirs, has not been investigated in the context of the recovery of life after the largest extinction since the evolution of metazoans. In this study, we develop a new high-resolution C isotopic record of seawater dissolved inorganic carbon (δ13CDIC) for the end-Smithian through Spathian, utilize it to construct an astrononmical time scale, and in turn, apply it to infer major changes in ocean structure mechanistically linked to the timing of ecosystem recovery.
A high-resolution δ13Ccarb record is constructed spanning the end-Smithian through Spathian (~250.55 to 247.32 Ma, Olenekian, Early Triassic)32,33, from an intermediate- to deep-water 200 to 500 m) slope succession in Majiashan, Chaohu, South China (Fig. 1). Observed fluctuations in δ13Ccarb are interpreted to record secular changes in seawater δ13CDIC, an inference that is supported by the lack of correlation between δ13Ccarb and lithofacies changes, δ18Ocarb, δ13Corg or wt.% CaCO3 (see Supplementary Figs S4 and S5). The veracity of the new δ13Ccarb record is corroborated by similarity in long-term δ13Ccarb trends between the Majiashan section and other global time-equivalent δ13Ccarb records from South China and elsewhere2,34,35. The Majiashan δ13Ccarb time-series (Fig. 1) reveals 3 scales of variation: (i) an abrupt 4% positive shift across the Smithian-Spathian boundary (S-S boundary) observed in previous records31, (ii) a subsequent 106-yr-scale stepwise decrease from peak values of +2% to +4% in the early Spathian to minimum values of 0% to −3% in the middle-late Spathian; and (iii) low-amplitude (0.5–1%), shorter-term (105-kyr scale) oscillations superimposed on the middle-late Spathian portion of the longer-term trend (see Supplementary Fig. S6).
To evaluate potential astronomical cycles preserved in the record and their uncertainties, evolutive average spectral misfit (e-ASM) analysis36 was performed on the δ13Ccarb record following data preparation (see R_analysis file) by statistically comparing the observed oscillations with theoretical periods from the astronomical models La0437 and La10d38 (see Supplementary Fig. S8, Supplementary Table S2). The results show continuous short-term eccentricity, obliquity and precession over a range of sedimentation rates (see Supplementary Fig. S8, Supplementary Table S3). Using the ASM-calibrated astronomical cycles, frequency domain minimal tuning was applied to generate a “floating” ATS (see Supplementary Fig. S10). Following frequency-domain minimal tuning using the average eccentricity period of 115.30 kyr (E2/2 + E3/2 from Supplementary Table S2; see Supplementary Fig. S10), the Majiashan δ13Ccarb record exhibits power spectra peaks at periods of 457.20 kyr, 127.00 kyr, 46.79 kyr, 29.31 kyr, 22.07 kyr and 19.03 kyr (Fig. 2B, see Supplementary Fig. S11, Supplementary Table S5). A strong and continuous obliquity signal in the Evolutive Power Spectral Analysis (EPSA) of the tuned data (Fig. 2C, Supplementary Fig. S12), as well as a relatively persistent precession signal (Fig. 2C), provide independent confirmation of the short eccentricity minimal tuning implemented here.
The astrochronologic testing results provide a good basis for developing a nominal anchored astronomical time scale (ATS) and for dating the age of the first occurrence of Mesozoic marine reptiles, which invaded the marine environment and represent the start of the establishment of the new marine ecosystem dominated by the air-breathing tetrapods28. Given the lack of high-resolution radioisotopic geochronology and biostratigraphy to “anchor” the ATS, we rely upon an assumption based on late Mesozoic and early Cenozoic carbon cycling studies, i.e. δ13Ccarb minima correspond to eccentricity maxima20,21,22,23,24,39,40,41,42,43. Thus, the reversed eccentricity curve of La10d was tied at 247.95 Ma to a depth of 162.62 m (Fig. 2E,F). Using this approach, the S-S boundary34 in the Chaohu area, marked by an abrupt 4% positive shift in δ13Ccarb at the top of fossil-rich black shale (pink line in Figs 1 and 2D–F), is constrained to 250.21 Ma, which compares well with the radioisotopic date of 250.55 ± 0.51 Ma32 for the earliest Spathian. The duration of the 1.36-m thick black shale (18.46 m to 19.82 m, see Supplementary Fig. S2A) below the S-S boundary was estimated to be 19.21 kyr using an astronomically calibrated average sedimentation rate of ~7.08 cm/kyr (see Supplementary Table S4). Although the exact stratigraphic level of the Spathian-Anisian boundary is unknown in the Chaohu area, it can be inferred at the Majiashan section to be at ~171.70 ± 3.72 m above the S-S boundary using an end-Spathian age of 247.32 ± 0.08 Ma33. In this case, the astronomically tuned time series constrains the duration of the Spathian interval to 2.89 ± 0.08 My, which falls within the uncertainty of the U-Pb estimated duration of 3.23 ± 0.60 My32,33,44.
According to our excavation at the Majiashan section, the lowest stratigraphic level of occurrence of marine reptiles in the Chaohu Fauna occurs in the Middle Member of the Nanlinghu Formation, ~117.00 m above the base of the Helongshan Formation (Fig. 1), and is constrained to ~248.81 Ma (Fig. 2). Abundant ichthyosauromorphs occur in the interval 135.83 m to 149.26 m above the base of the Helongshan Formation with a duration of ~279.79 kyr (Fig. 1), including Chaohusaurus, which was fully adapted to the marine aqueous habitat and yet maintained a birth posture typical of terrestrial reptiles, and Cartorhynchus with possible amphibious habits and suction-feeding behavior45. The most primitive Eosauropterygia46, which shows similarity to Middle Triassic Eosauropterygia, occurs ~156.12 m above the base of the Helongshan Formation (Fig. 1) and is constrained to ~248.10 Ma (Fig. 2). Ichthyosaurs were also found in the upper Spathian (Fig. 2).
Persistent eccentricity and obliquity cyclicity in the EHA of the tuned δ13Ccarb data (see Supplementary Fig. S12) indicates astronomically-paced redistribution of carbon between surficial C reservoirs. Seven phases of δ13Ccarb are identified from the minima of the filtered 405-kyr components (long-term eccentricity) (Fig. 2D). The good alignment between the amplitude envelope of the filtered 100-kyr components and the 405-kyr components in Phases 5 through 7 shows the robustness of the tuning results (Fig. 2E). The overall weaker short eccentricity and variable phase relationship observed in Phases 1 through 4 suggests a fundamental change in the response of seawater δ13C to astronomical forcing in the mid-Spathian, coincident with the onset of increased short-term δ13CDIC volatility and a 2% decrease in δ13CDIC, the last of a stepped long-term decrease following the S-S boundary positive excursion. The amplification of obliquity (Fig. 2C) begins between the two abrupt δ13C shifts that define the longer-term decrease in the Spathian.
The response of the ocean carbon reservoir to astronomical forcing is largely dependent on the oceanic structure, which in turn responds to climate change23. Astronomically paced changes in ocean ventilation (oxygenation) lead to periodic releases of 12C-enriched carbon to the surface ocean. For greenhouse times, such as the Early Triassic47, the greater water column stratification of greenhouse oceans makes the ocean C budget more sensitive to orbital variations20,23,24. Together the shift in eccentricity phasing and obliquity amplification likely record a major restructuring of oceanic circulation (cf. refs 24 and 25) linked to climate amelioration during the Spathian13,31. A strongly stratified water column would have supported an expanded oxygen minimum zone and build up of a large dissolved organic carbon (DOC) reservoir in the deep ocean (cf., ref. 48). Turnover from such an oceanic state to a better and deeper ventilated ocean with major restructuring would have released large amounts of this 12C-enriched carbon pool to surficial C reservoirs and accelerated the rate of carbon cycling thus amplifying the response of seawater δ13CDIC to eccentricity and obliquity forcing/pacing20,21. In this context, we interpret the overall higher δ13Ccarb values (+2 to +4%) of the first 800 kyr (Phase 2–3) of the Spathian as recording strong water column stratification, high productivity, enhanced organic matter burial and likely build up of the deep ocean DOC reservoir promoted by the expanded oxygen minimum zone13. The subsequent change in the nature of eccentricity and obliquity cyclicity, along with the final abrupt shift to values that fluctuate around a stable mean (~−2%) characteristic of pre-perturbation thermocline δ13CDIC values in the Majiashan slope environment31, constrains the timing of termination of O2-limited oceanic conditions to the mid-Spathian. The observation of obliquity amplification within phase 4, and continuing into phases 5 through 6, is consistent with the development of a high-latitude, oxygenated, intermediate to deep-water source perhaps in response to cooling and/or eustatic change (cf. ref. 49, 50, 51) that would have led to enhanced ventilation of the deep ocean. The near loss of long-term eccentricity δ13Ccarb cyclicity in Phase 7, and weakening of obliquity, could capture the return to a fully stable well-oxygenated ocean sustained by vigorous circulation (cf. ref. 24).
The ATS indicates that the stratigraphically lowest marine reptile fossil in the Chaohu Fauna, and around the world52, occurs in the later portion of Phase 4 and has an age of ~248.81 Ma. This is the oldest known Mesozoic marine reptile found to date despite concerted but unsuccessful search efforts to find older fossils. Thus, the timing of reptilian invasion into the oceans was likely not much earlier than 248.81 Ma. This estimate constrains the post-extinction ecosystem recovery period to ~3.35 Myr after the PTB (at ~252.16 Ma, as recognized in ref. 32). The main reptile fossil beds that yield Cartorhynchus, a basal and potentially amphibious ichthyosauriform45, as well as abundant multi-clade marine reptile fossils, occur within Phases 5 and 6 (Fig. 2D–F). The Chaohu Fauna is the oldest marine fauna with tetrapod as top predators and a high marine ecosystem complexity, as far as we know.
Previous studies of Early Triassic benthic faunas and vertebrate fossil localities with limited marine ecosystem complexity53,54 supported the hypothesis of a delayed biotic recovery2,4. The appearance of marine reptiles45,46 and the Triassic middle fish fauna (TMFF)55 in Chaohu in the middle Spathian marks the initiation of the establishment of a new Meso-Cenozoic marine ecosystem and thus indicates a high degree of biotic recovery following the end-Permian Mass Extinction at this time52. The temporal relationship between the occurrence of the oldest marine reptile fossil and obliquity amplification (Phase 4) and the appearance of multi-clade marine reptiles during the subsequent change in the nature of the eccentricity modulation (Phases 5–6), temporally linked to the final phase of a two-step decrease in seawater δ13CDIC, indicates a mechanistic link between the appearance and diversification of the marine reptiles and the major change in ocean structure and carbon cycling. We attribute the biotic recovery and initiation of a new marine ecosystem to the final breakdown of ocean stratification and the onset of a high-latitude deep-water source, which would have enhanced ventilation of the deep ocean. Together these changes in ocean structure would have stimulated surface ocean primary productivity promoting the diversification of the marine reptiles. They further suggest that reptiles may have first invaded Panthalassa in the middle Spathian in response to this reorganization.
Marine reptiles introduced a new pattern of shallow marine nutrient circulation in the Early Triassic that may have played a critical role in the post-extinction build-up of the marine ecosystem, by feeding at various depths and defecating near the sea surface52. The post-extinction recovery of the forest ecosystem in the middle Spathian is contemporaneous with that of the marine ecosystem56,57 as would be anticipated if changes in ocean circulation were driven by climate amelioration. Ultimately, stabilization of oceanic conditions in the Early Triassic, which involved a change in the response of carbon cycling to astronomical forcing, likely accelerated the building of the new Meso-Cenozoic marine ecosystem.
In summary, the first occurrence of the Mesozoic marine reptiles is approximately coincident with a shift in astronomically-paced marine carbon cycling, and a ~2% shift in seawater DIC, which indicates that the South China seas remained inhabitable to large air-breathing marine predators following the end-Permian Mass Extinction until a major rearrangement of oceanic circulation. This change led to intensified ventilation and restored well-oxygenated conditions, which is mechanistically linked to astronomically driven changes in C cycling between Earth’s surface reservoirs. The distribution of diversified marine reptiles along the coasts of the Panthalassan Sea in the late Spathian54 was likely fueled by the climate amelioration, changing ocean structure, and increased surface ocean primary productivity in the middle Spathian. The same factors may have encouraged reptiles to invade the sea. Ultimately, stabilization of oceanic conditions in the Early Triassic may have involved climate-life interactions in which a change in the astronomical pacing of climate and carbon cycling among the Earth’s surface carbon reservoirs accelerated the building of the new Meso-Cenozoic marine ecosystem.
Carbonate samples were collected and analyzed at a spacing of ~5–10 kyr from the Majiashan section, Chaohu spanning the late Smithian to Spathian in the Isotope Lab of Nanjing Institute of Geology and Paleontology, Chinese Academy of Sciences with an analytical precision of <0.03%. δ18Ocarb, δ13Ccarb δ13Corg with an analytical precision of <0.1% and wt.% CaCO3 of microdrilled samples were generated in the Stan Margolis Stable Isotope Lab, UC Davis. The δ13Ccarb data were prepared and analyzed in the R software package “Astrochon” (Meyers, 2014; R Core Team, 2015).
How to cite this article: Fu, W. et al. Eccentricity and obliquity paced carbon cycling in the Early Triassic and implications for post-extinction ecosystem recovery. Sci. Rep. 6, 27793; doi: 10.1038/srep27793 (2016).
Pruss, S., Fraiser, M. & Bottjer, D. J. Proliferation of Early Triassic wrinkle structures: Implications for environmental stress following the end-Permian mass extinction. Geology 32, 461–464 (2004).
Payne, J. L. et al. Large perturbations of the carbon cycle during recovery from the End-Permian Extinction. Science 305, 506–509 (2004).
Stanley, S. M. Evidence from ammonoids and conodonts for multiple Early Triassic mass extinctions. Proceedings of the National Academy of Sciences 106, 15264–15267 (2009).
Chen, Z.-Q. & Benton, M. J. The timing and pattern of biotic recovery following the end-Permian mass extinction. Nature Geosci 5, 375–383 (2012).
Knoll, A. H., Bambach, R. K., Payne, J. L., Pruss, S. & Fischer, W. W. Paleophysiology and end-Permian mass extinction. Earth and Planetary Science Letters 256, 295–313 (2007).
Sun, Y. et al. Lethally Hot Temperatures During the Early Triassic Greenhouse. Science 338, 366–370 (2012).
Romano, C. et al. Climatic and biotic upheavals following the end-Permian mass extinction. Nature Geosci 6, 57–60 (2013).
Wignall, P. B. & Hallam, A. Griesbachian (Earliest Triassic) palaeoenvironmental changes in the Salt Range, Pakistan and southeast China and their bearing on the Permo-Triassic mass extinction. Palaeogeography, Palaeoclimatology, Palaeoecology 102, 215–237 (1993).
Wignall, P. B. et al. An 80 million year oceanic redox history from Permian to Jurassic pelagic sediments of the Mino-Tamba terrane, SW Japan, and the origin of four mass extinctions. Global and Planetary Change 71, 109–123 (2010).
Grice, K. et al. Photic Zone Euxinia During the Permian-Triassic Superanoxic Event. Science 307, 706–709 (2005).
Algeo, T. J. et al. Changes in productivity and redox conditions in the Panthalassic Ocean during the latest Permian. Geology 38, 187–190 (2010).
Luo, G. et al. Isotopic evidence for an anomalously low oceanic sulfate concentration following end-Permian mass extinction. Earth and Planetary Science Letters 300, 101–111 (2010).
Song, H. et al. Early Triassic seawater sulfate drawdown. Geochimica et Cosmochimica Acta 128, 95–113 (2014).
Suzuki, N., Ishida, K., Shinomiya, Y. & Ishiga, H. High productivity in the earliest Triassic ocean: black shales, Southwest Japan. Palaeogeography, Palaeoclimatology, Palaeoecology 141, 53–65 (1998).
Meyer, K. M., Yu, M., Jost, A. B., Kelley, B. M. & Payne, J. L. δ13C evidence that high primary productivity delayed recovery from end-Permian mass extinction. Earth and Planetary Science Letters 302, 378–384 (2011).
Twitchett, R. J., Krystyn, L., Baud, A., Wheeley, J. R. & Richoz, S. Rapid marine recovery after the end-Permian mass extinction event in the absence of marine anoxia. Geology 32, 805–808 (2004).
Song, H., Tong, J. & Chen, Z. Q. Evolutionary dynamics of the Permian–Triassic foraminifer size: Evidence for Lilliput effect in the end-Permian mass extinction and its aftermath. Palaeogeography, Palaeoclimatology, Palaeoecology 308, 98–110 (2011).
Rieppel, O. Sauropterygia I. In Handbook of Paleoherpetology Vol. 12 (Verlag Dr. Friedrich Pfeil, 2000).
McGowan, C. & Motani, R. Ichthyopterygia In Handbook of Paleoherpetology Vol. 8 (Verlag Dr. Friedrich Pfeil, 2003).
Zachos, J. C. et al. Climate response to orbital forcing across the Oligocene-Miocene Boundary. Science 292, 274–278 (2001).
Cramer, B. S., Wright, J. D., Kent, D. V. & M., P. Orbital climate forcing of δ13C excursions in the late Paleocene–early Eocene (chrons C24n–C25n). Paleoceanography 18, 1097 (2003).
Pälike, H. et al. The heartbeat of the Oligocene climate system. Science 314, 1894–1898 (2006).
Wang, P., Tian, J. & Lourens, L. J. Obscuring of long eccentricity cyclicity in Pleistocene oceanic carbon isotope records. Earth and Planetary Science Letters 290, 319–330 (2010).
Giorgioni, M. et al. Orbital control on carbon cycle and oceanography in the mid-Cretaceous greenhouse. Paleoceanography 27, PA1204 (2012).
Huang, C., Tong, J., Hinnov, L. & Chen, Z. Q . Did the great dying of life take 700 k.y.? Evidence from global astronomical correlation of the Permian-Triassic boundary interval. Geology 39, 779–782 (2011).
Wu, H. et al. Time-calibrated Milankovitch cycles for the late Permian. Nature Communication 4: 2453 (2013).
Li, M. et al. Astronomical tuning of the end-Permian extinction and the Early Triassic Epoch of South China and Germany. Earth and Planetary Science Letters 441, 10–25 (2016).
Erwin, D. H. The Permo-Triassic extinction. Nature 367, 231–236 (1994).
Kump, L. R. & Arthur, M. A. Interpreting carbon-isotope excursions: carbonates and organic matter. Chemical Geology 161, 181–198 (1999).
Sepkoski, J. J., Bambach, R. K., Raup, D. M. & Valentine, J. W. Phanerozoic marine diversity and the fossil record. Nature 293, 435–437 (1981).
Song, H. et al. Large vertical δ13CDIC gradients in Early Triassic seas of the South China craton: Implications for oceanographic changes related to Siberian Traps volcanism. Global and Planetary Change 105, 7–20 (2013).
Ovtcharova, M. et al. New Early to Middle Triassic U–Pb ages from South China: Calibration with ammonoid biochronozones and implications for the timing of the Triassic biotic recovery. Earth and Planetary Science Letters 243, 463–475 (2006).
Lehrmann, D. J. et al. Timing of recovery from the end-Permian extinction: Geochronologic and biostratigraphic constraints from south China. Geology 34, 1053–1056 (2006).
Tong, J. et al. Events during Early Triassic recovery from the end-Permian extinction. Global and Planetary Change 55, 1–3 (2007).
Galfetti, T. et al. Late Early Triassic climate change: Insights from carbonate carbon isotopes, sedimentary evolution and ammonoid paleobiogeography. Palaeogeography, Palaeoclimatology, Palaeoecology 243, 394–411 (2007).
Meyers, S. R. & Sageman, B. B. Quantification of deep-time orbital forcing by average spectral misfit. American Journal of Science 307, 773–792 (2007).
Laskar, J. et al. A long-term numerical solution for the insolation quantities of the Earth. Astronomy and Astrophysics 428, 261–285 (2004).
Laskar, J., Fienga, A., Gastineau, M. & Manche, H. La2010: A new orbital solution for the long-term motion of the Earth. Astronomy and Astrophysics 532, A89 (2011).
Woodruff, F. & Savin, S. Mid-Miocene isotope stratigraphy in the deep sea: High-resolution correlations, paleoclimatic cycles, and sediment preservation. Paleoceanography 6, 755–806 (1991).
Flower, B. P. & Kennett, J. P. Middle Miocene deepwater paleoceanography in the southwest Pacific: Relations with East Antarctic Ice Sheet development. Paleoceanography 10, 1095–1112 (1995).
Billups, K., Pälike, H., Channell, J. E. T., Zachos, J. C. & Shackleton, N. J. Astronomic calibration of the late Oligocene through early Miocene geomagnetic polarity time scale. Earth and Planetary Science Letters 224, 33–44 (2004).
Holbourn, A., Kuhnt, W., Schulz, M. & Erlenkeuser, H. Impacts of orbital forcing and atmospheric carbon dioxide on Miocene ice-sheet expansion. Nature 438, 483–487 (2005).
Holbourn, A., Kuhnt, W., Schulz, M., Flores, J.-A. & Andersen, N. Orbitally-paced climate evolution during the middle Miocene “Monterey” carbon-isotope excursion. Earth and Planetary Science Letters 261, 534–550 (2007).
Galfetti, T. et al. Timing of the Early Triassic carbon cycle perturbations inferred from new U–Pb ages and ammonoid biochronozones. Earth and Planetary Science Letters 258, 593–604 (2007).
Motani, R. et al. A basal ichthyosauriform with a short snout from the Lower Triassic of China. Nature 517, 485–488 (2015).
Jiang, D. Y. et al. The Early Triassic eosauropterygian Majiashanosaurus discocoracoidis, gen. et sp. nov. (Reptilia, Sauropterygia), from Chaohu, Anhui Province, People’s Republic of China. Journal of Vertebrate Paleontology 34, 1044–1052 (2014).
Preto, N., Kustatscher, E. & Wignall, P. B. Triassic climates — State of the art and perspectives. Palaeogeography, Palaeoclimatology, Palaeoecology 290, 1–10 (2010).
Sexton, P. F. et al. Eocene global warming events driven by ventilation of oceanic dissolved organic carbon. Nature 471, 349–352 (2011).
Bornemann, A. et al. Isotopic evidence for glaciation during the Cretaceous super greenhouse. Science 319, 189–192 (2008).
Westerhold, T. & Röhl, U. High resolution cyclostratigraphy of the early Eocene-New insights into the origin of the Cenozoic cooling trend. Clim. Past 5, 309–327 (2009).
Meyers, S. R., Sageman, B. B. & Arthur, M. A. Obliquity forcing of organic matter accumulation during Oceanic Anoxic Event 2. Paleoceanography 27, 3212 (2012).
Motani, R. et al. Lunge feeding in early marine reptiles and fast evolution of marine tetrapod feeding guilds. Scientific Reports 5, 8900 (2015).
Foster, W. J. & Twitchett, R. J. Functional diversity of marine ecosystems after theLate Permian mass extinction event. Nature Geosci 7, 233–238 (2014).
Scheyer, T. M., Romano, C., Jenks, J. & Bucher, H. Early Triassic Marine Biotic Recovery: The Predators’ Perspective. PLoS ONE 9, 1–20 (2014).
Tintori, A., Hitij, T., Jiang, D., Lombardo, C. & Sun, Z. Triassic actinopterygian fishes: the recovery after the end-Permian crisis. Integrative Zoology 9, 394–411 (2014).
Looy, C. V., Brugman, W. A., Dilcher, D. L. & Visscher, H. The delayed resurgence of equatorial forests after the Permian-Triassic ecologic crisis. Proceedings of the National Academy of Sciences of the United States of America 96, 13857–13862 (1999).
Saito, R. et al. A terrestrial vegetation turnover in the middle of the Early Triassic. Global and Planetary Change 105, 152–159 (2013).
The study was enabled by grants from the Project 40920124002 and 41372016 from the National Natural Science Foundation of China to D.-Y.J., Project 123102 from State Key Laboratory of Palaeobiology and Stratigraphy (Nanjing Institute of Geology and Palaeontology, CAS) to D.-Y.J., Project 20120001110072 from the Research Fund for the Doctoral Program of Higher Education to D.-Y.J., National Geographic grant (Grant number 8669-09) to R.M. and an exchange scholar grant from the China Scholarship Council (CSC) to W.-L.F. The participation of I.P.M was supported by National Science Foundation award EAR-1024737. S.R.M acknowledges support from U.S. National Science Foundation award EAR-1151438, which funded his participation in this project, and also supported the 2014 IsoAstro Geochronology Workshop that W.-L.F. attended.
The authors declare no competing financial interests.
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Fu, W., Jiang, Dy., Montañez, I. et al. Eccentricity and obliquity paced carbon cycling in the Early Triassic and implications for post-extinction ecosystem recovery. Sci Rep 6, 27793 (2016). https://doi.org/10.1038/srep27793
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