The current model for the end-Permian terrestrial ecosystem crisis holds that systematic loss exhibited by an abrupt turnover from the Daptocephalus to the Lystrosaurus Assemblage Zone (AZ; Karoo Basin, South Africa) is time equivalent with the marine Permian–Triassic boundary (PTB). The marine event began at 251.941 ± 0.037 Ma, with the PTB placed at 251.902 ± 0.024 Ma (2σ). Radio-isotopic dates over this interval in the Karoo Basin were limited to one high resolution ash-fall deposit in the upper Daptocephalus AZ (253.48 ± 0.15 (2σ) Ma) with no similar age constraints for the overlying biozone. Here, we present the first U-Pb CA-ID-TIMS zircon age (252.24 ± 0.11 (2σ) Ma) from a pristine ash-fall deposit in the Karoo Lystrosaurus AZ. This date confirms that the lower exposures of the Lystrosaurus AZ are of latest Permian age and that the purported turnover in the basin preceded the end-Permian marine event by over 300 ka, thus refuting the previously used stratigraphic marker for terrestrial end-Permian extinction.
The end-Permian extinction event represents the most catastrophic demise of the Phanerozoic biosphere, with an estimated “instantaneous” biodiversity loss exceeding 90% of marine invertebrate species1,2 and a reportedly coeval turnover of up to 70% of terrestrial vertebrates3,4 but see 5. It is a deep-time model for ecosystem response to increasingly warmer climates, and considered a potential scenario comparable to changes now documented in today’s Earth Systems2,6. As a consequence of increasing global temperature in the latest Permian (Changhsingian), coincident with major mafic volcanism (>3.0 × 106 km3) associated with the emplacement of the Siberian Traps7,8, ocean temperatures climbed9, ocean circulation slowed10, and anoxic waters spread over marine shelves11. As a result, pulsed extinction of benthic, nektonic, and pelagic taxa extended into the early Triassic12.
Postulated global temperature increase over a time interval estimated to range from 60 to 120 ka4,7 is also thought to have affected and reorganized terrestrial ecosystems13,14,15. Evidence for the effects of increasing aridity are purported to be found in the sedimentologic and paleobiologic records of the Karoo Basin3,16,17,18, and elsewhere, and it is thought to have been recorded over a short stratigraphic interval. The Karoo model holds that changes in fluvial architecture, from broad and meandering channels to “braided” regimes19, resulted from the loss of wetland vegetation16 which, in turn, reduced resource availability for late Permian vertebrates leading to rapid extinction and turnover3,4. These reported Karoo patterns have very limited geochronometric context20,21 and are not without controversy.
An emerging vertebrate-fossil record, first investigated in the early 20th Century, formed the basis for subdividing the relatively monotonous sandstone-and-siltstone middle Permian to middle Triassic stratigraphy of the Karoo Basin22,23 (Fig. 1). Currently, eight vertebrate-assemblage zones are recognized as ranging from middle Permian (Eodicynodon) into the Triassic (Cynognathus), wherein two vertebrate-extinctions are recorded24. A middle Permian extinction pulse is identified at the top of the Tapinocephalus24,25 AZ and is documented by several U-Pb ages26. In contrast, the reported turnover from the Daptocephalus (= Dicynodon27) AZ to the Lystrosaurus AZ, long purported to be coeval with the end-Permian marine extinction interval, has never been well-constrained temporally, although an early Triassic detrital zircon age recently was reported for the upper Daptocephalus AZ18. The postulated correlation with the marine record currently rests on stable carbon-isotope and magnetic polarity data3,4, but see 21. An early Changhsingian age, ~1.5 million years older than the crisis, obtained from an ash fall deposit in magnetostratigraphic context is reported from the upper Daptocephalus AZ at one classic Karoo locality20,21 (Fig. 1). However, locating similar volcanogenic deposits in the Lystrosaurus AZ has been challenging. A pristine ash fall deposit on a farm in the Free State Province yields a U-Pb CA-ID-TIMS zircon age of 252.24 ± 0.11 (2σ) Ma demonstrating the reported terrestrial turnover in Gondwana occurred several hundred thousand years before the marine crisis, implying the extinction and turnover mechanisms that operated in terrestrial ecosystems differed from those that operated in the oceans.
Nooitgedacht, Free State
Farm Nooitgedacht 68 lies ~35 km to the NNW of a study area centered on the Bethel 763, Heldenmoed 677, Donald 207 (Fairydale) farms, and Tussen Die Riviere reserve, where 86% of the vertebrate data used to construct the end-Permian model were collected4,28. A rich vertebrate assemblage spanning the uppermost Daptocephalus and lowermost Lystrosaurus AZs recovered from the slopes of two koppies (hills), referred to as Loskop and Spitskop (Supplementary Fig. 1), are inferred to represent a complete Permo–Triassic Boundary (PTB) sequence29—but see geologic evidence for extensive unconformities contained in this stratigraphy20,21,30—and the locality has been utilized in studies on the extinction dynamics in the basin29,31. A rich assemblage of Lystrosaurus maccaigi, considered to be diagnostic of the pre-extinction fauna4,29,32,33, is overlain by two “marker” taxa, Lystrosaurus curvatus and Moschorhinus kitchingii, that have been used to support the placement of the “PTB” at the top of a so-called heterolithic facies18,29,31. A lower “PTB” position was recently proposed18, but the former29 is used to delineate the vertebrate biozone boundary in the current study (Fig. 2).
Similar to other Changhsingian successions in the Karoo Basin, Nooitgedacht’s stratigraphy comprises a seemingly monotonous succession of fine- to very-fine grained feldspathic wacke and mudrock, arranged in upward-fining cycles (Fig. 2a–c; Supplementary Note 1). Mudrock intervals range from coarse to fine siltstone, varying from greenish gray to grayish or brownish red in color33, which are intercalated with sandstone bodies. Mudrock in Daptocephalus AZ strata varies in color from brownish/reddish gray and dusky red to olive and light-olive gray. Upsection, mudrock displays increasingly reddish and brownish colors, while isolated and amalgamated sandstone lenses increase in abundance. These sandstones thin and split laterally, grading into thinly bedded, reddish gray and olive gray lenses of (coarse) siltstone; some of these heterolithic intervals have been interpreted to mark the PTB18,29 (Fig. 2a–c, red arrow). The overlying succession is inferred to be earliest Triassic based on the prevailing vertebrate biostratigraphic model, and is characterized by dusky red and olive-gray laminated mudrock that grades upwards into a sheet-sandstone succession (Fig. 2c). The latter consists of several fining-up cycles, with fine- to very fine-grained feldspathic wacke in which intraformational conglomerate lags occur infrequently21,30. The first thick sheet sandstone occurs approximately 12 m above the proposed “PTB”29 in our section (Fig. 2). Within the dusky red and olive-gray laminated mudrock interval and below the first thick channel-fill, we have identified a well-exposed thin, up to ~1.0 cm thick ash bed (Fig. 2a, d yellow arrow; Supplementary Fig. 2), from which we have recovered a population of pristine, euhedral zircon grains.
U-Pb CA-ID-TIMS results
Reported U-Pb dates are based on the 238U–206Pb decay scheme. This is the most robust system for geologically young rocks due to the greater abundance of 238U and ingrown radiogenic 206Pb. Results of fourteen single crystal zircon, CA-ID TIMS analyses are presented in Supplementary Table 1, and a concordia diagram and plot of individual 206Pb/238U zircon-crystal dates are presented in Fig. 3.
About 1000 zircon grains were recovered from ~800 g of the ash bed and ~100 and ~220 detrital zircon grains were recovered from the enveloping brownish/reddish gray siltstone above and below the ash bed, respectively. Zircon grains recovered from the ash bed are consistently euhedral, translucent, and typically long prismatic, 2/1 short prismatic, or equant and multi-faceted (Fig. 3; lower left insert). In contrast, detrital zircon grains show wide variation in color, morphology, and grain size, with variable degrees of surface abrasion and rounding. Only euhedral, prismatic, and multi-faceted grains, in which small melt inclusions may be present, were analyzed. U-Pb data obtained from 13 single, chemically abraded zircon grains show overlapping and concordant results (Fig. 3). This is consistent with petrographic observations showing what we interpret to be a primary, depositional fabric for the ash deposit (Supplementary Fig. 3). These have a weighted mean 206Pb/238U age of 252.24 ± 0.11 Ma (2σ, MSWD = 0.58). Data for four analyses were obtained using an in-house (ROM) spike (mixed 205Pb-235U) (shown as light-gray bars Fig. 3), which give three oldest and one youngest dates. If these four dates are excluded from the mean and only dates obtained with the community EARTHTIME (ET535) spike (mixed 205Pb-233U-235U) are considered, the age is ~10 ka younger at 252.23 ± 0.12 Ma (2σ, MSWD = 0.54). An older xenocrystic grain, z1, yields a date of 254.2 ± 0.7 Ma and plots just outside of the analytical uncertainty of the data cluster. Th/U ratios vary between 1.4 and 1.7 for all results with the exception of z2 and z14, which are somewhat lower and higher, respectively, at 0.94 and 2.3. We conclude the most robust age estimate for deposition of the ash-fall layer is 252.24 ± 0.11 Ma, based on all 13 dates.
To determine the magnetic polarity of the stratigraphy immediately above and below the ash fall deposit, we sampled the same enveloping brownish/reddish gray siltstone within about 5 cm above and below the ash bed (see Supplementary Note 2 for methodology using ceramic cube sampling results from thermal demagnetization and bulk susceptibility experiments). Response to progressive thermal demagnetization by the siltstone is of high quality, with the typical isolation of a component of magnetization over a range of laboratory unblocking temperatures to ~680 oC (Supplementary Figs. 4, 5; Supplementary Table 2) implying hematite as the key carrier of the remanence in these rocks, as supported by rock magnetic experiments (Supplementary Fig. 6). Samples from siltstone immediately above the ash bed yield magnetizations that are typically of steep negative inclination yet somewhat dispersed declinations. Those samples collected from below the ash bed yield magnetizations of moderate to steep negative inclination with greater dispersion (Supplementary Figs. 4, 5). We interpret these magnetizations to be of normal polarity, and that the observed dispersion in directions is a function of the more unorthodox means by which the siltstones were, by necessity, sampled (see Supplementary Note 2). The demagnetization data give no hint of the preservation of a magnetization of opposite (reverse) polarity in these rocks. Assuming that the magnetizations characteristic of the siltstones are early-acquired (i.e., primary) then the normal polarity magnetozone, with the upper and lower boundaries that remain undetermined, that is indicated by these data can be correlated with a normal polarity chron in geomagnetic polarity time scales that have been compiled for the interval near the PTB34,35. The correlation indicates that either the magnetozone represents the very earliest part of the normal polarity chron in which the PTB is defined to lie in the marine realm or it is part of the previous (older) normal polarity chron (Supplementary Fig. 7). The latter option is, at present, deemed less likely. In comparison to magnetic polarity stratigraphic data from the nearby Bethel farm28, the normal polarity magnetozone at Nooitgedacht lies above the horizon where the biozone contact is identified to lie within a reverse polarity zone. This interpretation is based on the current definition of the vertebrate biozones.
A strong signal of elevated Hg/TOC (>200–1000 ppb/wt.%) has been identified at many PTB sites worldwide, and linked to the emplacement of the Siberian LIP7,8. All Hg/TOC values from siltstone sampled across the biozone boundary29 and the ash bed are below 30 ppb/wt% (Fig. 2; Supplementary Note 3 and Supplementary Table 3), with the lowest values obtained directly at the inferred biozone boundary. In contrast, elevated Hg:TOC values are reported in the Global Boundary Stratotype Section and Point (GSSP) at Meishan that are up to 900 ppb/wt.% relative to a background of <100 ppb/wt.%36. Hence, no evidence exists for mercury enrichment in the intervals sampled in the Nooitgedacht section.
Palynomorph assemblages were recovered from two stratigraphic positions above the ash bed (Fig. 2, Supplementary Fig. 2). The palynomorph assemblage immediately above the ash bed, at a stratigraphic height of 29.9 m (Fig. 2), is of low diversity and dominated by algal remains (Leiosphaeridia) and simple spores. The sample contains low amounts of pollen (Protohaploxypinus) produced by glossopterids (Supplementary Note 4 Information; Supplementary Fig. 8). The sample at a stratigraphic height of 40.42 m is also dominated by algal remains with simple spores (e.g., Brevitriletes, Horriditriletes) and sulcate pollen (Cycadopites) being the dominant terrestrial components (Supplementary Fig. 9). Of interest is the absence of glossopterid pollen and the presence of the gymnospermous pollen Ephedripites, Cycadopites, Falcisporites, Lueckisporites and the cavate spore Densoisporites nejburgii. The latter palynomorphs represent gymnosperms such as conifers, peltasperms, corystosperms, and cormose lycophytes. Our two assemblages represent the transition of South African basinal lowland communities in which Glossopteris were still present to those characterized by other gymnosperms, cormose lycopsids, and ferns. This floral change is observed in many areas of Gondwana and was, until recently, interpreted as the terrestrial equivalent of the marine end-Permian biotic crisis37,38. More recent discoveries from the Sydney Basin in Australia, however, showed that the collapse of glossopterid dominated forests occurred about 370k years prior to the marine event6, although we note the presence there of a long diastem between the last Permian taxa characteristic of the Glossopteris flora and the first post-extinction pollen record39,40.
For over a century22, the vertebrate-fossil record of the Karoo Basin has been held as the world’s standard for interpreting the effects of the end-Permian crisis on terrestrial vertebrates41, the landscapes they inhabited3,4,32, and the ecosystems in which they lived15. According to this model, the last vestiges of the Permian fauna are restricted to the Daptocephalus (=Dicynodon) AZ, whereas the overlying Lystrosaurus AZ, with its purported rapid vertebrate recovery and diversification4,31, has been assigned an earliest Triassic age. This paradigm is extrapolated across the southern Gondwanan continents including Antarctica42, South America43, Laos44, and India45, and into the northern hemisphere including Angara46 and Cathaysia47.
The terrestrial calamity has been correlated with increasing global aridity in response to continued Siberian Trap magmatism, and considered to be time equivalent with the latest Permian phased extinctions in the marine record. Our late Changhsingian age from an ash bed in strata of the lower Lystrosaurus AZ at Nooitgedacht, some 340 ka older than the main marine extinction pulse1, indicates that the vertebrate-biozone boundary, irrespective of placement18,29, in the Karoo Basin, as currently recognized27,32, is not coincident with the marine crisis (Fig. 4). Hence, interpretations about behavioral48,49,50, physiological50,51,52, biogeographical53, extinction mechanisms54, and life-strategy patterns55,56,57 of the Lystrosaurus AZ tetrapods do not reflect a response to, or consequence of, the terminal marine crisis. Yet, our high precision age determination from the Nooitgedacht section and corresponding palynological record does conform with recent findings in eastern Australia6.
A U-Pb CA-ID-TIMS age of 252.31 ± 0.07 Ma is reported and interpreted to constrain the regional collapse of the Glossopteris flora in the Sydney Basin6. This age estimate, too, is ~370 ka prior to the onset of the marine extinction interval but concurrent with the onset of the initial pulse of Siberian Trap volcanism7,8. The Australian date is statistically indistinguishable from our age determination for the ash deposit in the Nooitgedacht section. Based on the proportion of major pollen-and-spore categories and several marker taxa, the Karoo palynoassemblages are considered to be contemporaneous and equivalent to two Australian zones. The pollen assemblage immediately above the ash-fall tuff (Fig. 2) is correlative with the Dulhuntyispora parvithola zone39,40 and the assemblage preserved stratigraphically higher is correlative with the Playfordiaspora crenulata zone39,40. It is at the base of the P. crenulata zone that a major floral change is interpreted as the demise of the Glossopteris flora in the Sydney Basin, Australia (Fig. 4). Assemblages characterized by taeniate bisaccate Protohaploxypinus and Striatopodocarpidites pollen are replaced by assemblages rich in algal remains and low abundance of non-taeniate, alete bissacate pollen and cavate spores. There is an absence of Glossopteris macroflora above that horizon in Australia, although leaves of this taxon are preserved in the P. crenulata zone of the Karoo21,58,59,60 indicating their persistence in southern Africa. The P. crenulata zone is recognized as latest Changhsingian in age, and does not represent the typical Late Permian Glossopteris palynofloras. This is consistent with palynoassemblages documented several tens of meters higher in the Katberg Formation exposed on the Donald 207 (Fairydale) farm28.
The age obtained from the ash deposit at Nooitgedacht necessitates that the Daptocephalus–Lystrosaurus faunal boundary be decoupled from the end-Permian extinction in the marine realm. This result also calls into question the prevailing paradigm for late Permian terrestrial ecosystem perturbation. Instead of the currently favored paradigm of calamitous and globally synchronous turnover in ecosystems3,18,19,41, the reported terrestrial turnover in Gondwana occurred hundreds of thousands of years before the marine one and, therefore, marine and terrestrial responses likely had different extinction mechanisms. Hence, a detailed comparison of terrestrial successions, made possible by high-precision U-Pb geochronology, suggests that greater consideration should be given to a more gradual, complex, and nuanced transition of terrestrial ecosystems during the Changhsingian and, possibly, the early Triassic.
U-Pb CA ID-TIMS Geochronology
About ~800 g of very fine-grained, light green ash from a ~1-cm-thick ash-fall layer was sampled with care taken to exclude material from adjacent beds and/or loose detritus that could contain zircon grains. The layer is hosted in a ~0.5-m-thick, flat-lying, massive, reddish-gray siltstone unit on Farm Nooitgedacht 68, Bethulie District (S30.32616°, E025.93242°). For comparison of zircon populations, similar-sized samples of the massive red siltstone were collected from immediately above and below the ash bed.
The samples were disaggregated in a ring mill and a heavy mineral concentrate was produced on a Wilfley table. This was followed by standard mineral-separation procedures using magnetic (Isodynamic Frantz) and heavy liquid (methylene iodide) methods, the latter in small (~10 mL) centrifuge tubes.
U-Pb analysis was by isotope dilution-thermal ionization mass spectrometry methods on single chemically abraded zircon grains (CA-ID-TIMS) in the Jack Satterly Geochronology Laboratory of the Department of Earth Sciences at the University of Toronto. Prior to dissolution and analysis, zircon crystals were thermally annealed at 900 ° C for 48 h to repair radiation damage in the crystal lattice. Subsequently, the grains were partially dissolved in ~0.1 ml ~50% hydrofluoric acid and ~0.020 ml of HNO3 at 200 °C for 9 h61. Zircon grains were rinsed with 6 N HCl followed by 8 N HNO3 at room temperature prior to dissolution. A 205Pb-233-235U spike from the EARTHTIME Project or an in-house 205Pb-235U (ROM) spike was added to the Teflon dissolution capsules during sample loading. Zircon was dissolved using ~0.10 ml of concentrated HF acid and ~0.020 ml of 8 N HNO3 at 200 °C for 5 days, then dried to a precipitate and re-dissolved in ~0.15 ml of 3 N HCl at 200̊ °C overnight62. U and Pb were isolated from the zircon using 50 μl anion exchange columns using HCl, deposited onto outgassed rhenium filaments with silica gel63, and analyzed with a VG354 mass spectrometer using a single Daly detector in pulse counting mode for Pb, and three Faraday cups in static analysis mode for U or Daly detector if the signal was <300KCps. Corrections to the 206Pb-238U ages for initial 230Th disequilibrium in the zircon have been made assuming a Th/U ratio in the magma of 4.2. All common Pb in each analysis was assigned the isotopic composition of procedural Pb blank. Dead time of the measuring system for Pb was 16 ns. The mass discrimination correction for the Daly detector is constant at 0.05% per atomic mass unit; the thermal mass fractionation correction for Pb was 0.10% per atomic mass unit (±0.076%, 2σ); and the U thermal mass fractionation correction was measured and corrected within each measurement block for static runs. Amplifier gains and Daly characteristics were monitored using the SRM 982 Pb standard. Decay constants are those of Jaffey et al.64 Age errors quoted in the text and Supplementary Table 2, and error ellipses in the concordia diagram and weighted mean age plot (Fig. 3) are given at the 95% confidence interval. Plotting of U-Pb data employed Isoplot 3.7665.
Magnetic properties and petrographic inspection
We sampled siltstone beds within 5 cm above and below the ~1 cm ash-fall bed sampled for geochronology, within the massive, ~0.5 m thick red siltstone interval. These intervals are highly weathered and fragmentary. After cleaning off the exposure with non-magnetic implements, small (<0.7 cm) chips of thinly bedded siltstone were carefully placed into ceramic boxes (measuring 1.7 cm on a side; Beijing Eusci Technologies Ltd.) with ceramic lids, keeping each chip upright and roughly oriented with respect to Geographic north. Chips were removed using non-magnetic tweezers, and, if needed, they were shaped into appropriate size using non-magnetic (Cu-Be) tools. Glass wool or cotton was used to pack the chips in the ceramic boxes, to prevent movement or fragmentation during transport, and the boxes taped shut. In the laboratory, the glass wool or cotton was removed and the ceramic cubes filled with Zircar alumina cement, which is completely non-magnetic. The ceramic boxes were labeled using a soft aluminum rod, and then subjected to progressive thermal demagnetization using an ASC TD48 thermal demagnetization unit. Magnetizations were measured on a pulse-cooled DC SQUID 2G Enterprises magnetometer. Demagnetization data were inspected using orthogonal demagnetization diagrams66 and directions of components of magnetization were determined using principal components analysis67. The general dispersion (in declination) of magnetizations isolated in these materials is largely attributed to the nature of the sampling procedure, necessitated by the very fissile and friable nature of the hematitic siltstone.
An intact sample of the ash-fall layer was prepared for petrographic inspection as follows. After collecting sufficient material from the layer for geochronologic analysis, we carved out the siltstone interval immediately above the ash-fall layer to form a bench indented some six to eight cm into the exposure that preserved the entire interval of ash together with immediately underlying siltstone. A dilute epoxy resin solution was poured onto the bench, in several stages over several hours to ensure that the ash and underlying siltstone was encased in resin. The hardened sample was removed from the exposure 24 h later. Large-format polished petrographic thin sections were prepared from the sample, to include the complete, intact ash-fall layer, the underlying, intact siltstone interval, and fragments of the overlying siltstone interval.
Analyses were completed on whole-rock powders and, for carbonate containing samples, on residual powder de-carbonated with hydrochloric acid. Organic carbon content was measured on a Costech ECS 4010 elemental analyzer (EA). Hg was measured with a Teledyne Leeman Labs Hydra IIc mercury analyzer.
Relative standard deviation was <4.1% for the EA using a pure methionine standard. For the Hydra IIc it was <9% using the NIST 2702 standard.
Siltstone samples for palynological analysis were prepared by RPS Laboratory, Northwich, Cheshire, United Kingdom, and residues sieved at 15 μm. Slides are curated in the Museum of Paleontology, University of California, Berkeley, California, under the locality Nooitgedacht 68 – UCMP PA1378, with PA1378.01 (40.42 m) and PA1378.02 (29.9 m). Preparations from horizons 30.35 m and 30.42 m yielded very low numbers spores and pollen from which it was not possible to evaluate either assemblage. Slides are N2990 P-1 and N2990 P-2, and N4042 P-1 and N4042 P-2. Specimen numbers: Plate 1, A–H: 398665–398672; Plate 2, A–X: 398673–398696.
Further information on research design is available in the Nature Research Reporting Summary linked to this article.
The paleomagnetic and rock magnetic datasets generated and/or analyzed during the current study are available on the MagIC database repository site (https://earthref.org/MagicIC) and on Paleomagnetism.org 2.0 (https://api.paleomagnetism.org). Palynological slides are curated in the Museum of Paleontology, University of California, Berkeley, California, under the locality Nooitgedacht 68 – UCMP PA1378, with PA1378.01 (40.42 m) and PA1378.02 (29.9 m). Slides are N2990 P-1 and N2990 P-2, and N4042 P-1 and N4042 P-2. Specimen numbers: Plate 1, A–H: 398665–398672; Plate 2, A–X: 398673–398696. The authors declare that all additional data supporting the findings of this study are included in this published article (and its Supplementary Information, Figures, and Tables).
Shen, S. et al. A sudden end-Permian mass extinction in South China. Geol. Soc. Am. Bull. 131, 205–223 (2018).
Payne, J. L. & Clapham, M. F. End-Permian mass extinction in the oceans: an ancient analog for the twenty-first century? Ann. Rev. Earth Planet. Sci. 40, 89–111 (2012).
Ward, P. D. et al. Abrupt and gradual extinction among Late Permian land vertebrates in the Karoo Basin, South Africa. Science 307, 709–714 (2005).
Smith, R. M. H. & Botha-Brink, J. Anatomy of a mass extinction: Sedimentological and taphonomic evidence for drought-induced die-offs at the Permo–Triassic boundary in the main Karoo Basin, South Africa. Palaeogeogr. Palaeoclimatol. Palaeoecol. 396, 99–118 (2014).
Schneider, J. W. et al. Late Paleozoic–early Mesozoic continental biostratigraphy. PalaeoWorld, https://doi.org/10.1016/j.palwor.2019.09.001 (2019).
Fielding, C. R. et al. Age and pattern of the southern high-latitude continental end-Permian extinction constrained by multiproxy analysis. Nat. Comm. 10, 385 (2019).
Burgess, S. D. & Bowring, S. High-precision geochronology confirms voluminous magmatism before, during, and after Earth’s most severe extinction. Sci. Adv. 1, e1500470 (2015).
Burgess, S. D., Muirhead, J. D. & Bowring, S. A. Initial pulse of Siberian Traps sills as the trigger of the end-Permian mass extinction. Nat. Comm. 8, 164 (2017).
Song, H., Wignall, P. B., Tong, J. & Yin, H. Two pulses of extinction furing the Permian–Triassic crisis. Nat. Geosci. 6, 52–56 (2013).
Hotskinski, R. M., Bice, K. L., Kump, L. R., Najjar, R. G. & Arthur, M. A. Ocean stagnation and end Permian anoxia. Geology 29, 7–10 (2001).
Schaal, E. K., Meyer, K. M., Lau, K., Silva-Tamayo, J. C., & Payne, J. L. in Volcanism and Global Environmental Change (eds Schmidt, A., Kristad, K. E., and Elkins-Tanton, L. T.) 275–290 (Cambridge University Press, Cambridge, 2015).
Zhang, F. et al. Multiple episodes of extensive marine anoxia linked to global warming and continental weathering following the latest Permian mass extinction. Sci. Adv. 4, e1602921 (2018).
Rey, K. et al. Global climate perturbations during the Permo-Triassic mass extinctions recorded by continental tetrapods from South Africa. Gond. Res. 3, 384–396 (2016).
MacLeod, K. G., Quinton, P. C. & Bassett, D. J. Warming and increased aridity during the earliest Triassic in the Karoo Basin, South Africa. Geology 45, 483–486 (2017).
Roopnarine, P. D., Angielczyk, K. D., Weik, A., & Dineen, A. Ecological persistence, incumbency and reorganization in the Karoo Basin during the Permian-Triassic transition. Ear. Sci. Rev. https://doi.org/10.1016/j.earscire2018.10.014 (2018).
Smith, R. M. H. & Ward, P. D. Pattern of vertebrate extinctions across an event bed at the Permian–Triassic boundary in the Karoo Basin of South Africa. Geology 29, 1147–1150 (2001).
Viglietti, P. A., Rubidge, B. S., & Smith, R. M. H. New Late Permian tectonic model for South Africa’s Karoo Basin: foreland tectonics and climate change before the end-Permian crisis. Sci. Rep. https://doi.org/10.1038/s41598-017-09853-3 (2017).
Botha, J. et al. New geochemical and palaeontological data from the Permian-Triassic boundary in the South African Karoo Basin test the synchronicity of terrestrial and marine extinctions. Palaeo Palaeo Palaeo 540, 109467 (2020).
Smith, R. M. H. Changing fluvial environments across the Permian–Triassic boundary in the Karoo Basin, South Africa, and possible causes of tetrapod extinctions. Palaeo Palaeo Palaeo 117, 81–104 (1995).
Gastaldo, R. A. et al. Is the vertebrate defined Permian–Triassic Boundary in the Karoo Basin, South Africa, the terrestrial expression of the End Permian marine event? Geology 43, 939–942 (2015).
Gastaldo, R. A., Neveling, J., Geissman, J. W. & Kamo, S. L. A Lithostratigraphic and Magnetostratigraphic Framework in a Geochronologic Context for a Purported Permian–Triassic Boundary Section at Old (West) Lootsberg Pass, Karoo Basin, South Africa. Geol. Soc. Am. Bull. 130, 1411–1438 (2018).
Broom, R. On the Permian and Triassic faunas of South Africa. Geol. Mag. Dec. 5, 29–30 (1906).
Rubidge, B. S., ed. Biostratigraphy of the Beaufort Group (Karoo Supergroup). Geol. Surv. S. Afr. Biostrat. Ser. 1, 1–46 (1995).
Day, M. O. et al. When and how did the terrestrial mid-Permian mass extinction occur? Evidence from the tetrapod record of the Karoo Basin, South Africa. Proc. Roy. Soc. B 282, 20150834 (2015).
Lucas, S. G. Permian Tetrapod Extinction Events. Ear. Sci. Rev. 170, 31–60 (2017).
Rubidge, B. S., Erwin, D. H., Ramezani, J., Bowring, S. A. & de Klerk, W. J. High-precision temporal calibration of Late Permian vertebrate biostratigraphy. U-Pb zircon constraints from the Karoo Supergroup, South Africa. Geology 41, 363–366 (2013).
Viglietti, P. A. et al. The Daptocephalus Assemblage Zone (Lopingian), South Africa: A proposed biostratigraphy based on a new compilation of stratigraphic range. J. Afr. Ear. Sci. 113, 153–164 (2016).
Gastaldo, R. A., Neveling, J., Geissman, J. W. & Looy, C. V. Testing the Daptocephalus and Lystrosaurus Assemblage Zones in a lithostratographic, magnetostratigraphic, and palynological framework in the Free State, South Africa. PALAIOS 34, 542–561 (2019).
Botha-Brink, J., Huttenlocker, A. K., & Modesto, S. P. in Early Evolutionary History of the Synapsida, Vertebrate Paleobiology and Paleoanthropology (eds Kammerer, C. F., Angielczyk, K. D., & Fröbisch, J.) 289–304 (Springer, Dordrecht, 2014).
Pace, D. W., Gastaldo, R. A. & Neveling, J. Early Triassic aggradational and degradational landscapes of the Karoo basin and evidence for climate oscillation following the P-Tr Event. J. Sed. Res. 79, 316–331 (2009).
Botha, J. & Smith, R. M. H. Rapid vertebrate recuperation in the Karoo Basin following the End-Permian extinction. J. Afr. Ear. Sci. 45, 502–514 (2006).
Viglietti, P. A., Smith, R. M. H. & Rubidge, B. S. Changing palaeoenvironments and tetrapod populations in the Daptocephalus Assemblage Zone (Karoo Basin, South Africa) indicate early onset of the Permo-Triassic mass extinction. J. Afr. Ear. Sci. 138, 102–111 (2018).
Li, J., Gastaldo, R. A., Neveling, J. & Geissman, J. W. Siltstones across the Daptocephalus (Dicynodon) and Lystrosaurus Assemblage Zones, Karoo Basin, South Africa, show no evidence for aridification. J. Sed. Res. 87, 653–671 (2017).
Szurlies, M. Late Permian (Zechstein) magnetostratigraphy in Western and Central Europe: Geol. Soc. London Spec. Pub. https://doi.org/10.1144/SP376.7. (2013).
Hounslow, M. W. & Balabanov, Y. P. A geomagnetic polarity time scale for the Permian, calibrated to stage boundaries. Geol. Soc. London Spec. Pub. https://doi.org/10.1144/SP450.8 (2016).
Wang, X. et al. Mercury anomalies across the end Permian mass extinction in South China from shallow and deep water depositional environments. Ear. Planet. Sci. Lett. 496, 159–167 (2018).
Lindström, S. & McLoughlin, S. Synchronous palynofloristic extinction and recovery after the end-Permian event in the Prince Charles Mountains, Antarctica: implications for palynofloristic turnover across Gondwana. Rev. Palaeobot. Palynol. 145, 89–122 (2007).
Shi, G. R., Waterhouse, J. B. & McLoughlin, S. The Lopingian of Australasia: a review of biostratigraphy, correlations, palaeogeography and palaeobiogeography. Geol. Jour. 43, 230–263 (2010).
Vajda, V. et al. End-Permian (252 Mya) deforestation, wildfires and flooding—An ancient biotic crisis with lessons for the present. Ear. Planet. Sci. Lett. 529, 115875 (2020).
Mays, C. et al. Refined Permian–Triassic floristic timeline reveals early collapse and delayed recovery of south polar terrestrial ecosystems. GSA Bull. https://doi.org/10.1130/B35355.1 (2019).
Benton, M. J. & Newell, A. J. Impacts of global warming on Permo-Triassic terrestrial ecosystems. Gond. Res. 25, 1308–1337 (2014).
Collinson, J. W., Hammer, W. R., Askin, R. A. & Elliot, D. H. Permian–Triassic boundary in the central Transantarctic Mountains, Antarctica. Geol. Soc. Am. Bull. 118, 747–763 (2006).
Langer, M. C. The first record of dinocephalians in South America. Late Permian (Rio do Rasto Formation) of the Paraná Basin, Brazil. Neues Jahrb. Geol. PaläOntol. Abhand. 215, 69–95 (2000).
Battail, B. Late Permian dicynodont fauna from Laos. Geol. Soc. Lond. Spec. Pub. 315, 33–40 (2009).
Gupta, A. & Das, D. P. Report of Lystrosaurus cf. curvatus and L. cf. declivis from the Early Triassic Panchet Formation, Damodar Valley. Indian J. Geosci. 65, 119–130 (2011).
Battail, B. Les genres Dicynodon et Lystrosaurus (Therapsida, Dicynodontia) en Eurasie: Une mise au point. A review. Geobios 30, 39–48 (1997).
Tong, J. et al. Triassic integrative stratigraphy and timescale of China. Sci. China Ear. Sci. 62, 189–222 (2019).
Damiani, R., Neveling, J., Modesto, S. & Yates, A. Barendskraal, a diverse amniote locality from the Lystrosaurus Assemblage Zone, Early Triassic of South Africa. Palaeontol. Afr. 39, 53–62 (2003).
Abdala, F., Cisneros, J. C. & Smith, R. M. H. Faunal Aggregation in the Early Triassic Karoo Basin. Earliest evidence of shelter-sharing behavior among tetrapods? PALAIOS 21, 507–512 (2005).
Botha-Brink, J., Huttenlocker, A., Angielczyk, K. D., Codron, D. & Ruta, M. Breeding young as a survival strategy during Earth’s greatest mass extinction. Sci. Rep. https://doi.org/10.1038/srep24053. (2016).
Botha-Brink, J. & Angielczyk, K. D. Do extraordinarily high growth rates in Permo-Triassic dicynodonts (Therapsida, Anomodontia) explain their success before and after the end-Permian extinction? Zool. J. Linn. Soc. 160, 341–365 (2010).
Laaß, M. et al. New insights into the respiration and metabolic physiology of Lystrosaurus. Acta Zool. 92, 363–371 (2010).
Sidor, C. A. et al. Provincialization of terrestrial faunas following the end-Permian mass extinction. Proc. Natl Acad. Sci. USA 110, 8129–8133 (2013).
Benton, M. J. Hyperthermal-driven mass extinctions: killing models during the Permian–Triassic mass extinction. Phil. Trans. Roy. Soc. A https://doi.org/10.1098/rsta.2017.0076 (2018).
Ray, S., Cox, A. & Bandyopadhyay, S. Lystrosaurus murrayi (Therapsida, Dicynodontia): bone histology, growth and lifestyle adaptations. Palaeontol 48, 1169–1186 (2005).
Huttenlocker, A. K. Body size reductions in nonmammalian eutheriodont therapsids (Synapsida) during the end-Permian mass extinction. PLoS ONE https://doi.org/10.1371/journal.pone.0087553 (2014).
Botha-Brink, J. Burrowing in Lystrosaurus. preadaptation to a post-extinction environment? J. Vert. Paleontol. https://doi.org/10.1080/02724634.2017.1365080 (2017).
Prevec, R., Gastaldo, R. A., Neveling, J., Reid, S. B. & Looy, C. V. An Autochthonous Glossoperid flora with Latest Permian palynomorphs and its depositional setting from the Dicynodon Assemblage Zone of the southern Karoo Basin, South Africa. Palaeo Palaeo Palaeo 292, 381–408 (2010).
Gastaldo, R. A., Knight, C., Neveling, J. & Tabor, N. Late Permian Paleosols from Wapadsberg Pass, South Africa: implications for Changhsingian Climate. Geol. Soc. Am. Bull. 126, 665–679 (2014).
Gastaldo, R. A. et al. Paleontology of the Blaauwater 67 Farm, South Africa: testing the Daptocephalus/Lystrosaurus Biozone Boundary in a Stratigraphic Framework. PALAIOS 34, 349–366 (2017).
Mattinson, J. M. Zircon U-Pb chemical abrasion (“CA-TIMS”) method. combined annealing and multi-step partial dissolution analysis for improved precision and accuracy of zircon ages. Chem. Geol. 220, 47–66 (2005).
Krogh, T. E. A low contamination method for hydrothermal decomposition of zircon and extraction of U and Pb for isotopic age determinations. Geochim. Cosmochim. Acta 37, 485–494 (1973).
Gerstenberger, H. & Haase, G. A highly effective emitter substance for mass spectrometric Pb isotope ratio determinations. Chem. Geol. 136, 309–312 (1997).
Jaffey, A. H., Flynn, K. F., Glendenin, L. E., Bentley, W. C. & Essling, A. M. Precision measurement of half-lives and specific activities of 235U and 238U. Phys. Rev. 4, 1889–1906 (1971).
Ludwig, K. R. User’s manual for Isoplot 3.76. A geochronological toolkit for Microsoft Excel. Berkeley Geochron. Cent. Spec. Publ. 4, 71 (2003).
Zijderveld, J. D. A. in Methods in Palaeomagnetism (eds Collinson, D. W., Creer, K. M. & Runcorn, S. K.) 254 (Elsevier, Amsterdam, 1967).
Kirschvink, J. L. The least squares line and plane and the analysis of paleomagnetic data. Geophys. J. Roy. Astron. Soc. 62, 699–718 (1980).
Our research efforts were supported, in part, by: the Council for Geoscience (South Africa) to JN; JWG startup funds at the University of Texas–Dallas; and NSF EAR 0749895, 0934077, 1123570, and 1624302 to RAG. Field assistance by R. Jia and T. Stonesifer, Colby College, and S. Makubalo, Council for Geosciences, are acknowledged and appreciated. Anthony Hocking and the staff at the Royal Hotel Bethulie, South Africa, and A.J. Griesel, land owner, are acknowledged for their support of our efforts. Assistance in the paleomagnetism laboratory was provided by Z. Haque. Student participation was supported by the Selover Family student-research endowment and Barrett T. Dixon Geology Research and Internship Fund for undergraduate experiences in the Department of Geology, Colby College.
The authors declare no competing interests.
Peer review information Nature Communications thanks Mark Schmitz, Shu-zhong Shen and the other, anonymous, reviewer for their contribution to the peer review of this work. Peer reviewer reports are available.
Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
About this article
Cite this article
Gastaldo, R.A., Kamo, S.L., Neveling, J. et al. The base of the Lystrosaurus Assemblage Zone, Karoo Basin, predates the end-Permian marine extinction. Nat Commun 11, 1428 (2020). https://doi.org/10.1038/s41467-020-15243-7