Environmental histories that span the last full glacial cycle and are representative of regional change in Australia are scarce, hampering assessment of environmental change preceding and concurrent with human dispersal on the continent ca. 47,000 years ago. Here we present a continuous 150,000-year record offshore south-western Australia and identify the timing of two critical late Pleistocene events: wide-scale ecosystem change and regional megafaunal population collapse. We establish that substantial changes in vegetation and fire regime occurred ∼70,000 years ago under a climate much drier than today. We record high levels of the dung fungus Sporormiella, a proxy for herbivore biomass, from 150,000 to 45,000 years ago, then a marked decline indicating megafaunal population collapse, from 45,000 to 43,100 years ago, placing the extinctions within 4,000 years of human dispersal across Australia. These findings rule out climate change, and implicate humans, as the primary extinction cause.
The planet lost the majority of its largest mammals, birds and reptiles outside of Africa during the late Quaternary (the past 130,000 years). Identifying the drivers of the global extinctions of these megafauna (animals with average weights >44 kg) remains controversial1, with climate fluctuations2,3,4,5, human impact through hunting6,7,8 and/or habitat alteration9,10, and/or a synergistic combination of climate and humans11,12,13 the commonly cited causes. The major challenge has been precisely aligning individual records that contain unambiguous and regionally representative signals of these different factors to test extinction hypotheses robustly. Nowhere is the issue more acute than in Australia, where 85% of the continent’s large mammal species went extinct sometime shortly after 50 kyr ago9,10,14,15, approximately the same time that humans established their first firm presence around the continent14,16. Dating both human colonisation and megafaunal extinction in Australia has been hampered by the occurrence of both events at or beyond the reliable limits of radiocarbon dating15,17,18,19.
A major challenge that has emerged is that most data relevant to the debate come from sites scattered across the continent that capture local events and may not be representative of regional changes.
An alternative approach to the analysis of individual (local) sites is to capitalize on the regional averaging of proxy signals offered by marine sediment sequences from the continental shelf surrounding Australia. Marine sedimentary sequences have distinct advantages over most terrestrial records, including generally continuously deposition and they can be precisely aligned and dated using the global marine isotope stratigraphy, the latter providing complementary age control to radiocarbon-based chronological frameworks. Here we present a continuous, stratigraphically well-constrained 150,000-year multi-proxy record from a sediment core recovered ∼100 km offshore south-western Australia, in which we identify the timing and sequence of events of the most widespread and sustained regional ecosystem changes over the past 150,000 years and precisely date regional megafaunal extinction. South-west Australia experiences a seasonal delivery of south-westerly air masses (winter-dominated)20,21,22 that supports large, dense forests with a diverse biota23. Importantly, the region has some of the earliest evidence for human arrival on the continent19,24 and is a candidate refugium for large mammals during past periods of aridity25, making it an ideal location to explore the response of megafauna to climate changes and human activity.
We utilize the number of spores from the dung fungus Sporormiella as our proxy for herbivore biomass in the catchment feeding the core site (a land area of ∼10,000 km2). We record high levels of Sporormiella from 150 to 45 kyr ago, indicating megafaunal populations were present under a range of climatic conditions from the warm, wet, interglacials to the hyper-aridity of the penultimate glacial during the period 150–130 kyr ago, and, critically, during the Marine Isotope Stage (MIS) 5–4 transition characterized by substantial changes in vegetation and fire regime ∼70 kyr ago. Importantly, however, Sporormiella underwent a marked and irreversible decline from 45 to 43.1 kyr ago, indicating megafaunal population collapse, with extinction apparently complete within 4,000 years of human occupation of the continent. Our results provide the first stratigraphically constrained sequence of events for Australian megafaunal extinctions, rule out extreme aridity and habitat change as causal mechanisms, leaving human agency, specifically imperceptible overkill7 as the most probable extinction cause.
Recovery and analysis of the Cape Pasley marine core
Gravity core MD03-2614G was recovered at 34° 43.728′ S and 123° 25.698′ E from a water depth of 1,070 m, ∼100 km south of Cape Pasley, south-western Australia, as part of the IMAGES program (Fig. 1). A well-constrained chronostratigraphy, established from tuning the planktonic δ18O record of Globigerinoides ruber to reference records and 11 accelerated mass spectrometry (AMS) 14C dates (Supplementary Tables 1 and 2; Supplementary Fig. 1) indicates that the 8.4 m core captures all of MIS 1–6, providing a continuous record of environmental change through the last ∼150 kyr (Fig 2 and Methods). In the absence of large river systems in the Cape Pasley area, delivery of terrigenous material to the site is by continental run-off and wind, the latter at present predominantly from the north to northwest (Fig. 1). Our environmental record was established through study of fossil pollen, charcoal, Sporormiella dung spores and terrestrial sediment (Methods). Palynological sampling was designed to include all MIS and sub-stages, with targeted higher resolution (0.7 kyr per sample) analysis across the likely period of overlap between human settlement and megafauna (55–42 kyr ago; ref. 14).
Environmental change in south-western Australia
The Cape Pasley marine core record provides a high-resolution record of environmental change from the south-west of Australia. This marine record shows that the region experienced substantial environmental change during the past 150 kyr (Fig. 2; Supplementary Fig. 3). Overall, vegetation change has followed Northern Hemisphere ice-volume variation with expansion of tree cover under warm, high-precipitation regimes during MIS 5 and, to a lesser degree, MIS 1, and contraction during maximum cold and dry phases of MIS 6 2 (Fig. 2; Supplementary Fig. 3). The greatest density of forest, dominated by Eucalyptus, is identified during MIS 5.5 (the last interglacial), most likely developed under climatic conditions comparable to those today in the south-western corner of the continent (Fig. 1) and indicates that this period experienced the highest effective precipitation of the entire record. Marked and sustained decreases in percentages of woody elements, principally Eucalyptus, and increases in woody herbaceous scrub taxa, principally Asteraceae and Chenopodiaceae (Fig. 2; Supplementary Fig. 3), date from the MIS 5–4 transition at ∼70 kyr ago in response to regional drying. Generally, low terrestrial sediment input between 70 and 15 kyr ago also provides evidence for drier climatic conditions (Fig. 2). The records from the North Australian Basin and tropical Queensland (Lynch’s Crater and ODP Site 820) record similar changes to drier vegetation types through this period26,27,28 and these environmental changes are broadly coincident with the hydrological changes inferred from the Lake Eyre sedimentary record29.
Before ∼70 kyr ago, charcoal peaks in the Cape Pasley record are associated with high values for Myrtaceous elements (Fig. 2; Supplementary Fig. 4), indicating that sclerophyll forests were the principal source of fuel for fires. After ∼70 kyr ago, lower and more stable values for charcoal indicate a reduction in biomass burning and that burning events were less extreme. This altered fire regime coincides with the change to more open vegetation shown by the expansion of herbaceous and herbaceous taxa and reduced terrestrial sediment levels (Fig. 2; Supplementary Figs 3 and 4). The record from the Cape Range Peninsula also shows high levels of charcoal associated with peak Myrtaceae values in the early part of the last glacial cycle (Fig. 1)30 before changing to a sparsely vegetated landscape with reduced biomass burning (Supplementary Fig. 4). Contrary to the previously reported environmental impacts recorded in connection with human arrival in the north of the continent13,31, the Cape Pasley record shows no sustained change in charcoal flux coincident with initial human arrival (at 50–45 kyr ago).
The timing of megafaunal extinction in south-western Australia
Spores of the coprophilous fungi Sporormiella, commonly produced on the dung of herbivores32 and shown in the fossil record to be consistent and reliable markers of Pleistocene megafaunal biomass (declining during mass extinctions and increasing during the introduction of domesticated livestock in recent centuries33,34), were identified in this study (Supplementary Fig. 2) and used to indicate the presence of megafaunal populations. As a marine sequence, the Cape Pasley record is not subject to local taphonomic biases that may occur and require consideration at terrestrial settings such as local moisture levels35, near-by herbivore activity36 and position of the core site within the basin37. In our record, Sporormiella is abundant throughout MIS 6, 5, 4 and the early part of MIS 3, and rare in the later part of MIS 3, 2 and MIS 1. Vegetation, oxygen isotope and terrigenous sediment records show that MIS 6 was at least as dry and cool as MIS 2. High Sporormiella percentages in MIS 6, however, indicate that megafauna numbers were not significantly impacted by these extreme climatic conditions. Before 45 kyr ago the Sporormiella value is 9.7%, but declines sharply to 2% by 43.1 kyr ago (Supplementary Table 4; Supplementary Fig. 5). Declines of Sporormiella abundances to <2% of the pollen sum have repeatedly been shown to mark late Pleistocene megafaunal extinctions in North America38,39,40 and late Holocene extinctions in Madagascar34. We therefore interpret the marked decline of Sporormiella immediately after 45 kyr ago in our record as indicating the collapse of the Pleistocene megafaunal population in south-western Australia with extinction complete by 43.1 kyr ago. This extinction event post dates the substantial climatically driven regional environmental changes at ∼70 kyr ago by ∼27,000 years and precedes the cold and aridity of MIS 2 by 13,000 years.
The observed timing of the extinction event we record in south-western Australia (from 45 to 43.1 kyr ago) is in accord with megafaunal extinction in other regions. Across the Australian arid zone, the extinction of the giant bird Genyornis newtoni10 occurred 45.7±2.5 kyr ago with over 200 sites that contain burnt egg shell indicative of human consumption of its eggs9,41,42. At the Wet Cave sequence from Naracoorte (South Australia)43, extinction of megafauna occurred by 45.3 kyr ago and extinction of megafauna at Lynch’s Crater (north-east Queensland) by ∼41 kyr ago (ref. 44). These age estimates accord with the age for continent-wide extinction of megafauna of 46.4 kyr ago (confidence interval 51–40 kyr ago) derived from OSL and U-series ages of articulated remains at 28 sites15. Importantly, the extinction event we identify in south-western Australia commences 2,000 years after the established age for human dispersal across Australia at ca. 47 kyr ago (ref. 16) and is mid-range within the estimate for megafauna–human overlap on mainland Australia centred on ∼44 kyr ago (ref. 14). The recent discovery of Diprotodon bone and eggshells of Geyornis in a well-stratified archaeological sequence at Warratyi rock shelter in central Australia dated to ≥49–46 kyr ago includes evidence for direct interaction between humans and megafauna in this time range18, supporting our results. Archaeological evidence from Devil’s Lair (Fig. 1) shows human presence in south-west Australia by ∼48 kyr ago and regional human occupation by 45.5 kyr ago (ref. 19) with megafaunal extinction taking place at that site between 47 and 42 kyr ago (ref. 15).
Our results provide the most refined stratigraphically constrained sequence of events for Australian megafaunal extinctions and the first regionally representative record of their loss. Our new data establish the precise timing and order of the most substantial, widespread and sustained environmental changes of the last glacial cycle, as well as megafaunal extinctions, in south-western Australia (Fig. 3). Specifically, they show that: (1) dense eucalypt woodland gave way to open Chenopodiaceae–Asteraceae shrubland at the MIS 5–4 transition at ∼70 kyr ago, a change initiated some ∼23,000 years before evidence for the presence of people on the continent, indicating that anthropogenic mechanisms were not responsible for the sustained change in vegetation; (2) there were few widespread fire events after 70 kyr ago, likely owing to the less flammable nature of the open vegetation; and (3) the regional collapse of megafaunal populations commenced at 45 kyr ago and took <2,000 years in total (concluded by 43.1 kyr ago).
We therefore conclude there is no temporal association between climatically driven environmental changes and megafaunal extinction in the south-west region. There is also no indication in our data that the megafauna suffered a slow demise commensurate with increases in aridity. Furthermore, our data show no impact on megafauna presence of the marked stepwise increases in aridity over the longer term (during a full glacial cycle). This work adds to a growing body of evidence showing similar timing for extinction in the south-west of Australia as for extinction at sites in central9,10, southern36 and north-eastern Australia35, as well as continent-wide extinction of all megafauna by ∼46 kyr ago (ref. 15).
The debate over megafaunal extinction causes has consistently been between climate and humans. Having eliminated climate as the primary cause of extinction, we turn to consideration of human causation, of which hunting is most favoured as extinction driver. In Australia, there are no reported kill sites to indicate concentrated hunting efforts (other than transient sites where humans gathered and consumed Genyornis eggs) or widespread slaughter of megafauna. However, this does not disprove that human hunting took place and is itself informative for shaping debate. Large mammals are demographically vulnerabile to hunting pressure owing to their typically low reproduction rates and low population growth7,8. It has been estimated that low intensity hunting (such as the killing of just one juvenile per person per decade) could result in a species being extinguished over a few hundred years7. Such selective, low-level hunting would be virtually imperceptible in the archaeological record, accounting for the lack of reported kill sites. In this scenario, all species of megafauna could have been lost from the entire continent within a few thousand years. In the Cape Pasley record, megafaunal population collapse commenced within 2,000 years of the established date for human dispersal on Australia at ∼47 kyr ago (ref. 16), with extinction completed within 4,000 years. We conclude our results are consistent with extinction being driven by such ‘imperceptible overkill’7.
Sediment samples were dried at 50 °C, weighed and washed through a 63 μm mesh, dried and weighed again. The size fraction >250 μm was separated by dry sieving. On average, 10–12 specimens of the planktonic foraminifera species G. ruber (white) were picked from the >250 μm size fraction. Only clean foraminifera specimens of approximately the same size were selected. Measurements of stable oxygen and carbon isotopes were performed on a Thermo DeltaPlus mass spectrometer equipped with a GasBench 2 carbonate preparation device. The isotope values were calibrated versus NBS 19 (National Bureau of Standards) and the in-house standard ‘Standard Bremen’ (Solnhofen limestone). Isotope values are reported in per mil (‰) relative to the VPDB (Vienna Pee Dee Belemnite) scale. The analytical precision (1−sigma value) as obtained from 11 replicate Standard Bremen measurements was on average 0.058‰ for δ18O and 0.044‰ for δ18C. Only the oxygen-isotope data are reported in this paper.
Eleven AMS 14C dates were obtained for core MD03-2614G principally within the period of Sporormiella decline (Supplementary Table 1). Sample KIA 22661 was comprised of Pterpoda taken from the >250 μm size fraction and was prepared at the Leibniz Laboratory for Radiometric Dating and Stable Isotope Research. The sample was treated with 15% H2O2 in an ultrasonic bath followed by 100% H3PO4 at 90 °C produce CO2. The CO2 was reduced with H2 at 600 °C using a Fe catalyst and the resulting ion–graphite mixture was packed into a target and measured. The following 10 samples were comprised of monospecific planktic foraminifera picked from the >250 μm size fraction of washed sediment. These 10 samples were prepared at the INSTAAR Laboratory for AMS Radiocarbon Preparation and Research (NSRL) before measurement by Accelerator Mass Spectrometry at the Keck Carbon Cycle AMS Laboratory at the UC Irvine (KCCAMS). Foraminifera were leached for 5 min in a 0.001 M solution of HCl. Each sample was then reacted with H3PO4 and the CO2 produced was cryogenically purified. The purified CO2 was reduced with H2 in the presence of a Fe catalyst and the resulting graphite was packed into AMS targets and measured.
Tuning and tie-points. The age model for core MD03-2614G was established by tuning the G. ruber δ18O curve from MD03-2614G to nearby planktonic δ18O records from the Great Australian Bight45,46, Vostock ice core Deuterium (ref. 47) and the globally stacked benthic δ18O record48 (Supplementary Table 2). Reference curves were chosen for core intervals of comparable resolution49. The Globigerina bulloides δ18O curve was well in phase from the last glacial maximum (LGM) to 37 kyr ago but offset below. Radiocarbon dates were given preference to accomplish the graphic correlation with different reference curves.
Bayesian age modelling. The planktonic δ18O and radiocarbon ages were used to develop an age model using a P_sequence deposition model in OxCal 4.2 (refs 50, 51) with General Outlier analysis detection (probability=0.05)52. The 14C ages were calibrated using the Marine13 calibration data set17. To accommodate possible changes in the marine reservoir age, a Delta_R of 91±54 14C years was used (determined from the 14CHRONO Marine Reservoir Database at http://calib.org/marine/). Using Bayes’ theorem, the algorithms employed sample possible solutions with a probability that is the product of the prior and likelihood probabilities. Taking into account the deposition model and the actual age measurements, the posterior probability densities quantify the most likely age distributions; the outlier option was used to detect ages that fall outside the calibration model for each group, and if necessary, down-weight their contribution to the final age estimates. Modelled ages are reported here as thousands of calendar years BP, kyr or ka and plotted against depth (Supplementary Fig. 1).
The terrigenous fraction of the sediment represents continental run-off and wind-blown dust in the <63 μm size fraction. The sand-sized fraction >63 μm is almost entirely composed of pelagic carbonate particles, such as planktonic foraminifera, pteropods and coccoliths, as well as benthic foraminifera and bryozoan debris. Bulk sediment samples were dried at 50 °C and finely ground in an agate mortar. Total organic and total carbon were analysed with a Leco CS200 furnace. The accuracy is 0.2% according to 52 parallel measurements of a commercial Leco standard. The proportion of organic carbon was subtracted from total carbon to calculate the carbonate content of the bulk sediment. The non-carbonate fraction was calculated as 100% CaCO3.
Pollen preparation and counting
A total of 39 samples were analysed in this study. Samples of ∼4–5 cm3 each were processed using the following method. Sub-sampled sediment was suspended in ∼40 ml of 10% sodium pyrophosphate followed by sieving over 210 and 7 μm mesh. The sediment fraction retained was treated with 10% HCl then acetolysis (10 min) and heavy liquid separation (sodium polytungstate S.G. 2.0, 20 min at 2,000 r.p.m.; 2 × ). A known amount of Lycopodium spores was added to the samples before processing to allow calculation of pollen and charcoal concentrations. Slides were mounted with glycerol and sealed with paraffin wax. Pollen was generally well preserved and abundant throughout the core. Pollen was counted along evenly spaced transects at magnification of × 630 on a Zeiss Axioskop. The average number of pollen counted per sample was ∼230 grains. Pollen percentages were calculated on a pollen sum consisting of all angiosperms and gymnosperms pollen grains counted (that is, excluding pteridophyte and fungal spores).
Charcoal fragments larger than 10 μm were counted along three equally spaced transects of each sample slide and results presented as percentages of the dryland pollen sum.
Sporormiella identification and counting
Identification of Sporormiella was made according to the following criteria. They are ascospores with a sigmoid germinal aperture extending the entire length of the cell. Cells are 12–28 μm × 9–15 μm and are present as two types; end cells show one flattened and one round end, middle cells show two flattened ends53 (Supplementary Fig. 2). Sporormiella spores were calculated as a percentage of the pollen sum.
Palynological results and statistical analyses
A summary pollen diagram with the results of the palynological analysis is presented in Supplementary Fig. 3. Zonation of the pollen diagram was made using the outcome of stratigraphically constrained cluster analysis (CONISS routine)54. The 12 major pollen taxa (shown on Supplementary Fig. 3) were used in CONISS; all minor taxa, charcoal and Sporormiella were excluded. The main divisions of the diagram were placed at ∼70 and 15 kyr ago and the resulting zonation concurs with the per-eye interpretation of the pollen data and confirms that significant vegetation change took place at ∼70 kyr ago, coincident with the reduction in fire. The CONISS results also indicate that Sporormiella decline is not associated with major changes in vegetation.
Ramp function regression and bootstrap re-sampling (RAMPFIT)55 were applied to the Sporormiella data to quantify uncertainties. The RAMPFIT output confirms the per-eye interpretation of the Sporormiella curve and places the onset of the decline at 44.966±0.851 kyr ago and the completion at 43.087±0.645 kyr ago, with the number of Sporormiella spores decreasing from 9.694±0.412% to 2.041±0.729% (Supplementary Table 3, 4; Supplementary Fig. 5).
Data on the physical properties of core MD03-2614G are archived in the PANGAEA database (doi:10.1594/PANGAEA.131767). Radiocarbon dating was supported by the NSF’s Archaeology and Archaeometry Program (BCS-0914821). All relevant data are available from the authors.
How to cite this article: van der Kaars, S. et al. Humans rather than climate the primary cause of Pleistocene megafaunal extinction in Australia. Nat. Commun. 8, 14142 doi: 10.1038/ncomms14142 (2017).
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Barnosky, A. D., Koch, P. L., Feranec, R. S., Wing, S. L. & Shabel, A. B. Assessing the causes of late Pleistocene extinctions on the continents. Science 306, 70–75 (2016).
Cooper, A. et al. Abrupt warming events drove Late Pleistocene Holarctic megafaunal turnover. Science 349, 602–606 (2015).
Wroe, S. et al. Climate change frames debate over the extinction of megafauna in Sahul (Pleistocene Australia-New Guinea). Proc. Natl Acad. Sci. USA 110, 8777–8781 (2013).
Webb, S. Megafauna demography and late Quaternary climatic change in Australia: a predisposition to extinction. Boreas 37, 329–345 (2008).
Wroe, S. & Field, J. A review of the evidence for a human role in the extinction of Australian megafauna and an alternative interpretation. Quat. Sci. Rev. 24, 2692–2703 (2006).
Brook, B. W. et al. Would the Australian megafauna have become extinct if humans had never colonised the continent? Comments on ‘A review of the evidence for a human role in the extinction of Australian megafauna and an alternative explanation’ by Wroe, S. & Field, J. Quat. Sci. Rev. 25, 560–564 (2007).
Brook, B. W. & Johnson, C. N. Selective hunting of juveniles as a cause of the imperceptible overkill of the Australian Pleistocene megafauna. Alcheringa 30, 39–48 (2006).
Johnson, C. N. Australia’s Mammal Extinctions: a 50,000 Year History Cambridge University Press (2006).
Miller, G. et al. Human predation contributed to the extinction of the Australian megafaunal bird Genyornis newtoni ∼47 ka. Nat. Commun. 7, 10496 (2016).
Miller, G. H. et al. Pleistocene extinction of Genyornis newtoni: human impact on Australian megafauna. Science 283, 205–208 (1999).
Metcalf, J. L. et al. Synergistic roles of climate warming and human occupation in Patagonian megafaunal extinctions during the Last Deglaciation. Sci. Adv. 2, e1501682 (2016).
Saltré, F. et al. Climate change not to blame for late Quaternary megafauna extinctions in Australia. Nat. Commun. 7, 10511 (2016).
Miller, G. H. et al. Ecosystem collapse in Pleistocene Australia and a human role in megafaunal extinction. Science 309, 287–290 (2005).
Gillespie, R., Brooks, B. W. & Baynes, A. Short overlap of humans and megafauna in Pleistocene Australia. Alcheringa 30, 163–186 (2006).
Roberts, R. G. et al. New ages for the last Australian megafauna: continent-wide extinction about 46,000 years ago. Science 292, 1888–1892 (2001).
O’Connell, J. F. & Allen, J. The process, biotic impact, and global implications of the human colonization of Sahul about 47,000 years ago. J. Archaeol. Sci. 56, 73–84 (2015).
Reimer, P. J. et al. IntCal13 and Marine13 radiocarbon age calibration curves 0–50,000 years cal BP. Radiocarbon 55, 1869–1887 (2013).
Hamm, G. et al. Cultural innovation and megafauna interaction in the early settlement of arid Australia. Nature 539, 280–283 (2016).
Turney, C. S. M. et al. Early human occupation at Devil’s Lair, southwestern Australia 50,000 years ago. Quat. Res. 55, 3–13 (2001).
Cullen, L. E. & Grierson, P. F. Multi-decadal scale variability in autumn-winter rainfall in south-western Australia since 1655 AD as reconstructed from tree rings of Callitris columellaris. Clim. Dyn. 33, 433–444 (2009).
Hope, P., Timbal, B. & Fawcett, R. Associations between rainfall variability in the southwest and southeast of Australia and their evolution through time. Int. J. Clim. 30, 1360–1371 (2010).
Turney, C. S. M. et al. Tropical and mid-latitude forcing of continental Antarctic temperatures. Cryosphere 9, 2405–3415 (2015).
Cook, L. G., Hardy, N. B. & Crisp, M. D. Three explanations for biodiversity hotspots: small range size, geographical overlap and time for species accumulation. An Australian case study. New Phytol. 207, 390–400 (2015).
Pearce, R. H. & Barbetti, M. A 38,000-year-old archaeological site at Upper Swan, Western Australia. Archaeol Oceania 16, 168–172 (1981).
Byrne, M. Evidence for multiple refugia at different time scales during Pleistocene climatic oscillations in southern Australia inferred from phylogeography. Quat. Sci. Rev. 27, 2576–2585 (2008).
Kershaw, A. P., van der Kaars, S. & Flenley, J. R. in Tropical Rainforest Responses to Climatic Change 2nd edn, (eds Bush, M. B. et al.) 85–124 (Springer-Verlag, 2011).
Kershaw, A. P., Bretherton, S. C. & van der Kaars, S. A complete pollen record of the last 230 ka from Lynch’s Crater, north-eastern Australia. Palaeogeogr. Palaeoclimatol. Palaeoecol 251, 23–45 (2007).
Moss, P. T. & Kershaw, A. P. The last glacial cycle from the humid tropics of northeastern Australia: comparison of a terrestrial and a marine record. Palaeogeogr. Palaeoclimatol. Palaeoecol 155, 162–176 (2000).
Cohen, T. J. et al. Hydrological transformation coincided with megafaunal extinction in central Australia. Geology 43, 195–198 (2015).
van der Kaars, S. & De Deckker, P. A Late Quaternary pollen record from deep-sea core Fr10/95, GC17 offshore Cape Range Peninsula, northwestern Western Australia. Rev. Palaeobot. Palynol. 120, 17–37 (2002).
Kershaw, A. P., Clark, J. S., Gill, A. M. & D’Costa, D. M. in Flammable Australia: The fire regimes and biodiversity of a continent (eds Bradstock, R. A. et al.) 3–25 (Cambridge University Press, 2002).
Davis, O. K. & Shafer, D. S. Sporormiella fungal spores, a palynological means of detecting herbivore density. Palaeogeogr. Palaeoclimatol. Palaeoecol 237, 40–50 (2006).
Davis, O. K. Spores of the dung fungus Sporormiella: increased abundance in historic sediments and before Pleistocene megafaunal extinction. Quat. Res. 28, 290–294 (1987).
Burney, D. A., Robinson, G. S. & Burney, L. P. Sporormiella and the late Holocene extinctions in Madagascar. Proc. Natl Acad. Sci. USA 100, 10800–10805 (2003).
Wood, J. R. & Wilmhurst, J. M. Wetland soil moisture complicates the use of Sporormiella to trace past herbivore populations. J. Quat. Sci. 27, 254–259 (2012).
Gill, J. L. et al. Linking abundances of the dung fungus Sporormiella to the density of bison: implications for assessing grazing by megaherbivores in paleorecords. J. Ecol. 101, 1125–1136 (2013).
Johnson, C. N. et al. Using dung fungi to interpret decline and extinction of megaherbivores: problems and solutions. Quat. Sci. Rev. 24, 107–113 (2015).
Gill, J. L., Williams, J. W., Jackson, S. T., Lininger, K. B. & Robinson, G. S. Pleistocene megafaunal collapse, novel plant communities, and enhanced fire regimes in North America. Science 326, 1100–1103 (2009).
Davis, O. K. & Shafer, D. S. Sporormiella fungal spores, a palynological means of detecting herbivore density. Palaeogeogr. Palaeoclimatol. Palaeoecol. 237, 40–50 (2006).
Robinson, G. S., Pigott Burney, L. & Burney, D. A. Landscape paleoecology and megafaunal extinction in southeastern New York State. Ecol. Monogr. 75, 295–315 (2005).
Grellett-Tinner, G., Spooner, N. A. & Worthy, T. H. Is the ‘Genyornis’ egg of a mihirung or another extinct bird from the Australian dreamtime? Quat. Sci. Rev. 133, 147–164 (2016).
Miller, G. H., Fogel, M. L., Magee, J. W. & Clarke, S. J. The Genyornis egg: a commentary on Grellet-Tinner et al. Quat. Sci. Rev (in the press).
Pate, F. D., McDowell, M. C., Wells, R. T. & Smith, A. M. Additional AMS radiocarbon dates for Wet Cave and the timing of megafaunal extinctions in the Naracoorte region of South Australia. Alcheringa 30, 277–279 (2006).
Rule, S. et al. The aftermath of megafaunal extinction: ecosystem transformation in Pleistocene Australia. Science 335, 1483–1486 (2012).
Andres, M. S. Late Quaternary paleoceanography of the Great Australian Bight: a geochemical and sedimentological study of cool-water carbonates, ODP Leg 182, Site 1127. Diss. ETH 14831, 1–189 (2002).
Calvo, E., Pelejero, C., De Deckker, P. & Logan, G. A. Antarctic deglacial pattern in a 30 kyr record of sea surface temperature offshore South Australia. Geophys. Res. Lett. 34, L13707 (2007).
Petit, J. R. et al. Climate and atmospheric history of the past 420000 years from the Vostok ice core, Antarctica. Nature 399, 429–436 (1999).
Liesicki, L. E. & Raymo, M. E. A Pliocene-Pleistocene stack of 57 globally distributed benthic δ18O records. Paleoceanography 20, PA1003 (2005).
Pahnke, K., Zahn, R., Elderfield, H. & Schulz, M. 340,000-year centennial-scale marine record of Southern Hemisphere climatic oscillation. Science 301, 948–952 (2003).
Ramsey, C. B. Radiocarbon dating: revolutions in understanding. Archaeometry 50, 249–275 (2008).
Bronk Ramsey, C. & Lee, S. Recent and planned developments of the program OxCal. Radiocarbon 55, 720–730 (2013).
Ramsey, C. B. Dealing with outliers and offsets in radiocarbon dating. Radiocarbon 51, 1023–1045 (2011).
Cook, E. J., van Geel, B., van der Kaars, S. & van Arkel, J. A review of the use of non-pollen palynomorphs in palaeoecology with examples from Australia. Palynology 36, 155–178 (2011).
Grimm, E. C. CONISS: a FORTRAN 77 program for stratigraphically constrained cluster analysis by the method of incremental sum of squares. Comput. Geosci. 13, 13–35 (1987).
Mudelsee, M. Ramp function regression: a tool for quantifying climate transitions. Comput. Geosci. 26, 293–307 (2000).
AUSLIG. Vegetation. Atlas of Australian Resources Vol. 6, Division of National Mapping (1990).
New, M., Lister, D., Hulme, M. & Makin, I. A high-resolution data set of surface climate over global land areas. Clim. Res. 21, 1–25 (2002).
Wessel, P., Smith, W. H. F., Scharroo, R., Luis, J. & Wobbe, F. Generic mapping tools: improved version released. EOS Trans. AGU 94, 409–410 (2013).
We acknowledge funding from the German Research Foundation (DFG) for sediment coring with R/V Marion Defresne during the AUSCAN voyage (Grant NU60/11-1). G.H.M acknowledges NSF grant BCS-0914821 for the radiocarbon dating,
The authors declare no competing financial interests.
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van der Kaars, S., Miller, G., Turney, C. et al. Humans rather than climate the primary cause of Pleistocene megafaunal extinction in Australia. Nat Commun 8, 14142 (2017). https://doi.org/10.1038/ncomms14142
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