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Boreal earliest Triassic biotas elucidate globally depauperate hard substrate communities after the end-Permian mass extinction

Scientific Reports volume 6, Article number: 36345 (2016) | Download Citation

Abstract

The end-Permian mass extinction constituted the most devastating biotic crisis of the Phanerozoic. Its aftermath was characterized by harsh marine conditions incorporating volcanically induced oceanic warming, widespread anoxia and acidification. Bio-productivity accordingly experienced marked fluctuations. In particular, low palaeolatitude hard substrate communities from shallow seas fringing Western Pangaea and the Tethyan Realm were extremely impoverished, being dominated by monogeneric colonies of filter-feeding microconchid tubeworms. Here we present the first equivalent field data for Boreal hard substrate assemblages from the earliest Triassic (Induan) of East Greenland. This region bordered a discrete bio-realm situated at mid-high palaeolatitude (>30°N). Nevertheless, hard substrate biotas were compositionally identical to those from elsewhere, with microconchids encrusting Claraia bivalves and algal buildups on the sea floor. Biostratigraphical correlation further shows that Boreal microconchids underwent progressive tube modification and unique taxic diversification concordant with changing habitats over time. We interpret this as a post-extinction recovery and adaptive radiation sequence that mirrored coeval subequatorial faunas, and thus confirms hard substrate ecosystem depletion as a hallmark of the earliest Triassic interval globally.

Introduction

The end-Permian (P-T) mass extinction 252 Ma was the most severe biotic crisis of the Phanerozoic, initiating wholesale biodiversity collapse1,2,3,4,5,6,7. Up to 90% of all marine species are estimated to have disappeared8,9,10,11, with synchronous niche loss affecting terrestrial assemblages12,13,14. Although the underlying causes of the P-T event are not completely understood15, a primary driver might have been massive volcanic activity within the Siberian igneous province7,16,17,18,19,20. This generated excessive emissions of thermogenic methane, CO2 and SO2 that cascaded oceanic warming, acidification and anoxia/euxinia with accompanying bio-productivity decline10,16,21,22,23,24,25,26,27,28.

Ecosystem recovery after the P-T interval was seemingly protracted, but this has been reconstructed largely from the well-documented record of soft-bottom marine organisms29,30,31,32. In contrast, corresponding hard substrate assemblages remain enigmatic, primarily because of limited sampling. To date, the most informative fossils derive from the subequatorial shallow Panthalassic basins bordering Western Pangaea33, and the Tethyan margin of the South China Craton34,35. These collectively infer disappearance of rich latest Permian encrusting benthos, and its subsequent replacement in the earliest Triassic by monogeneric colonies of microconchid tubeworms – an extinct suspension-feeding clade possibly related to ‘lophophorates’36,37. However, the broader palaeobiogeographical continuity of these successions is speculative, especially with regard to mid-high palaeolatitude (>30°N) faunas from the Boreal Realm. These occupied a completely separate bio-region38 and are thus crucial for establishing globally continuous patterns. Here we document the first Early Triassic Boreal hard substrate benthic assemblages from East Greenland, a remote landmass that preserves one of the most extensive P-T marine rock sections known worldwide12,39. Our new fossils reveal compatible microconchid predominance, but with a unique Boreal signature of morphological diversification across changing depositional settings; this not only elucidates distinctive regional endemism, but also opportunistic ecosystem expansion during the initial recovery phase after the P-T boundary.

Results

Lithostratigraphy and palaeoenvironment

We systematically collected 131 bivalve shell samples and five large rock slabs, all with encrusted microconchids, from a 600 m transect through the Wordie Creek Formation39,40,41. This was exposed along the Blue River (Blåelv) and adjacent Stensiö Plateau at Kap Stosch on the Hold with Hope peninsula of East Greenland42 (Fig. 1). During the latest Permian–Early Triassic, this landmass formed part of the northwestern coastal margin of Pangaea verging on the Boreal Sea. Thick siliciclastic sequences accumulated as sub-basin infills within the burgeoning rift zone between Greenland and Norway41,43,44,45. Evidence of these deposits is today preserved at Kap Stosch (Fig. 2), as well as laterally equivalent localities on Geographical Society Ø, Traill Ø, Wegener Halvø and Jameson Land39. The lowermost beds in the Blue River section comprise the Upper Permian (Wuchiapingian) Ravnefjeld Formation, which is unconformably overlain by a shore-faceprograding deltaic sequence containing ammonoids (Hypophiceras triviale–Hypophiceras martini zones: sensu Bjerager et al.39), and constitutes the basal horizon of the Wordie Creek Formation (Fig. 3). This earliest Triassic (Induan) unit successionally trends through marine shales and mudstones with sandy–conglomeratic turbidites in the lower–middle Griesbachian Metophiceras subdemissum–Ophiceras commune ammonoid zones, to mudstones and shore-face sandstones with fluvial conglomerate in the mid–upper Griesbachian to Dienerian Wordieceras decipiensBukkenites rosenkrantzi ammonoid zones39. Dienerian strata of the Anodontophora breviformaAnodontophora fassaensis bivalve zones represent tidally-influenced paralic sandstones and overlying terrestrial red siltstones with poorly developed palaeosols, bivalves, numerous invertebrate traces, conchostracans and aquatic vertebrate remains42,43. Two thick sandstone bodies (SB II and SB III) also intercalate within these sediments, which are characteristically rich in fish fossils (actinopterygians and coelacanths) that provide a readily identifiable cross-referencing field zonation (Fish zones 1–5: sensu Nielsen42).

Figure 1: Locality.
Figure 1

Map of Greenland with enlargement of the Hold with Hope peninsula showing with the Kap Stosch field site (black circle). Modified from Nielsen42 and Bjerager et al.39. Graphics created by G.N. in CorelDraw 11, www.coreldraw.com.

Figure 2: Lithostratigraphy and fossil content.
Figure 2

(a) Schematic section of the lowermost Triassic succession at Kap Stosch with (b) microconchid morphotypes recovered from intervals 1–5. (c) Stratigraphic occurrence of associated fossils. SB II and SB III indicate major sandstone facies. Compiled and graphically drawn by G.N. in CorelDraw 11, www.coreldraw.com.

Figure 3: Biostratigraphical correlation.
Figure 3

Upper Permian–Lower Triassic ammonoid and fish zonation39,42,43 from Kap Stosch, East Greenland. Not depicted to scale. Compiled and graphically drawn by G.N. in CorelDraw 11, www.coreldraw.com.

We examined five discrete fossiliferous intervals (herein numbered 1–5: Fig. 2; see also Supplementary Fig. S1) within the Wordie Creek Formation, which yielded microconchids from the M. subdemissum, O. commune, W. decipiens and B. rosenkrantzi ammonoid zones, and A. breviforma bivalve zone respectively (Figs 2 and 3). Lithologically these horizons comprised mudstones with abundant bivalves, and locally occurring Archaeolithophyllum boundstones (=red algal carbonates) grading upwards into fine-grained sandstones. Archaeolithophyllum algae have also been reported in the earliest Triassic deposits of Jameson Land further to the south.46. Dimensionally very small pyrite framboids were recovered from intervals (1) – (M = 6.8 μm; SD = 1.5), (3) – (M = 4.4 μm; SD = 1.8), and (4) – (M = 5.6 μm; SD = 1.4). These infer dysoxic (1), to anoxic (3–4) bottom waters23, and concur with prolific occurrences of the dysaerobic soft-substrate bivalve Claraia46. The smallest framboid diameters were derived from the Archaeolithophyllum boundstones of interval (3), implying microbe-enriched local anoxia. In contrast, the absence of framboids from intervals (2) and (5), coupled with prevalent crystalline pyrite, suggests periodic oxic fluctuations23.

Microconchid assemblages

Our microconchid fossils were found attached to both Claraia shells and boundstones (Fig. 4). No other encrusting organisms were detected except for shallow (~1 mm deep) borings possibly attributable to the clionaid poriferan ichnite Entobia (Fig. 4); these were associated with a single clast from interval (3). Microconchids occurring in the boundstones infested thin calcitic sheets of Archaeolithophyllum (see thin section in Supplementary Fig. S2). Density of the microconchid encrustations ranged from 8–83 tubes/cm2 across all substrates, with the most prolific coverage on Claraia shells in intervals (1) M = 29.4 tubes/cm2, and (2) M = 22.9 tubes/cm2. Colonies attached to boundstones alternatively averaged only 11.8 tubes/cm2, but this could reflect under-sampling of the unexposed bedding planes. Abundant microconchids (M = 29.4 tubes/cm2) were also scattered randomly across the mudstone layers in interval 5 (Figs 4 and 5; see also Supplementary Fig. S3), but these had likely detached (as implied by their smooth undamaged bases and lack of adhering particles: Fig. 5) from consolidated organic substrates such as algal filaments or microbial mats47.

Figure 4: Triassic microconchids from Kap Stosch, East Greenland.
Figure 4

(a) Microconchus encrusting Claraia shells from interval (1) (PMU 28936). (b–e) Microconchus encrusting Claraia shells from interval (2): (b) PMU 28942; (c–e) PMU 28940. (f,g) Microconchus encrusting Archaeolithophyllum boundstone from interval (3) (PMU 28954, PMU 28950); black arrow in (g) indicates an uncoiled tube. (h) Dense accumulation of Spathioconchus weedoni gen. et sp. nov. distributed across mudstone bedding planes from interval (5) (PMU 28962). (i) Entobia-like borings on a carbonate clast from interval 3 (PMU 28951). Scale bars 5 mm.

Figure 5: ESEM images of selected microconchids.
Figure 5

(a) Spirally coiled Microconchus encrusting Claraia shells from interval (3) (PMU 28949). (b,c) Helically uncoiled Microconchus from interval (3) (PMU 28951). (d) Helically uncoiled Microconchus from interval (5) (PMU 28961). Scale bars 500 μm.

Individual microconchid tube shapes also varied substantially between colonies, as well as across different substrates and intervals (Fig. 2). For example, those adhering to Claraia shells in intervals (1–5) formed squat spiral tubes, whereas those attached to algal filaments within boundstones from interval (3) displayed both spiral and helically uncoiled tubes (Fig. 5). Microconchids dispersed across mudstone layers in interval (5) were helically uncoiled and upright with a convolutional basal attachment (Fig. 5). Their external ornamentation was, nonetheless, identical with fine transverse riblets and lateral striae, accompanied by prominent punctae that penetrated the microlamellar tube structure (Supplementary Fig. S4); these features are taxonomically consistent with the genus Microconchus and species such as M. valvatus48. On the other hand, a unique conical tube morphotype with diminutive globular attachment area (Fig. 6) was recovered from fine-grained facies in interval (5). Its distinctive shape, coupled with unusual attachment base, surface ornamentation and tube structure comprising coarse transverse ridges and minute punctae serve to diagnose a new taxon Spathioconchus weedoni gen. et sp. nov. (see Supplementary Note). Structural diversity in microconchid tubes49,50,51 has elsewhere been attributed to prevailing environment52, with progressive uncoiling being an adaptation to avoid burial in accumulating sediment49, or overgrowth by accreting microbial mats34. We further interpret the reduced attachment area and peculiar conical form of S. weedoni as characteristics of an upright life position and densely packed colonial arrangement.

Figure 6: Spathioconchus weedoni gen. et sp. nov.
Figure 6

(a–d) Examples showing conical tube form with small attachment base, smooth external surface and (d) adaperturally concave riblets. (e,f) Enlargement of basal attachment showing characteristic ‘nucleus’ (arrowed). (g) Holotype PMU 28962a bearing riblets at attachment base/tube border (arrowed). (h) Microlamellar tube structure interrupted by prominent punctae (arrowed). (i) Diminutive punctae (arrows) on the exfoliated tube exterior. PMU 28962. Scale bars (a–c,g) 500 μm, (d,e) 200 μm, (f) 100 μm, (h,i) 20 μm.

Discussion

The prevalence of microconchids in offshore and lower shore-face settings bordering Western Pangaea provided the original basis for positing global impoverishment of hard substrate marine ecosystems during the earliest Triassic33. Indeed, prolific microconchids have since been found in shallow and deep-water microbialites, on Claraia shells and bioclastic limestones34,35 throughout the Tethyan Realm (Fig. 7). These mainly subequatorial palaeogeographical records are complimented here by the first equivalent Boreal occurrences, which demonstrate a coherent signature of microconchid ecosystem dominance and a near total dearth of other skeletonized encrusting organisms. Previous reports of the serpulid polychaetes Spirorbis and Serpula from Kap Stosch53,54 and Jameson Land12 in East Greenland can be confidently re-identified as microconchids36. The only other hard substrate faunal element in our samples was the Entobia-like ichnite, which equates to the possible phoronid boring Talpina from Western Pangaea33; however, these traces are extremely rare suggesting that endoliths, when present, constituted a minute component of the entire biotic assemblage.

Figure 7: Palaeogeographic distribution of Early Triassic microconchids.
Figure 7

1. East Greenland12,53,54. 2. Western USA33,60. 3. Poland47. 4. Hungary66. 5. Italy8,74,75. 6. Iran74. 7. South China34,35,76,77,78. 8. Southwest Japan79. 9. Persian Gulf 80. 10. Oman81. 11. Australia82. Palaeogeographic map from Blakey83. Graphics created by G.N. in CorelDraw 11, www.coreldraw.com.

In addition to their numerical abundance, both the structural and taxonomic diversity of Boreal microconchids noticeably increased over time: Griesbachian assemblages of coiled Microconchus being restricted to Claraia shells, but subsequently replaced by sympatric colonies of coiled and helically uncoiled Microconchus attached to Claraia and algal layers. Finally, conical Spathioconchus weedoni appeared as a novel element in mudstone facies from the early Dienerian onwards. This clear eco-morphological trending infers progressive adaptation and habitat expansion, incorporating an innovative dispersal into localized paralic conditions. Interestingly, Yang et al.35 described similar coeval microconchid morphotypes from Griesbachian microbialites in South China. Their specimens included spiral and helically uncoiled forms resembling Microconchus utahensis, Helicoconchus elongatus, and M. aberrans respectively. Compatible structural diversification thus seems to have occurred in both the Boreal-Panthalassan and Tethyan realms, where microconchids paralleled stromatolites55, inarticulate brachiopods56, Claraia bivalves4,5,57 and various foraminiferans58 as opportunistic occupiers of benthic marine ecospace in the earliest Triassic33,34,35. By the Spathian (late Olenekian), however, bivalves and foraminiferans, together with boring suspension-feeders33,59 had colonised hard substrates to create transient metazoan reefs; these established on multi-taxic sponge60 and bivalve61 frameworks during the Smithian–Spathian “coral gap”10,11,60. The recovery of lower tier, skeletonised biotas was therefore evidently delayed in comparison to soft-bottom communities31,32,62, a phenomenon that we show manifested simultaneously within both low, and mid-high palaeolatitude assemblages. Certainly, some filter feeding organisms such as crinoids seem to have re-diversified earlier in the Boreal Realm (at least after the latest Induan A. fassaensis bivalve zone equivalent63), yet typical encrusters including cyclostome bryozoans and serpulid polychaetes did not fully re-establish until the Rhaetian64. This conspicuous underrepresentation – which is likely not taphonomic because Palaeozoic encrusters possessed similar calcitic skeletons65 and cemented to the substrate throughout the sessile phase of their life cycle – accords with extreme fluctuations in oceanic salinity66, de-oxygenation9,40,67, intense weathering and run-off that are thought to have promoted widespread eutrophication and the proliferation of stromatolite-forming microbial substrates10,11,26,68 in the absence of mat-grazing organisms55,69. Moreover, these markedly atypical conditions apparently favoured microconchids, which were ubiquitous across marine to brackish and even freshwater habitats36,70,71 and readily colonized microbial/algal substrates, perhaps because of their stability and immediate supply of nutrients and oxygen34,72. The propagation of these environments during the earliest Triassic could therefore explain the selective survival of microconchids versus other encrusting benthos, and otherwise reflects the ecosystem homogeneity that characterised the post P-T interval on a global scale.

Methods

Our microconchid fossils were inspected using both a binocular microscope and Philips XL30 Environmental Scanning Electron Microscope (ESEM) installed at the Faculty of Earth Sciences, University of Silesia, Sosnowiec, Poland. Uncoated ESEM samples were examined with back-scattered (BSE) imaging under low vacuum conditions. Samples for pyrite framboids were thin-sectioned and assessed by ESEM. More than 50 specimens were measured and interpreted following the procedures of Wignall and Newton73 and Bond and Wignall23. All fossils documented herein are housed in the Palaeontology Collection at Museum of Evolution, Uppsala University (PMU), Sweden under the registration numbers PMU 28933–PMU 28963.

Additional Information

How to cite this article: Zatoń, M. et al. Boreal earliest Triassic biotas elucidate globally depauperate hard substrate communities after the end-Permian mass extinction. Sci. Rep. 6, 36345; doi: 10.1038/srep36345 (2016).

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Acknowledgements

The Swedish Polar Research Secretariat provided field exploration funding to B.P.K. and H.B. The Faculty of Earth Sciences, University of Silesia facilitated travel and analysis of the fossils by M.Z. G.N. is financially supported by a Wallenberg Scholarship grant to Per. E. Ahlberg (Uppsala University). The Leading National Research Centre (KNOW) received by the Centre for Polar Studies for the period 2014–2018 covered publication costs for M.Z.

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Affiliations

  1. Centre for Polar Studies KNOW (Leading National Research Centre), University of Silesia, Faculty of Earth Sciences, Będzińska 60, 41-200 Sosnowiec, Poland

    • Michał Zatoń
  2. Uppsala University, Department of Organismal Biology, Norbyvägen 18A, 752 36 Uppsala, Sweden

    • Grzegorz Niedźwiedzki
    •  & Henning Blom
  3. Uppsala University, Museum of Evolution, Norbyvägen 16, 752 36 Uppsala, Sweden

    • Benjamin P. Kear

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Contributions

G.N., H.B. and B.P.K. collected the fossils and lithological samples. M.Z. and G.N. analysed the data. M.Z., B.P.K., G.N. and H.B. wrote the paper.

Competing interests

The authors declare no competing financial interests.

Corresponding author

Correspondence to Michał Zatoń.

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https://doi.org/10.1038/srep36345

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