Bolide impact triggered the Late Triassic extinction event in equatorial Panthalassa.

Extinctions within major pelagic groups (e.g., radiolarians and conodonts) occurred in a stepwise fashion during the last 15 Myr of the Triassic. Although a marked decline in the diversity of pelagic faunas began at the end of the middle Norian, the cause of the middle Norian extinction is uncertain. Here we show a possible link between the end-middle Norian radiolarian extinction and a bolide impact. Two palaeoenvironmental events occurred during the initial phase of the radiolarian extinction interval: (1) a post-impact shutdown of primary and biogenic silica production within a time span of 10(4)-10(5) yr, and (2) a sustained reduction in the sinking flux of radiolarian silica for ~0.3 Myr after the impact. The catastrophic collapse of the pelagic ecosystem at this time was probably the dominant factor responsible for the end-middle Norian conodont extinction.

The biodivern class="Chemical">sipan>ty crin class="Chemical">sis at the Triasn class="Chemical">sic–Jurassic boundary (TJB) has traditionally been identified as one of the “big five” mass extinctions of the Phanerozoic1. Although diversity depletions at the end-Ordovician, end-Permian, and end-Cretaceous intervals resulted exclusively from elevated levels of extinction, the TJB diversity loss was primarily the result of attrition related to reduced origination, along with a higher background extinction rate in the Late Triassic23. Available biostratigraphic data suggest that prominent faunal groups in the marine realm, such as radiolarians, conodonts, and ammonoids, experienced a three-step extinction during the last 15 Myr of the Late Triassic: at the end of the middle Norian, at the end of the Norian, and at the end of the Rhaetian (Fig. 1). Catastrophic processes, such as episodes of anoxia and mantle plume volcanism, in the Central Atlantic Magmatic Province (CAMP) have been proposed to account for the second (end-Norian) and third (end-Rhaetian) extinction events456. However, the cause of the initial (end-middle Norian) extinction event has been uncertain, despite the fact that it was apparently of global extent.

Figure 1

Osmium isotope values, generic diversity, and palaeogeography in the Late Triassic.

(a) Late Triassic generic diversities of radiolarians23, conodonts41, and Pacific (North American) ammonoids40, as compared with the Os isotope record945 in the Panthalassa Ocean. The abrupt decrease in the 187Os/188Os ratio in the middle Norian is synchronous with the Manicouagan impact event at 214–215 Ma. Stepwise or episodic extinctions in the (1) end-middle Norian, (2) end-Norian, and (3) end-Triassic are possibly linked with a large bolide impact7, an oceanic anoxic event (OAE)4, and the Central Atlantic Magmatic Province (CAMP) volcanic event56, respectively. The gradual decrease in radiolarian diversity just prior to the end-middle Norian may have occurred within radiolarian biozone 6B. Gray shaded areas in the radiolarian and conodont generic diversities represent the number of genera; the genera first appear in the upper Norian and Rhaetian. The geological time scale is from refs 46 and 47. Triassic radiolarian fossil zones (FZ) and their age correlations are from refs 7, 20 and 48; the biostratigraphic framework for our age model is shown in Supplementary Fig. S2. (b) Late Triassic palaeogeographic map showing approximate locations of the Manicouagan carter and the inferred depositional area of the bedded chert in the Mino Belt, in low-latitude zones of the Panthalassa Ocean11. The map is created using ACD Systems Canvas Draw software (Version 2.0).

Here, we show that the remarkable turnover of papan class="Chemical">n class="Chemical">siliceous planpan>kton (radiolarians) in the end-middle Norian was triggered by a large impact event. Such an event has been inferred from anomalous concentrations of platinum group elements (PGEs)78 and negative Os isotope excursions9 in a claystone layer in an Upper Triassic bedded chert succesn class="Chemical">sion in the Sakahogi section, Japan (Supplementary Fig. S1), which accumulated in a deep seafloor environment in an equatorial region of the palaeo-Pacific Ocean (Panthalassa)1011. The claystone layer is 4–5 cm thick and contains a lower and an upper sublayer (Supplementary Fig. S3). The lower sublayer contains microspherules in a matrix of clay minerals (mainly illite), cryptocrystalline quartz, and hematite. The upper sublayer is composed of undisturbed clay minerals (illite) and cryptocrystalline quartz. The late middle Norian age of the clay layer711 suggests that the PGE anomalies and microspherules in the lower sublayer originated from an extraterrestrial source, related to an impact event that formed the 90-km-diameter Manicouagan crater in Canada (214–215 Ma)1213. In addition, a magnetostratigraphic analysis shows a normal polarity interpretation for the clay layer11, which is consistent with the palaeomagnetic data for the Manicouagan melt rock14. Studies of PGEs and Os isotopes have revealed that the anomalously high PGE abundances in the lower sublayer resulted from a large chondritic impactor with a diameter of 3.3–7.8 km (refs 8 and 9). An impactor of this size would produce a crater of ~56–101 km in diameter8, assuming an impactor entry velocity of 20 km s−1, an entry angle of 45° and a crystalline target (density = 2750 kg m−3). The size range of such a crater is consistent with the size of the Manicouagan crater (diameter, ~90 km)15. Outside of Japan, a Norian impact ejecta deposit with shocked quartz and spherules has been found in an Upper Triassic nonmarine sequence in southwestern Great Britain, which has yielded a diagenetic age (from authigenic K-feldspar) of 214 ± 2.5 Ma (ref. 16). Although the recalculated age of 216.7 Ma for the British ejecta deposit using the method of Renne and coworkers1718 is slightly outside the range of the Manoucouagan impact event age, a strong mineral correspondence between samples from Manicouagan and the ejecta deposit provides convincing evidence that the Manicouagan impact was the source of the Great Britain ejecta deposit19.

Results

Extinction and origination patterns

We anpapan class="Chemical">n class="Chemical">alysed a large dataset of Upper Triasnpan> class="Chemical">sic radiolarian occurrences in the Inuyama area7202122, to assess the magnitude of the extinction event caused by the middle Norian impact, and to compare this event with extinction events at other stage boundaries. An analysis of the stratigraphic ranges of radiolarian species in Japan indicates a dramatic increase in extinction and origination rates across the impact horizon (Fig. 2). Radiolarians show similar (and relatively low) extinction and origination rates throughout much of the late Carnian–middle Norian. Across the ejecta horizon, a dramatic increase in extinction rate is observed in the 1-Myr interval following the impact event. Such a high extinction rate of radiolarians has not been recognized within the Norian interval23, and surprisingly, the magnitude of the extinction event is substantially higher than that of the radiolarian extinction at the TJB21. Radiolarian species diversity data show a steady decrease in diversity throughout the late Carnian to middle Norian. A sharp increase in diversity is observed across the ejecta horizon, and the diversity reaches a maximum value of 40 species (without singletons) during the late Norian. The diversity then declines rapidly throughout the Rhaetian, reaching a low point in the Hettangian (19 species). These results suggest that the middle Norian impact triggered the extinction and contemporaneous evolutionary radiation of the radiolarian fauna in the equatorial Panthalassa Ocean.

Figure 2

Extinction and origination rates of Late Triassic radiolarian species in the Panthalassa Ocean.

The extinction rate of the middle Norian impact event is substantially higher than the rate at the Triassic–Jurassic boundary (TJB). Error bars are one standard deviation, estimated from bootstrap resampling of the stratigraphic ranges of species with 1000 iterations. See Supplementary Fig. S2 for the age model.

Biostratigraphy and chemostratigraphy

An apan class="Chemical">nalysis of patterns of radiolarian extinction (Fig. 2) reveals a high extinction rate in the 1 Myr interval after the impact event. To determine whether the extinctions were coincident with the impact event, we conducted a detailed bed-by-bed biostratigraphic analysis of the ~2 Myr interval across the ejecta horizon (Fig. 3). Our biostratigraphic analysis of the study section clearly shows that the impact event initiated the radiolarian extinction and the evolutionary radiation of new taxa. The present data show no catastrophic pattern24 of radiolarian extinctions at the impact event horizon. However, gradual extinctions of radiolarians are observed within ~1 m above the ejecta horizon, in the end-middle Norian (Fig. 3). A biostratigraphic analysis shows that 14 middle Norian taxa gradually disappeared during this interval, including all Capnodoce and most Capnuchosphaera species. An initial phase of diversification (phase D1) started in the upper sublayer of the claystone and in the overlying chert bed. A second major wave of diversification (phase D2) is observed ~33 cm above the ejecta horizon. Given an average sedimentation rate of 1.1 mm kyr−1 in the middle Norian chert succession (Supplementary Fig. S2), this second diversification occurred within ~0.3 Myr after the impact event.

Figure 3

Biostratigraphy and chemostratigraphy of the middle–upper Norian.

Stratigraphic profiles of Os isotope ratios9, organic carbon isotopes, mass accumulation rates of biogenic silica, and radiolarian biostratigraphy in bedded cherts of the Sakahogi section. Biostratigraphic ranges of 29 radiolarian species in the study interval at Sakahogi show extinctions of middle Norian species (red) corresponding with successive blooms of opportunistic species (purple) and radiations of new species (blue). Dashed lines mark the initial (D1) and second (D2) phases of diversification of upper Norian radiolarian species. For an explanation of radiolarian taxon ranges, see Supplementary Table S4.

To evn class="Chemical">alpan>uate changes in primary productivity, we examined stratigraphic variations in organic n class="Chemical">carbon isotopic values (δ13Corg) from the study section at Sakahogi (Supplementary Table S1). The data show that δ13Corg values are relatively constant below the ejecta claystone (average δ13Corg, −25.22‰), but that a negative δ13Corg excursion is present in the upper claystone sublayer (Fig. 3). The δ13Corg values increase rapidly upwards, and then recover to pre-impact levels at the first chert bed overlying the claystone layer (−25.13‰). Above the claystone interval, δ13Corg values vary from −27.09‰ to −24.57‰ (average δ13Corg, −25.44‰).

Discussion

A preliminary bipapan class="Chemical">n class="Chemical">ostranpan> class="Chemical">tigraphic study of the section at Sakahogi shows that most of the middle Norian radiolarian taxa are present in the 30 cm interval above the ejecta layer, and apparently survived well into the late Norian7 (Supplementary Fig. S4). However, our new biostratigraphic data collected from above the previously sampled horizon indicate that extinctions of middle Norian species occurred in a stepwise fashion in the ~1 m interval above the ejecta horizon. Furthermore, our high-resolution palaeontological and geochemical data reveal that two palaeoenvironmental events occurred during the initial phase of the radiolarian extinction interval (Fig. 3). The first event (E1) consisted of the post-impact shutdown of primary productivity and a remarkable decline in the amount of biogenic silica preserved before the first phase of diversification (D1). The second event (E2) consisted of a large and sustained reduction in the sinking flux of radiolarian silica and the proliferation of siliceous sponges, occurring before the second phase of diversification (D2) and lasting for ~0.3 Myr after the impact.

During the ipan class="Chemical">nin class="Chemical">tin class="Chemical">al E1 event, the post-impact reduction in primary productivity occurred during deposition of the clay layer, as suggested by the negative δ13Corg excursion observed in the claystone. Concentrations of TOC with low δ13Corg values could be interpreted to represent a change in the proportion of organic matter derived from land plants versus oceans2526. However, low and relatively stable C/N ratios (mean, 1.8; standard deviation, 0.6) throughout the study section indicate that contributions of land-derived organic matter are minor to absent. The rapid decrease in the biogenic silica content in the claystone (Supplementary Table S3) further indicates that the productivity of silica-secreting radiolarians was sharply reduced, and that marine primary productivity declined during the initial E1 event. Laboratory studies show that radiolarians prey on phytoplankton, such as dinoflagellates, haptophytes, and thecate nonmotile algae2728; however, we know little about the ecological factors that influence radiolarian productivity. A decline in radiolarian production in the near-surface zone may imply major changes at the base of the marine food chain, such as a substantial reduction in primary productivity or a shift toward primary producers not favored by pre-impact taxa.

The negapapan class="Chemical">n class="Chemical">tive δ13Corg excurnpan> class="Chemical">sion and the rapid decrease in biogenic SiO2 content observed in the upper part of the claystone occurs within a 3.2-cm-thick section, suggesting a very short time scale for the E1 event. We used previously published 187Os/188Os ratio results9 to estimate the duration of low-productivity conditions after the impact. Previous studies have revealed that 187Os/188Os ratios declined abruptly, from 0.477 to 0.126, in the lower sublayer of the claystone. This excursion can be interpreted as a result of the mixing of ambient seawater Os (characterized by relatively high 187Os/188Os ratios) with meteoritic Os (characterized by low 187Os/188Os ratios); the meteoric Os was vaporized at the time of the impact and was subsequently dissolved into seawater. The 187Os/188Os ratio, which is lowest in the lower sublayer, gradually increases towards the upper sublayer, and reaches pre-impact levels in chert samples overlying the claystone layer. No discrete extraterrestrial particles were observed in the upper sublayer claystone, which indicates that the 187Os/188Os ratio of this sublayer records the Os isotope composition of ancient seawater9. Therefore, the recovery of 187Os/188Os values in the upper sublayer claystone after the impact event may reflect post-impact removal of excess dissolved meteoritic Os from seawater, which occurred over a period of 104–105 yr, as Os residence times range from 10 to 60 kyr (refs 29 and 30). Although the marine residence time of Os in the Late Triassic is not precisely known, deposition of the upper sublayer clay may have occurred over the period 104–105 yr after the impact event. This interval is hypothesized to represent the duration required for the restoration of productivity by primary and silica-secreting organisms after the middle Norian impact. However, simulations using an ocean–atmosphere/carbon-cycle model31, which suggest a global collapse of primary productivity (in the Strangelove Ocean) resulting in the delivery and cycling of carbon in the oceans and on land, cannot explain such short-term (104–105 yr) shifts in δ13Corg values across the ejecta layer. The global implications of the magnitude and short duration of the negative δ13Corg excursion reported here remain to be verified at other middle–late Norian boundary intervals worldwide.

Following the resurgepan class="Chemical">nce in primary producn class="Chemical">tivity after the E1 event, the biogenic npan> class="Chemical">silica content had recovered to pre-impact values by the first chert bed overlying the claystone layer. However, our analysis reveals that major biotic components of the bedded chert changed temporarily from radiolarians to siliceous sponges, for ~0.3 Myr after the impact. Assuming a constant sedimentation rate in the middle–upper Norian chert succession of 1.1–1.6 mm kyr−1, and a constant dissolution rate of biogenic silica during that time, the mass accumulation rates (MAR) of radiolarian silica in the pre-impact chert beds is estimated at ~0.1 g cm−2 kyr−1, which is the same as the biogenic silica flux near the equator in the modern Pacific Ocean (0.1–0.3 g cm−2 kyr−1)32. After the impact event, the MAR decreased to 0.02 ± 0.01 g cm−2 kyr−1 in the upper sublayer claystone, and then remained low during the deposition of sponge spicule-rich cherts. On the other hand, the MAR of the siliceous sponge silica increased markedly across the claystone layer of the ejecta deposit, from ~0.01 to ~0.08 g cm−2 kyr−1, and subsequently decreased to ~0.01 g cm−2 kyr−1 after the E2 event. Our data and previous data9 on terrigenous elements (e.g., Ti, Al, and K) indicate that the flux of terrestrial components (aeolian dust) derived from continental crust2233 did not change substantially through the study interval; thus, the significant and sustained reduction in the flux of radiolarian silica appears to have coincided with an increasing volume of siliceous sponge spicules. During the Mesozoic, the concentration gradient caused by the export of silica from surface to deep waters by sinking of marine plankton may not have been as intense as in modern diatom-dominated oceans34, and such concentration gradients in any case would have been briefly interrupted by fluctuations in radiolarian productivity. Even lacking a direct record of Triassic silica concentrations, it is likely that a reduction in radiolarian productivity in the Panthalassa Ocean during the E2 event, which probably increased the amount of dissolved silicic acid in seawater, favored the proliferation of siliceous sponges after the impact event. Laboratory experiments on silicon uptake by siliceous sponges reveal that an increased concentration of silicic acid in water has a striking positive effect on both the size and robustness of siliceous sponge spicules35. Our hypothesis that dissolved silicic acid increased in seawater at the time of the E2 event is supported by the observation that longer and more robust skeletons of siliceous sponge spicules were dominant only in the spicules of the spicule-rich chert (Supplementary Fig. S10).

Decreases in the papan class="Chemical">n class="Chemical">sinpan>king flux of radiolarian n class="Chemical">silica during the E1 and E2 events may reflect a decline in radiolarian production in middle Norian taxa, including in Capnodoce and Capnuchosphaera species. These middle Norian radiolarians are very rare above the E1 intervn class="Chemical">al, whereas a small spumellarian species is abundant within the E2 interval; this spumellarian species is reported as Spumellaria gen. et sp. indet. A, and its occurrence can be used to identify the stratigraphic position of the ejecta layer in other Triassic chert sections within the Jurassic accretionary complexes in Japan9. These taxa can be considered as short-lived opportunistic species, as they disappeared at the end of the radiolarian faunal turnover interval. The present biostratigraphic analysis also reveals that radiation of late Norian taxa was contemporaneous with a temporal bloom in the numbers of opportunistic spumellarian species in the E2 interval. The timing of these radiation events suggests that the decrease in radiolarian biomass in the middle Norian taxa enhanced the bloom of opportunistic radiolarian species and the evolutionary radiation of late Norian taxa in the E1 and E2 intervals. Hence, the gradual extinction of middle Norian radiolarian taxa during the ~1 Myr period could be explained by ecological pressures imposed by late Norian taxa, provided that the late Norian taxa were more rapidly growing and more efficient phytoplankton feeders than the middle Norian taxa. These unusual radiation patterns are similar to those observed in the Panthalassic TJB sections in Japan and Canada2122. As with the TJB event, changes in seawater acidity, temperature, and/or a reduced nutrient levels in ocean surface waters are possible drivers for the decline in the production of middle Norian radiolarian taxa. The primary cause of this decline is difficult to identify, but the relatively long period of the E2 interval (~0.3 Myr after the impact) largely excludes the possibility that the decline was triggered by instantaneous environmental stresses (e.g., extended darkness, global cooling, or acid rain2436) that would have been caused by a bolide impact.

Did the middle–late Noriapan class="Chemical">n exn class="Chemical">tincnpan> class="Chemical">tion event occur uniformly on a global scale, or does it represent a regional phenomenon in the Panthalassa Ocean? The record of radiolarian faunal change across the middle–upper Norian boundary has been established at the species level in several regions3738, showing that widespread and apparently sudden extinctions affected the Subfamily Capnodocinae and Family Capnuchosphaeridae at the boundary23. As a first approximation, it is probably reasonable to assume that a geographically widespread faunal change across the middle–upper Norian boundary was related to an impact event that triggered the radiolarian extinction in the equatorial Panthalassan Ocean. Existing radiolarian records are not sufficiently precise to constrain these relationships with biostratigraphic resolutions comparable to those presented here for the middle–upper Norian. Further biostratigraphic analyses of middle–upper Norian boundary sections will be required to validate this hypothesis.

We propn class="Chemical">ospan>e that the impact event was probably the major factor responpan>sible for the conodont and Pacific (North American) ammonoid extinctions that occurred in the middle–upper Norian boundary394041. The base of the Epigondolella bidentata conodont zone and the base of the Gnomohn class="Chemical">alorites cordilleranus ammonoid zone in western North America3940 define the position of the middle–upper Norian boundary that is most closely aligned with the traditional base of the Sevatian41, and which can be correlated with the radiolarian extinction interval in the study section in Japan. Although ammonoids are absent in the studied section, the biostratigraphic record of conodonts suggests that a few Parvigondolella species survived across the ejecta layer, but that an important middle Norian Epigondolella species became extinct just below the impact horizon (Supplementary Fig. S11). The present data also show the first appearance of late Norian Epigondolella species in the E1 and E2 intervals. Conspicuous morphological changes occur in this genus across the ejecta layer; Epigondolella species below the ejecta layer are characterized by a wide platform, whereas those above the ejecta layer possess a longer and more narrow platform. The catastrophic collapse of the pelagic ecosystem during the E1 and E2 events was probably the major factor responsible for the conodont turnover that occurred at the end of the middle Norian.

This study has reven class="Chemical">alpan>ed that late middle Norian open-ocean ecn class="Chemical">osystems experienced profound disruptions after a large impact event (chondritic impactor of 3.3–7.8 km in diameter), and that the event was posn class="Chemical">sibly related to the 90-km-diameter Manicouagan crater in Canada. Although many marine sections over the past 540 Myr have been examined, no catastrophic collapse in marine ecosystems caused by an extraterrestrial impact has yet been described, with the outstanding exception of the Cretaceous–Paleogene boundary (KPB) crisis24 and the middle Norian event reported here. Given that no large volcanic events occurred in the Norian3, the fossil record of the middle–upper Norian is key to evaluating the general importance of impacts as causes of biotic and environmental changes in pelagic ecosystems.

Methods

Biostratigraphy

To extract radiolarians for bipapan class="Chemical">n class="Chemical">ostranpan> class="Chemical">tigraphic analyses, 53 chert samples were soaked in a dilute HF solution (5%) for 24 h, and were then passed through a 32-μm mesh sieve. This treatment was repeated 2–5 times to obtain sufficient residue for analysis. After drying the residue, radiolarians were handpicked under a binocular microscope and were observed using a scanning electron microscope. Conodonts were handpicked from the same residues used for the radiolarian biostratigraphy.

Carbon isotope and major element analyses

Samples for whole-rock geochemicn class="Chemical">alpan> analysis were collected from 45 n class="Chemical">chert and claystone beds across the ejecta layer. Veins and strongly recrystallized/weathered parts of the samples were avoided to minimize the effects of diagenetic and metamorphic overprinting on the sediment geochemistry. Samples were crushed and fragments were carefully hand-picked to avoid contamination by altered and weathered materials. These hand-picked fragments were then pulverized in an agate mortar for carbon isotope analysis. All glassware used in the analyses was baked for 3 h at 450 °C, and all tools were cleaned with methanol between uses to avoid organic carbon contamination. Approximately 0.8 g of each sample was treated with an excess of 6 M hydrochloric acid for 48 h at 60 °C. Samples were then rinsed five times with ultrapure water (>18 MΩ) and dried. Carbon isotope ratios and carbon and nitrogen contents were measured using an elemental analyser (FlashEA 1112) coupled to a Thermo-Finnigan Delta Plus Advantage isotope ratio mass spectrometer at the Centre for Advanced Marine Core Research, Kochi University, Japan. Isotopic measurements were repeated two times for 19 samples across the claystone (ejecta) layer to check the reproducibility of the results. The carbon isotope ratios were calculated using standard Alanine; the precision of the organic carbon ratio (δ13Corg) determinations was ± 0.5‰. The analyses showed good reproducibility of values, with 3% or less fluctuation (average, 2%; N = 18). All isotopic results are reported in conventional delta (δ) notation, defined as per mill (‰) deviations from the Vienna Peedee Belemnite (VPDB) standard value.

Major element (papan class="Chemical">n class="Chemical">Si, npan> class="Chemical">Ti, Al, Fe, Mn, Mg, Ca, Na, K, and P) contents of the bulk-sediment samples from the cherts and claystones in the Sakahogi section were measured using a Rigaku ZSX Primus II X-ray fluorescence (XRF) spectrometer at the University of Tokyo. After drying the powdered samples at 110 °C for ~12 h, loss on ignition (LOI) was calculated from the weight loss during ignition at 950 °C for over 6 h. Fused glass beads for XRF analysis were made from a mixture of 0.4 g of ignited sample powder and 4 g of lithium tetraborate (Li2B4O7) flux at ~1190 °C for 7 min in a Pt crucible. The analytical results were generally within 3% (relative percent difference) of accepted values of reference material JB-2, issued by the Geological Survey of Japan42.

Diversity measurements

Regionpapan class="Chemical">n class="Chemical">al species-level divernpan> class="Chemical">sities of radiolarians throughout the Carnian to Hettangian were measured in 10 chert sequences in the Inuyama area, Japan. The data comprise 2196 occurrences of 156 radiolarian species from 361 stratigraphic levels in the study sections; the collection intensity was uniform and without sampling gaps (Supplementary Fig. S2). Species ranges were analysed using metrics established by Foote43, including: total diversity, total diversity minus singletons, estimated mean standing diversity, per-taxon rate, and the Van Valen rate. Extinction (E) and origination (O) rates reported here were calculated for 1-Myr intervals using Foote’s per-taxon rate:

where n class="Chemical">pan class="Chemical">Nbt is the npan>umber of taxa crn class="Chemical">osn class="Chemical">sing both the bottom and top of an interval, NbL is the number of taxa crossing the bottom but not the top of the interval, and NFt is the number of taxa first appearing in the interval and crossing the top of the interval. Errors for the extinction and origination rates are represented by one standard deviation determined in each direction of a bootstrap resampling of the stratigraphic ranges of species based on 1000 iterations. To estimate per-taxon rates for the 1-Myr intervals, we constructed an age model for the Upper Triassic bedded chert sequence based on the average sedimentation rate estimated from the measured thickness and the time interval of its deposition. Extinction and origination patterns of radiolarian species show that the derived rates for all four metrics used (i.e. per-taxon rate, per-taxon rate without singletons, Van Valen with singletons, and Van Valen without singletons) have similar values. Consequently, only the per-taxon rate with singletons is discussed.

Productivity reconstruction

The Triasn class="Chemical">sipan>c bedded n class="Chemical">cherts in the Inuyama area comprise biogenic n class="Chemical">silica (radiolarian tests and siliceous sponge spicules) and terrestrial components derived from the continental crust (aeolian dust)2233. Biogenic silica (BSi) was calculated as follows:

where PAAS is a shn class="Chemical">alpan>e standard based onpan> the composition of post-Archean average Austrn class="Chemical">alian shales44. In this calculation, the amount of terrigenous Si that is mainly supplied by aeolian dusts is subtracted from the total concentration of Si in the bedded cherts. To assess the relative contributions of the radiolarian and sponge silica to the BSi, we determined the volumetric composition of radiolarians and siliceous sponges three times by standard 300-grain points counts (grain-solid method) for 118 thin sections. The percentages of radiolarian and sponge silica (Sirad and Sisponge, respectively) were then calculated as follows:

where Vrad and Vspopan class="Chemical">nge are the volumetric compn class="Chemical">ositions of the radiolarians and siliceous sponges based on thin section analysis, respectively. Then, the mass accumulation rate (g cm−2 kyr−1) of radiolarian and sponge silica (MARrad and MARsponge, respectively) was calculated as follows:

where ρ is the bulk denpapan class="Chemical">n class="Chemical">sity of npan> class="Chemical">chert (2.46 g cm−3) or claystone (1.69 g cm−3) and a is the sedimentation rate for chert (0.11–0.16 cm kyr−1) or claystone (0.09 cm kyr−1). The sedimentation rate of the claystone layer was calculated from the measured thickness (3.2 cm), and the time interval of its deposition was estimated using a mean oceanic residence time of Os (~3.5 kyr)29, as discussed above.

Additional Information

How to cite this arn class="Chemical">tipan>cle: Onoue, T. et n class="Chemical">al. Bolide impact triggered the Late Triasn class="Chemical">sic extinction event in equatorial Panthalassa. Sci. Rep. 6, 29609; doi: 10.1038/srep29609 (2016).