Flora of the Late Triassic

  • Evelyn Kustatscher
  • Sidney R. Ash
  • Eugeny Karasev
  • Christian Pott
  • Vivi Vajda
  • Jianxin Yu
  • Stephen McLoughlin
Chapter
Part of the Topics in Geobiology book series (TGBI, volume 46)

Abstract

The Triassic was a time of diversification of the global floras following the mass-extinction event at the close of the Permian, with floras of low-diversity and somewhat uniform aspect in the Early Triassic developing into complex vegetation by the Late Triassic. The Earth experienced generally hothouse conditions with low equator-to-pole temperature gradients through the Late Triassic. This was also the time of peak amalgamation of the continents to form Pangea. Consequently, many plant families and genera were widely distributed in the Late Triassic. Nevertheless, two major floristic provinces are recognizable during this interval—one in the Southern Hemisphere (Gondwana) and another in the Northern Hemisphere (Laurussia); these being largely separated by the Tethys Ocean and a palaeotropical arid belt. Regional variations in topography, climate and light regime imposed further constraints on the distribution of plant groups in the Late Triassic such that two floristic sub-provinces are recognizable within Gondwana, and nine within Laurussia based on the plant macrofossil and dispersed spore-pollen records. In a broad sense, the Late Triassic saw the diversification of several plant groups that would become important components of younger Mesozoic floras (e.g., Bennettitales, Czekanowskiales, Gnetales and several modern fern and conifer families). The representation of these groups varied not only geographically, but waxed and waned through time in response to climatic pulses, such as the Carnian Pluvial Event. Significant turnovers are apparent in both macrofossil- and palyno-floras across the Triassic–Jurassic boundary, especially in the North Atlantic and Gondwanan regions. The geographic and temporal variations in the floras have necessitated the establishment of numerous regional palynozonation schemes that are tentatively correlated in this study. Major plant macrofossil assemblages of the Late Triassic world are also placed in a stratigraphic context for the first time. The Late Triassic floras also record the re-diversification of insect faunas based on a broad array of damage types preserved on leaves and wood. By the Late Triassic, all modern terrestrial arthropod functional feeding groups were established, and several very specialized feeding traits and egg-laying strategies had developed. Although age constraints on various fossil assemblages need to be improved, this study provides the first global overview of the temporal and geographic distributions of Late Triassic floras, and establishes a basis for future targeted research on Triassic phytogeography and phytostratigraphy.

Keywords

Non-marine ecosystems Palaeoclimate Plant fossils Palynomorphs Palaeo-provinces Mass-extinction Plant-animal interactions 

Notes

Acknowledgements

We want to thank Lawrence (Larry) Tanner for the organization of this book as well as Brian Axsmith and Spencer Lucas for their constructive reviews. Part of the material was studied by Evelyn Kustatscher under the projects ‘Taxonomic revision of the Carnian (Upper Triassic) conifers from the historical Raibl flora from Northern Italy’ (AT-TAF2999) and ‘Palaeozoic relict and “modern” Mesozoic ferns in the Ladinian and Carnian floras of Europe’ (DE-TAF239, AT-TAF236, SE-TAF149), which received funding through SYNTHESYS, which was made available by the European Community-Research Infrastructure Action under the FP7 ‘Structuring the European Research Area’ Programme. Evelyn Kustatscher acknowledges also financial support from the Alexander von Humboldt-Foundation (3.3-ITA/1141759STP). This paper is also part of the IGCP 630 cooperation project ‘Permian-Triassic climatic and environmental extremes and biotic response’. Eugeny Karasev thanks E.B. Volynets (Institute of Biology and Soil Sciences) for photos of fossil plants from the Late Triassic of Primorye. Eugeny Karasev received funding from the subsidy allocated to Kazan Federal University (#5.2192.2017/4.6) for the state assignment in the sphere of scientific activities. Christian Pott acknowledges funding from the German and Swedish Research Councils (DFG KR2125/3, VR 2012-4375) and from the ‘Friends of the Swedish Museum of Natural History’ (Riksmusei Vänner, Stockholm) and funding through SYNTHESYS (AT-TAF 467). Vivi Vajda acknowledges support from UNESCO grant IGCP 632 and the Swedish Research Council grant VR 2015-4264. Financial support to Stephen McLoughlin by the Swedish Research Council (VR grant 2014-5234) and National Science Foundation (project #1636625) is gratefully acknowledged.

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Copyright information

© Springer International Publishing AG 2018

Authors and Affiliations

  • Evelyn Kustatscher
    • 1
    • 2
  • Sidney R. Ash
    • 3
  • Eugeny Karasev
    • 4
  • Christian Pott
    • 5
    • 6
  • Vivi Vajda
    • 5
  • Jianxin Yu
    • 7
  • Stephen McLoughlin
    • 5
  1. 1.Museum of Nature South TyrolBozen/BolzanoItaly
  2. 2.Department für Geo– und Umweltwissenschaften, Paläontologie und GeobiologieLudwig–Maximilians–Universität, and Bayerische Staatssammlung für Paläontologie und GeologieMunichGermany
  3. 3.Department of Earth and Planetary SciencesUniversity of New MexicoAlbuquerqueUSA
  4. 4.Borissiak Paleontological InstituteRussian Academy of SciencesMoscowRussia
  5. 5.Palaeobiology DepartmentSwedish Museum of Natural HistoryStockholmSweden
  6. 6.LWL-Museum of Natural HistoryWestphalian State Museum and PlanetariumMünsterGermany
  7. 7.State Key Laboratory of Biogeology and Environmental GeologyChina University of GeosciencesWuhanP.R. China

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