Skip to main content

Thank you for visiting You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

Uppermost Triassic phosphorites from Williston Lake, Canada: link to fluctuating euxinic-anoxic conditions in northeastern Panthalassa before the end-Triassic mass extinction


The end-Triassic mass extinction (ETE) is associated with a rise in CO2 due to eruptions of the Central Atlantic Magmatic Province (CAMP), and had a particularly dramatic effect on the Modern Fauna, so an understanding of the conditions that led to the ETE has relevance to current rising CO2 levels. Here, we report multiple phosphorite deposits in strata that immediately precede the ETE at Williston Lake, Canada, which allow the paleoenvironmental conditions leading up to the mass extinction to be investigated. The predominance of phosphatic coated grains within phoshorites indicates reworking in shallow water environments. Raman spectroscopy reveals that the phosphorites contain organic carbon, and petrographic and scanning electron microscopic analyses reveal that the phosphorites contain putative microfossils, potentially suggesting microbial involvement in a direct or indirect way. Thus, we favor a mechanism of phosphogenesis that involves microbial polyphosphate metabolism in which phosphatic deposits typically form at the interface of euxinic/anoxic and oxic conditions. When combined with data from deeper water deposits (Kennecott Point) far to the southwest, it would appear a very broad area of northeastern Panthalassa experienced anoxic to euxinic bottom water conditions in the direct lead up to the end-Triassic mass extinction. Such a scenario implies expansion and shallowing of the oxygen minimum zone across a very broad area of northeastern Panthalassa, which potentially created a stressful environment for benthic metazoan communities. Studies of the pre-extinction interval from different sites across the globe are required to resolve the chronology and spatial distribution of processes that governed before the major environmental collapse that caused the ETE. Results from this study demonstrate that fluctuating anoxic and euxinic conditions could have been potentially responsible for reduced ecosystem stability before the onset of CAMP volcanism, at least at the regional scale.


The end-Triassic mass extinction (ETE) appears nearly coincident with the emplacement of the Central Atlantic Magmatic Province (CAMP) ~201.51 million years ago1,2,3,4,5. Approximately 80% of all marine and terrestrial species became extinct during the ETE making it the second biggest biodiversity6,7 and the third biggest ecological crisis8 during the Phanerozoic. Proposed causes of the mass extinction include CAMP-related global warming4,9,10, global cooling11, ocean acidification12,13,14,15, sea-level changes16, and ocean anoxia3,16,17,18. The knowledge base of the conditions leading up to the ETE is poorly resolved, as the main focus has remained on the timing associated with an initial emplacement of CAMP. Yet, recent studies of the pre-extinction interval reveal biotic, climatic and geochemical changes before the onset of known CAMP volcanism19,20,21,22. Here, we present the first detailed study investigating the genesis of Upper Triassic phosphorite deposits from Williston Lake, British Columbia, which intriguingly occur directly before the ETE interval (Figs. 1 and 2).

Figure 1

Paleogeography and modern location of study localities. (a) Early Jurassic paleogeographic reconstruction with the approximate paleolocation of Williston Lake sites after Greene et al.14 and Kennecott Point site after Kasprak et al.18, and outlined area within Pangaea showing the extent of CAMP. (b) Map of the studied localities at Williston Lake, British Columbia modified from Wignall et al.24 1 = Black Bear Ridge (56.08758333°N, 123.04388889°W), 2 = Pardonet Creek (56.03527778°N, 123.03500000°W), 3 = Ne Parle Pas (56.01682778°N, 123.08305556°W).

Figure 2

Stratigraphic columns of studied sections showing depositional environment. Green arrows show the position of studied samples depicted in the figures below. Placement of Initial Carbon Isotope Excursion is after Wignall et al.24. Volcano marks the end-Triassic mass extinction. Aragonite fans described in Greene et al.15 Pr. Fm = Pardonet Formation.

Phosphorite beds at Williston Lake are predominantly composed of phosphatic coated grains. Deposits containing phosphatic coated grains are rare throughout the Phanerozoic and their origin remains incompletely understood23,24,25. It is widely accepted that direct precipitation of phosphates occurs near the sediment-water interface and requires distinct environmental conditions26,27,28,29. Formation of authigenic phosphorites (phosphogenesis) is generally associated with microbial polyphosphate metabolism and biogeochemical processes where steep, or temporally dynamic, redox gradient conditions occur26,27,28. Pufahl and Grimm29 suggested that phosphatic coated grains are proxies for fluctuations in organic carbon flux and primary productivity. Our study suggests that the formation of these phosphatic coated grain deposits was microbially mediated based on textural features and Raman spectroscopy. While phosphorites are an indicator of steep or dynamically-variable redox gradient conditions, the occurrence of benthic macrofauna within phosphatic beds implies that transient oxygenation events occurred during phosphogenesis24. Our results demonstrate a development of oxygen restricted conditions, which would be stressful to most benthic metazoans established in shelf waters off northeastern Panthalassa prior to the ETE and preceding the earliest known CAMP volcanism.

Study area

Exposures of the Fernie Formation along Williston Lake, British Columbia, Canada span the Triassic/Jurassic boundary and include the record of the entire Rhaetian Stage, the final stage of the Triassic across different environments24 (Fig. 2). The siliciclastic-carbonate strata were deposited in a foreland basin on the western side of the Pangaean continental shelf 30,31 (Fig. 1). The Rhaetian Stage is marked by sea-level fall followed by a major transgression at the end of the Rhaetian coincident with an initial worldwide negative carbon isotope excursion24,31(Fig. 2).

We investigated three sections (Ne Parle Pas Point, Pardonet Creek, and Black Bear Ridge) that contain phosphorite deposits in the interval immediately preceding the ETE. The sea-level fall during the Rhaetian generated a major hiatus in the more proximal Black Bear Ridge section such that nearly the entire Rhaetian sequence is missing at this locality; nevertheless, a veneer of phosphatic coated grains is preserved at the sequence boundary. Strata recording a more complete Rhaetian Stage are at the distal sites of Ne Parle Pas Point and Pardonet Creek where both sites record lowstand strata missing at the Black Bear Ridge locality (Fig. 2). The upper 13 m of the Ne Parle Pas section and the upper 3.5 m of the Pardonet Creek sequence consist of calcareous siltstone interbedded with phosphatic grainstone beds recording a transition from offshore to lower shoreface depositional environments (Fig. 2). In general, phosphorite accumulations are associated with a condensed, transgressive record32, yet intriguingly Williston Lake phosphorites are deposited within the regressive sequence24 (Fig. 2).


Description of phosphorite deposits

The phosphorite beds studied here represent high-energy phosphatic grainstone beds that vary from 5 to 40 cm in thickness (Fig. 2). The grainstone beds represent storm events sandwiched between calcareous siltstone to sandstone deposits. Phosphatic clasts were transported from a shallower part of the shelf to the deeper offshore transition zone during high-energy, storm-related events as evidenced by fragmented grains, rip-ups, phosphate grapestones and scouring surfaces between fine-grained siltstone and coarse-grained phosphatic grainstone beds (Fig. 3A,B,E,F). The phosphorite deposits predominantly consist of phosphatic coated grains with some peloids, muscovite, quartz silt, bioclasts and phosphatic pebbles embedded in a sparry calcite matrix. According to Wignall et al.24, the phosphatic units contain some of the more biotically diverse assemblages versus surrounding units, and include infaunal and epifaunal bivalves, nautiloids, ammonoids, and echinoderms. In all localities, phosphatic coated grains vary in shape from spheroids to ellipsoids and are predominantly fragmented due to reworking and winnowing (Fig. 3A). Occasionally phosphatic coated grains embedded in a phosphatic matrix are present (Fig. 3B). Phosphatic coated grains are 50 to 380 μm in diameter, more commonly between 100 and 150 μm. Phosphatic cortices are uniformly composed of Ca-phosphate (apatite) while nuclei composition includes sedimentary clasts (most common), quartz, feldspar, and shell fragments. The nuclei of phosphatic coated grains are coated by concentric phosphatic laminae, which vary in thickness and alternate between light brown and dark brown layers (Fig. 3C,D). Concentric layers are irregular in places replicating the shape of the nucleus and occasional objects within laminae (Fig. 3C,D). The presence of concentric and irregular laminations along with unaltered bioclasts suggest the primary origin of phosphatic coated grains excluding the possibility of diagenetic replacement.

Figure 3

Photomicrographs of phosphatic coated grains (PCG). All images are in plane-polarized light. (a) Fragmented phosphatic coated grains. Note size and shape variation. Sample PC 10. (b) Phosphatic coated grains embedded within phosphatic crust resembling grapestone structure with phosphatic peloids. Sample NPP17.5. (c) Light and dark brown concentric laminations. White arrow points to the divergence area where outer laminae replicate shape of a clast within cortex. Red arrow points to unaltered shell fragment within the cortex of phosphatic coated grain. Sample PC 7. (d) Phosphatic coated grain with irregular concentric laminations. Sample NPP 17.5. (e) Coarser grained P-rich sediment separated by scouring surface from underlying finer-grained sediment. Sample NPP 16. (f) Bivalve clasts filled with silt and peloids that were ripped up and transported by storms. PC7

Samples dissolved in acetic acid from the Ne Parle Pas site that contain nuclei composed of calcium carbonate intraclasts reveal phosphatized tubes (Fig. 4C). Phosphatized tubes are between 2 and 3 microns in diameter creating an interwoven network identical in shape, size, and structure to endolithic borings33. Thus, these carbonate intraclasts were infested by euendoliths during “normal” conditions followed by rapid phosphatization before micritization could occur.

Figure 4

Photomicrographs and SEM images of putative microbial structures, euendolith borings, and pyrite framboids. (a) SEM image of microscopic spherical cavities (~0.5 – 1 μm in diameter) within PCG cortex. Sample BBR0. (b) Close-up of image A. Sample BBR0. (c) SEM image of sample dissolved in acetic acid, which reveals phosphatized euendolith borings (dashed line). Sample NPP 17.5. (d) Photomicrograph in plane-polarized light of filamentous structures (black arrows) within phosphate and microscopical spherical cavities with distinct rim (red arrows) resembling microbial remains. Sample PC 7. (e) SEM image of sample dissolved in acetic acid, which reveals an aggregation of pyrite framboids. Sample NPP 17.5. (f) Backscatter SEM image of pyrite framboids within phosphate. Sample PC 7.

Microbial mineralization

Raman spectroscopy is widely used as an analytical tool for differentiation between carbonaceous material of biogenic versus abiogenic origin in the rock record. At all Williston Lake localities, micro Raman spectroscopy documents intense and broad bands occurring at around 1350 cm−1 (D band) and 1600 cm−1 (G band) within phosphatic cortices which are diagnostic of organic matter (kerogen)34 (Fig. 5A). Further analysis of the deconvoluted carbon first-order spectrum derived from the D-G spectrum seen in Fig. 5A shows five bands resolved into Gaussian bands where the high difference between bands D and D4 can be observed (Fig. 5A). The second derivative spectra of the D and G bands illustrate that the G band doesn’t have a doublet on the negative peak (Fig. 5B). Both differences in D4 and D bands and the absence of a doublet on the negative peak of the G band corroborate the presence of disordered carbonaceous matter, likely of biological origin, within the phosphorites34. In contrast, Raman spectroscopic analysis conducted on the matrix and nuclei of phosphatic coated grains does not record features that support the presence of any kind of carbonaceous material (Fig. C, D).

Figure 5

Raman spectroscopic analysis. (a) Representative Raman spectrum of phosphate cortex showing high intensity peaks of D-G bands and deconvolution of D and G bands modeled by six Gaussian peaks below (fitted peaks are scaled for clarity). High intensity peaks of D-G bands and big difference between bands D4 and D verify the biogenic origin of carbonaceous matter34. Sample PC7. (b) The second derivative spectra derived from the first order carbon spectra (A) shows no negative doublet on the negative peak at the G band (see red arrow) corroborating the presence of biogenic carbonaceous material within phosphate cortices. Sample PC7. (c) Representative Raman spectrum of calcareous matrix showing low intensity peaks of D-G bands and deconvolution of D and G bands modeled by three Gaussian peaks below (fitted peaks are scaled for clarity). CC = calcite. Sample PC7. (d) The second derivative spectra derived from the first order carbon spectra (C) shows absence of any intensity within D-G bands corroborating the absence of biogenic carbonaceous material within calcareous matrix. Sample PC7. (e) Representative Raman spectrum of nuclei of PCG showing low intensity peaks of D-G bands. QTZ = quartz. Sample PC7.

SEM and petrographic examinations of studied samples show microscopic spherical cavities (0.5 to 1 μm in diameter) within phosphatic coated grains cortices (Fig. 4A,B,D). Photomicrographs of these cavities reveal a distinct rim and hollow core structure that rules out the possibility of abiotic precipitates that resemble microbial forms35. Cosmidis et al.36 documented coccus-like and rod-like biomorphs in a Miocene/Pliocene Peruvian phosphatic crust that are identical in shape, size and distribution to our microscopic spherical objects. Salama et al.37 showed that microspheres (0.5 to 2.5 μm in diameter) embedded in carbonaceous matrix from Upper Cretaceous phosphatic peloids are fossilized remains of coccoidal bacteria. Both studies concluded that the observed microspheres were once a part of microbial colonies that formed near the oxic-anoxic boundary in zones of sulfate reduction36,37. Thin section observations revealed the presence of curved filamentous structures, ~1 μm in width and varying in length from 5 to 27 μm (Fig. 4D), which we interpret as putative microbial remains. Observed microscopical spherical cavities and filamentous morphotypes within carbonaceous material indicate the bacterial origin of relatively diverse microbial communities.

The evidence for microbial mineralization is unsurprising as all of the currently accepted mechanisms of marine phosphogenesis require microbes to concentrate P either in a direct or an indirect way36. We would like to emphasize that the presence of microbes within the cortices of phosphatic coated grains do not necessarily imply their direct role in the apatite accretion within phosphatic coated grains, although such a scenario is plausible, but rather that they may have played a fundamental role in the delivery of P via polyphosphate metabolism. Documented pyrite framboids within phosphoclasts imply the presence of sulfide likely provided by sulfate reducing bacteria in reducing conditions38 (Fig. 4E,F). This is in accordance with the study by Wignall et al.24 which documented euxinic conditions based on framboidal size at Williston Lake sections.


Modern and ancient phosphorite deposits are mainly associated with oceanic upwelling regions associated with hypoxic oxygen-minimum zones (OMZ) overlying organic-rich sediments e.g.27,28. In such regions, phosphogenesis is thought to be driven by microbes that concentrate P as part of polyphosphate metabolism27,28,38, with the colorless sulfur bacteria, in addition to others, commonly considered key players. The sulfur bacteria live at interfaces between organic rich, sulfidic conditions below and oxic conditions above, and are thought to accumulate polyphosphate in order to help survive during prolonged, but fluctuating anoxic and sulfidic conditions35. Thus, many sedimentary phosphate concentrations indicate that environmental conditions cycled between oxic and euxinic/anoxic during phosphogenesis.

Mechanisms of authigenic apatite precipitation that do not involve polyphosphate metabolism include the sourcing of P from vertebrate bone39, or from dissolving Fe-oxide-bearing mineral phases, again under stratified redox conditions27,40. While these P sources are plausible drivers of Williston Lake phosphogenesis, we do not favor them as explanations. In the former case, fish bones are not abundant in the Williston Lake deposits and they do not serve as nuclei for the phosphatic coated grains. Similarly, with respect to P being concentrated through adsorption and subsequent dissolution of iron hydroxides, we would expect this mechanism to operate in a system dominated by iron-rich siliciclastic deposition, as opposed to the organic-rich system here that contains pyrite (Fig. 4E,F), indicating a sulfide-dominated depositional environment such as those that favor phosphogensis via concentration through microbial polyphosphate metabolism41,42.

Here, we consider the presence of phosphatic coated grains to indicate conditions fluctuated between oxic and sulfidic conditions in shallow water as a result of intensified oceanic upwelling and OMZ expansion in the lead up to the ETE in northeastern Panthalassa. The presence of phosphorites suggests that the foreland basin was well-connected to the ocean at the time of phosphogenesis. Models investigating genesis of phosphatic coated grains from Arning et al.26 and Pufahl and Grimm29 propose that phosphatic coated grains are deposited near the sediment-water interface (upper 5-20 cm of sediment) in organic-rich sediment under suboxic to anoxic conditions where repeated reworking of phosphatic grains and fluctuation of redox conditions play a crucial role. Although phosphatic coated grains are sometimes referred to as phospho-ooids, the process responsible for phospho-ooid formation is different from carbonate ooids, which precipitate by wave agitation in supersaturated waters with calcium carbonate37, while the apatite in phosphatic coated grains precipitates authigenically below the sediment-water interface29. We suggest that these phosphatic coated grains formed between storm and fair weather wave-base, but specifically in proximity to the wave-agitation zone where they were more prone to episodic reworking and mixing by storms and where the upwelling front would be best developed and intensified32. High-energy storm events reworked phosphate clasts further transporting them to the current place of deposition (phosphatic grainstone beds). The infilling of microbial borings in carbonate clasts by phosphate indicates relatively rapid phosphatization, before the borings were infilled by cements, or the microbial borers could fully micritize the carbonate grains (Fig. 4C).

The presence of putative microbial fossils within the phosphate cortices lends credence to a microbial involvement either in an indirect way by concentrating high amounts of P or in a direct way by facilitating an actual apatite accretion. The fact that the phosphatic beds contain macrofauna suggests a strong association with transient oxic conditions during which benthic metazoa colonized the seafloor until the next euxinic/anoxic event24. Taken together, the presence of phosphorites indicates a dynamic environment that shifted between oxic, hypoxic and possibly anoxic or euxinic conditions in the time preceding the ETE. Our study demonstrates evidence supporting microbial mineralization during the phosphogenesis either in a direct or an indirect way, likely by polyphosphate-metabolizing bacteria, similar to those that mediate phosphogenesis in modern settings that fluctuate between oxic and euxininc/anoxic conditions25,38.

Schoepfer et al.20 and Kasprak et al.18 investigated an open ocean, deep-water section (~200-500 m water depth) from northeastern Panthalassa, spanning the Triassic-Jurassic boundary several hundred km to the west of Williston Lake, at Kennecott Point, British Columbia (Fig. 1). Both of these studies interpret nitrogen-limited conditions, water-column stratification and deoxygenation at Kennecott Point through an ~10 m-thick interval, estimated to represent approximately half a million years20 before the ETE using geochemical and biomarker proxies. Although precise geochronology is problematic at Williston Lake, the timing of biogeochemical disturbance at Kennecott Point coincides well with deposition of the upper Rhaetian phosphate grainstone beds. Given that the Kennecott Point (deep) and Williston Lake (relatively shallow) sites are likely contemporaneous, it would appear that a broad area of northeastern Panthalassa experienced fluctuating euxinic-anoxic conditions in the lead up to the ETE, beginning ~500 kyr before the extinction. Fluctuating, oxygen-restricted conditions likely created a hostile environment for benthic fauna at least in shallow water settings where most benthos are less adapted to low oxygen conditions. For example, off the coast of Oregon, recent intensified upwelling brought oxygen-poor waters to shallow shelf depths (<50 m) where emergent anoxia nearly eradicated the macroscopic benthic invertebrate community and initiated the development of sulfide-oxidizing bacterial mats43. At Williston Lake sites, Wignall et al.24 documented the demise of shallow-water infaunal bivalves right before the initial negative carbon isotope excursion marking the major environmental collapse of the ETE. This stressed environment potentially made marine biota more susceptible to subsequent cascading effects from CAMP emplacement, at least in northeastern Panthalassa.

Photic zone euxinia combined with anoxic conditions is considered to be a potent mechanism for the ETE since these conditions are widely documented in Panthalassic and Tethys basins during the ETE3,18. It is worth noting that the first appearance of euxinia on the shelves, as suggested by the presence of upper Rhaetian phosphorites, could indeed precede the onset of CAMP volcanism, adding to the growing dataset that environmental conditions began to deteriorate before the beginning of CAMP volcanism in different parts of the globe19,20,22. Dike and sill intrusions in organic rich sediments in Brazil were proposed as a potential mechanism that drove the climate change preceding the onset of CAMP volcanism19,21,44. Study44 using pedogenic carbonate isotopes as a proxy for temperature variations has documented two periods of extreme temperature increase by 6 °C in congruence with atmospheric CO2 rise preceding the ETE. Thus, it is worth considering that intensified oceanic upwelling and OMZ expansion in northeastern Panthalassa was possibly related to climate warming as a result of higher pCO2. Additional studies are required to reveal conditions leading up the ETE which governed on the regional versus global scale.


Spectroscopic, petrographic and SEM investigations on the genesis of uppermost Triassic phosphorites from Williston Lake, British Columbia, provide evidence supporting microbially-induced mineralization, likely by polyphosphate-accumulating bacteria. The genesis of phosphatic coated grains requires deposition near the sediment-water interface under suboxic to anoxic conditions where repeated reworking of phosphatic grains and fluctuation of redox conditions play an essential role26,29. Our study provides direct biosedimentary evidence that fluctuating euxinic-anoxic conditions existed in relatively shallow marine settings (above storm-wave base) preceding the ETE in northeastern Panthalassa. These results are compatible with previous studies of Schoepfter et al.20 and Kasprak et al.,18 from the deep-water Kennecott Point section, suggesting that environmental disturbances, likely episodic euxinia, preceded the ETE for approximately 500 kyr. For the first time, our study shows that euxinic-anoxic conditions existed not just in the deeper part of the northeastern Panthalassic basin prior to the ETE, but also in shallow water settings of the foreland basin covering a very broad area of northeastern Panthalassa. Intervals of phosphogenesis are linked to periods of an intensified oceanic upwelling and OMZ expansion where possibly sulfide-oxidizing microbial communities were thriving inducing apatite precipitation, while the benthic biota flourished in between euxinic/anoxic intervals, at least at the Williston Lake region. Such conditions were likely stressful for shallow water benthic metazoans making them more susceptible to cascading effects from CAMP volcanism. Additional studies from Panthalassic and Tethys basins are required to further elucidate conditions leading up to the ETE at the regional and global scale and their effects on ecosystems.


Specimens from different phosphatic horizons covering all three studied sections were examined. Standard petrographic microscopy was performed on thin sections using a Zeiss Axio Imager.M2m equipped with a Zeiss HRc camera. Internal grain structure and elemental composition were investigated on a FEI Nova NanoSEM 450 in back-scattered electron mode with the help of an Energy-dispersive X-ray spectroscopy microprobe. To determine mineral content and the presence of kerogen, we used a Horiba XploRa PLUS Raman Microscope and Horiba XGT-7200 X-ray fluorescence microscope. Samples were dissolved in 10% acetic solution for 72 hours in order to observe the morphology of phosphatic clasts.

Data availability

All data generated or analysed during this study are included in this published article. All figures were created by authors of the paper.


  1. 1.

    Schaller, M. F., Wright, J. D., Kent, D. V. & Olsen, P. E. Rapid emplacement of the Central Atlantic Magmatic Province as a net sink for CO2. Earth and Planet. Sci. Lett 323–324, 27–39 (2012).

    ADS  Article  CAS  Google Scholar 

  2. 2.

    Blackburn, T. J. et al. Zircon U-Pb geochronology links the end-Triassic extinction with the Central Atlantic Magmatic Province. Science 340, 941–945 (2013).

    ADS  CAS  PubMed  Article  PubMed Central  Google Scholar 

  3. 3.

    Jaraula, C. M. et al. Elevated pCO2 leading to Late Triassic extinction, persistent photic zone euxinia, and rising sea levels. Geology 41, 955–958 (2013).

    ADS  CAS  Article  Google Scholar 

  4. 4.

    Pálfy, J. & Kocsis, A. T. Volcanism of the Central Atlantic magmatic province as the trigger of environmental and biotic changes around the Triassic–Jurassic boundary. Volcanism, Impacts and Mass Extinctions: Causes and Effects. Geol. Soc. of Am. Sp. Paper 505, 245–261 (2014).

    Google Scholar 

  5. 5.

    Thibodeau, A. M. et al. Mercury anomalies and the timing of biotic recovery following the end-Triassic mass extinction. Nature. Communications 7, 11147 (2016).

    CAS  Google Scholar 

  6. 6.

    Sepkoski, J. Patterns of Phanerozoic extinction: a perspective from global data bases in Global events and event stratigraphy in the Phanerozoic. (ed. Walliser, O. H.) 35-51 (Springer, 1996).

  7. 7.

    Alroy, J. et al. The shifting balance of diversity among major marine animal groups. Science 329, 1191–1194 (2010). cm−1

    ADS  CAS  PubMed  Article  Google Scholar 

  8. 8.

    McGhee, G. R. Jr, Sheehan, P. M., Bottjer, D. J. & Droser, M. L. Ecological ranking of Phanerozoic biodiversity crises: ecological and taxonomic severities are decoupled. Palaeogeogr. Palaeoclimatol., Palaeoecol. 211, 289–297 (2004).

    Article  Google Scholar 

  9. 9.

    McElwain, J. C., Beerling, D. J. & Woodward, F. I. Fossil plants and global warming at the Triassic-Jurassic boundary. Science 285, 1386–1390 (1999).

    CAS  PubMed  Article  Google Scholar 

  10. 10.

    Wignall, P. B. Large igneous provinces and mass extinctions. Earth Sci. Rev 53, 1–33 (2001).

    ADS  CAS  Article  Google Scholar 

  11. 11.

    Guex, J., Bartolini, A., Atudorei, V. & Taylor, D. High-resolution ammonite and carbon isotope stratigraphy across the Triassic–Jurassic boundary at New York Canyon (Nevada). Earth Planet. Sci. Lett. 225, 29–41 (2004).

    ADS  CAS  Article  Google Scholar 

  12. 12.

    Hautmann, M., Benton, M. J. & Tomasovych, A. Catastrophic ocean acidification at the Triassic-Jurassic boundary. N. Jb. Geol. Palaont. Abh 249, 119–127 (2008).

    Article  Google Scholar 

  13. 13.

    Kiessling, W., Aberhan, M., Brenneis, B. & Wagner, P. J. Extinction trajectories of benthic organisms across the Triassic–Jurassic boundary. Palaeogeogr. Palaeoclimatol. Palaeoecol 244, 201–222 (2007).

    Article  Google Scholar 

  14. 14.

    Greene, S. E. et al. Recognising ocean acidification in deep time: An evaluation of the evidence for acidification across the Triassic-Jurassic boundary. Earth Sci. Rev 113, 72–93 (2012).

    ADS  CAS  Article  Google Scholar 

  15. 15.

    Greene, S. E., Bottjer, D. J., Corsetti, F. A., Berelson, W. M. & Zonneveld, J. P. A subseafloor carbonate factory across the Triassic-Jurassic transition. Geology 40, 1043–1046 (2012).

    ADS  CAS  Article  Google Scholar 

  16. 16.

    Hallam, A. A revised sea-level curve for the early Jurassic. Journal of the Geological Society 138, 735–743 (1981).

    ADS  Article  Google Scholar 

  17. 17.

    Hallam, A. & Wignall, P. B. Facies changes across the Triassic–Jurassic boundary in Nevada, USA. J. Geol. Soc. 157, 49–54 (2000).

    ADS  CAS  Article  Google Scholar 

  18. 18.

    Kasprak, A. H. et al. Episodic photic zone euxinia in the northeastern Panthalassic Ocean during the end-Triassic extinction. Geology 43, 307–310 (2015).

    ADS  CAS  Article  Google Scholar 

  19. 19.

    Ruhl, M. & Kürschner, W. M. Multiple phases of carbon cycle disturbance from large igneous province formation at the Triassic-Jurassic transition. Geology 39, 431–434 (2011).

    ADS  CAS  Article  Google Scholar 

  20. 20.

    Schoepfer, S. D., Algeo, T. J., Ward, P. D., Williford, K. H. & Haggart, J. W. Testing the limits in a greenhouse ocean: Did low nitrogen availability limit marine productivity during the end-Triassic mass extinction? Earth Planet. Sci. Lett. 451, 138–148 (2016).

    ADS  CAS  Article  Google Scholar 

  21. 21.

    Davies, J. H. et al. End-Triassic mass extinction started by intrusive CAMP activity. Nature Communications 8, 15596 (2017).

    ADS  CAS  PubMed  PubMed Central  Article  Google Scholar 

  22. 22.

    Yager, J. A. et al. Duration of and decoupling between carbon isotope excursions during the end-Triassic mass extinction and Central Atlantic Magmatic Province emplacement. Earth Planet. Sci. Lett. 473, 227–236 (2017).

    ADS  CAS  Article  Google Scholar 

  23. 23.

    Piecha, M. A considerable hiatus at the Frasnian/Famennian boundary in the Rhenish shelf region of northwest Germany. Palaeogeogr. Palaeoclimatol. Palaeoecol 181, 195–211 (2002).

    Article  Google Scholar 

  24. 24.

    Wignall, P. B. et al. The end Triassic mass extinction record of Williston Lake, British Columbia. Palaeogr. Palaeoclimatol. Palaeoecol 253, 385–406 (2007).

    ADS  Article  Google Scholar 

  25. 25.

    Zoss, R. et al. Microbial communities associated with phosphogenic sediments and phosphoclast‐associated DNA of the Benguela upwelling system. Geobiology, 1–15 (2018).

  26. 26.

    Arning, E. T. et al. Genesis of phosphorite crusts off Peru. Marine Geology 262, 68–81 (2009).

    ADS  CAS  Article  Google Scholar 

  27. 27.

    Crosby, C. H. & Bailey, J. The role of microbes in the formation of modern and ancient phosphatic mineral deposits. Frontiers in microbiology 3, 241 (2012).

    CAS  PubMed  PubMed Central  Article  Google Scholar 

  28. 28.

    Hiatt, E. E., Pufahl, P. K. & Edwards, C. T. Sedimentary phosphate and associated fossil bacteria in a Paleoproterozoic tidal flat in the 1.85 Ga Michigamme Formation, Michigan, USA. Sedimentary Geology 319, 24–39 (2015).

    ADS  CAS  Article  Google Scholar 

  29. 29.

    Pufahl, P. K. & Grimm, K. A. Coated phosphate grains: Proxy for physical, chemical, and ecological changes in seawater. Geology 31, 801–804 (2003).

    ADS  CAS  Article  Google Scholar 

  30. 30.

    Orchard, M. J. et al. An intercalibrated biostratigraphy of the Upper Triassic of Black Bear Ridge, Williston Lake, northeast British Columbia. Natural Resources Canada, Geological Survey of Canada, (2001).

  31. 31.

    Zonneveld, J. P., Beatty, T. W., Williford, K. H., Orchard, M. J. & McRoberts, C. A. Stratigraphy and sedimentology of the lower Black Bear Ridge section, British Columbia: candidate for the base-Norian GSSP. Stratigraphy 7, (61–82 (2010).

    Google Scholar 

  32. 32.

    Pufahl, P. K. & Groat, L. A. Sedimentary and igneous phosphate deposits: formation and exploration: an invited paper. Economic Geology 112, 483–516 (2017).

    Article  Google Scholar 

  33. 33.

    Tribollet, A. & Payri, C. Bioerosion of the coralline alga Hydrolithon onkodes by microborers in the coral reefs of Moorea, French Polynesia. Oceanologica acta 24, 329–342 (2001).

    Article  Google Scholar 

  34. 34.

    Marshall, C. P., Edwards, H. G. & Jehlicka, J. Understanding the application of Raman spectroscopy to the detection of traces of life. Astrobiology 10, 229–243 (2010).

    ADS  CAS  PubMed  Article  PubMed Central  Google Scholar 

  35. 35.

    Mänd, K. et al. Authigenesis of biomorphic apatite particles from modern upwelling zone sediments off Namibia. Geobiology 16, 640–658 (2018).

    PubMed  Article  CAS  PubMed Central  Google Scholar 

  36. 36.

    Cosmidis, J., Benzerara, K., Menguy, N. & Arning, E. Microscopy evidence of bacterial microfossils in phosphorite crusts of the Peruvian shelf: Implications for phosphogenesis mechanisms. Chemical Geology 359, 10–22 (2013).

    ADS  CAS  Article  Google Scholar 

  37. 37.

    Salama, W., El-Kammar, A., Saunders, M., Morsy, R. & Kong, C. Microbial pathways and palaeoenvironmental conditions involved in the formation of phosphorite grains, Safaga District, Egypt. Sedimentary geology 325, 41–58 (2015).

    ADS  CAS  Article  Google Scholar 

  38. 38.

    Vietti, L. A., Bailey, J. V., Fox, D. L. & Rogers, R. R. 2015, Rapid formation of framboidal sulfides on bone surfaces from a simulated marine carcass fall. Palaios 30, 327–334 (2015).

    ADS  Article  Google Scholar 

  39. 39.

    Suess, E. Phosphate regeneration from sediments of the Peru continental margin by dissolution of fish debris. Geochim. Cosmochim. Acta 45, 577–588 (1981).

    ADS  CAS  Article  Google Scholar 

  40. 40.

    Ruttenberg, K. C. & Berner, R. A. Authigenic apatite formation and burial in sediments from non-upwelling continental margin environments. Geochim. Cosmochim. Acta 57, 991–1007 (1993).

    ADS  CAS  Article  Google Scholar 

  41. 41.

    Goldhammer, T., Brüchert, V., Ferdelman, T. G. & Zabel, M. Microbial sequestration of phosphorus in anoxic upwelling sediments. Nature Geoscience 3, 557–561 (2010).

    ADS  CAS  Article  Google Scholar 

  42. 42.

    Schulz, H. N. & Schulz, D. H. Large sulfur bacteria and the formation of phosphorite. Science 307, 416–418 (2005).

    ADS  CAS  PubMed  Article  PubMed Central  Google Scholar 

  43. 43.

    Chan, F. et al. Emergence of anoxia in the California current large marine ecosystem. Science 319, 920–920 (2008).

    ADS  CAS  PubMed  Article  PubMed Central  Google Scholar 

  44. 44.

    Cleveland, D. M. et al. Pedogenic carbonate isotopes as evidence for extreme climatic events preceding the Triassic-Jurassic boundary: Implications for the biotic crisis? Geological Society of America Bulletin 120, 1408–1415 (2008).

    ADS  CAS  Article  Google Scholar 

Download references


We are grateful to Nick Rollins and Thomas Orvis for SEM assistance. This research was funded by the NSF Earth-Life Transitions (ELT) program (EAR-1338329) to FC and DB, an NSERC Discovery Grant to JPZ and by grants to EL from the American Association of Petroleum Geologists (AAPG), Geological Society of America (GSA), Society for Sedimentary Geology (SEPM) and a USC Research Enhancement Fellowship. AJC acknowledges support from the NHMLA Trelawney Endowment. We would also like to thank two anonynous reviewers for the constructive comments that improved this manuscript.

Author information




E.L., D.J.B. and F.A.C. designed research; E.L. performed research with the assistance from A.J.C. in Raman spectroscopy and wrote the paper; E.L., D.J.B. and J.P.Z., participated in field work; E.L., D.J.B., F.A.C., J.P.Z., A.J.C. and J.V.B. analyzed data and assisted in manuscript writing/revision.

Corresponding author

Correspondence to Ekaterina Larina.

Ethics declarations

Competing interests

The authors declare no competing interests.

Additional information

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

Rights and permissions

Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article’s Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit

Reprints and Permissions

About this article

Verify currency and authenticity via CrossMark

Cite this article

Larina, E., Bottjer, D.J., Corsetti, F.A. et al. Uppermost Triassic phosphorites from Williston Lake, Canada: link to fluctuating euxinic-anoxic conditions in northeastern Panthalassa before the end-Triassic mass extinction. Sci Rep 9, 18790 (2019).

Download citation

Further reading


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


Quick links

Nature Briefing

Sign up for the Nature Briefing newsletter — what matters in science, free to your inbox daily.

Get the most important science stories of the day, free in your inbox. Sign up for Nature Briefing