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Tournaisian

Coordinates: 43°33′20″N 3°21′26″E / 43.5556°N 3.3572°E / 43.5556; 3.3572
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(Redirected from Kinderhookian)
Tournaisian
358.9 ± 0.4 – 346.7 ± 0.4 Ma
Paleogeography of the Tournaisian (350 Ma)
Chronology
Etymology
Name formalityFormal
Usage information
Celestial bodyEarth
Regional usageGlobal (ICS)
Time scale(s) usedICS Time Scale
Definition
Chronological unitAge
Stratigraphic unitStage
Time span formalityFormal
Lower boundary definitionFAD of the conodont Siphonodella sulcata (discovered to have biostratigraphic issues as of 2006).[2]
Lower boundary GSSPLa Serre, Montagne Noire, France
43°33′20″N 3°21′26″E / 43.5555°N 3.3573°E / 43.5555; 3.3573
Lower GSSP ratified1990[3]
Upper boundary definitionFAD of the benthic foraminifer Eoparastaffella simplex
Upper boundary GSSPPengchong Section, Guangxi, China
24°26′00″N 109°27′00″E / 24.4333°N 109.4500°E / 24.4333; 109.4500
Upper GSSP ratified2008

The Tournaisian is in the ICS geologic timescale the lowest stage or oldest age of the Mississippian, the oldest subsystem of the Carboniferous. The Tournaisian age lasted from 358.9 Ma to 346.7 Ma.[4] It is preceded by the Famennian (the uppermost stage of the Devonian) and is followed by the Viséan. In global stratigraphy, the Tournaisian contains two substages: the Hastarian (lower Tournaisian) and Ivorian (upper Tournaisian). These two substages were originally designated as European regional stages.

Name and regional alternatives

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The Tournaisian was named after the Belgian city of Tournai. It was introduced in scientific literature by Belgian geologist André Hubert Dumont in 1832. Like many Devonian and lower Carboniferous stages, the Tournaisian is a unit from West European regional stratigraphy that is now used in the official international time scale.[5]

The Tournaisian correlates with the regional North American Kinderhookian and lower Osagean stages and the Chinese Tangbagouan regional stage. In the British Isles, where the Hastarian and Ivorian are difficult to distinguish, the entire Tournaisian was equivalent to the Courceyan regional stage.

Stratigraphy

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The base of the Tournaisian (which is also the base of the Carboniferous system) is at the first appearance of the conodont Siphonodella sulcata within the evolutionary lineage from Siphonodella praesulcata to Siphonodella sulcata. The first appearance of ammonite species Gattendorfia subinvoluta is just above this and was used as a base for the Carboniferous in the past.[6] The GSSP for the Tournaisian is near the summit of La Serre hill, in the Lydiennes Formation of the commune of Cabrières, in the Montagne Noire (southern France).[7] The GSSP is in a section on the southern side of the hill, in an 80 cm deep trench, about 125 m south of the summit, 2.5 km southwest of the village of Cabrières and 2.5 km north of the hamlet of Fontès.

The top of the Tournaisian (the base of the Viséan) is at the first appearance of the fusulinid species Eoparastaffella simplex (morphotype 1/morphotype 2).

The Tournaisian contains eight conodont biozones:

Paleoenvironments

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The Tournaisian coincides with Romer's gap, a period of remarkably few terrestrial fossils, thus constituting a discontinuity between the Devonian and the more modern terrestrial ecosystems of the Carboniferous.

The middle of the Tournaisian is marked by a southern glaciation event, of a slightly lesser extent than the glaciations which swept over Gondwana in the later Carboniferous and the very end of the Devonian.[8][9] During the Tournaisian, South America was located at south polar latitudes and formed the westernmost part of the supercontinent Gondwana. The southwestern coastline of Gondwana was bustling with distinctive cold-water brachiopod and bivalve faunas.[10]

Coal is less common in the Tournaisian than in the rest of the Carboniferous, and forests and swamps were at low-density despite some trees reaching heights of up to 40 meters (131 feet). Anabranching channels and anastomosing rivers (with permanent channels splitting around large vegetated islands) would not develop until the Viséan, and river systems of the Tournaisian were more similar to those of the Late Devonian.[11]

Flora

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The Tournaisian saw a new diversification of arborescent (tree-sized) lycophytes and giant sphenophytes (horsetails). They coexisted alongside ferns and lignophytes (wood-bearing plants), including early seed plants such as lyginopteridalean pteridosperms ("seed ferns").[12] The Tournaisian was a transitional stage for lignophyte evolution: Devonian progymnosperm taxa such as Archaeopteris had gone extinct, but new types of woody trees such as Pitus and Protopitys set the stage for even greater morphological diversity. There is still much debate over the proportion of spore-bearing (progymnosperm) to seed-bearing (spermatophyte) woody plants, but both were evidently major parts of Tournaisian ecosystems.[13]

Tropical and subtropical swamps, in what is now Europe, North America, and China, represent a low-latitude paleobiogeographical realm known as the Amerosinian realm.[12] Divaricating (widely branching) trunks of Lepidodendropsis lycophytes are by far the most abundant and widespread plant fossils of the Tournaisian, yet there was some minor variation in other flora through time and space. In eastern North America, lyginopterids and probable progymnosperms were also common, as indicated by leaf form genera such as Adiantites, Rhodeopteridium, and Genselia.[12] The progymnosperm leaf Triphyllopteris may be more common in Europe while the lycophyte Sublepidodendron characterizes Tournaisian China. Late Devonian seed plants like Rhacopteris also persisted into the Tournaisian tropics. Lepidodendron, a massive arborescent lycophyte which would dominate coal forests through the rest of the Carboniferous, first appeared near the Tournaisian-Viséan boundary.[12]

Northern Asia (Kazakhstan and Siberia) was positioned within subtropical or temperate northern latitudes, and developed its own endemic floras, the Angaran realm. The most common plant fossils in this region were shrub-sized lycophytes such as Ursodendron and Tomiodendron, shorter than their arborescent tropical relatives.[12]

Gondwanan plant fossils are uncommon: southernmost Gondwana was covered by dwarf lycophytes, even smaller than those of the Angaran realm.[14] Subtropical and temperate lycophytes such as Lepidodendropsis, Archaeosigillaria, and Frenguellia could be found in some parts of the supercontinent, such as Argentina and Australia.[12] In the middle Tournaisian glaciation, species-poor frigid tundra developed in western Argentina.[14] These south polar tundras hosted the oldest known seed plants in Gondwanan territories, which likely spread south across a land bridge once the Rheic Ocean closed between Laurussia and Gondwana.[15] Tournaisian terrestrial sediments in South America are additionally characterized by the miospore index fossil Waltzispora lanzonii. The floral diversity of Tournaisian southern tundra consists almost entirely of relict Devonian genera; this suggests that Late Devonian land plant extinctions in lower latitudes were mostly driven by competition from new tropical species, rather than global environmental pressures.[15]

Invertebrates

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Trilobites experienced their final substantial diversification event in the mid-late Tournaisian, briefly regaining a level of diversity not seen since the Middle Devonian. Almost all new species belonged to the recently-evolved family Phillipsiidae, while the few surviving Devonian-type trilobites declined.[16] Most early Tournaisian trilobites were widespread deep-water species. By the late Tournaisian, they had recolonized shallower environments and divided into three different biogeographic zones corresponding to North America, Europe, and East Asia.[17]

Notable formations

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References

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  1. ^ "International Chronostratigraphic Chart" (PDF). International Commission on Stratigraphy. September 2023. Retrieved November 10, 2024.
  2. ^ Kaiser 2009.
  3. ^ Paproth, Feist & Flajs 1991.
  4. ^ Gradstein et al. (2004)
  5. ^ Heckel & Clayton (2006)
  6. ^ Menning et al. (2006); for the old definition, see Paeckelmann & Schindewolf (1937)
  7. ^ The GSSP was published by Paproth et al. (1991)
  8. ^ Ezpeleta, Miguel; Rustán, Juan José; Balseiro, Diego; Dávila, Federico Miguel; Dahlquist, Juan Andrés; Vaccari, Norberto Emilio; Sterren, Andrea Fabiana; Prestianni, Cyrille; Cisterna, Gabriela Adriana; Basei, Miguel (2020). "Glaciomarine sequence stratigraphy in the Mississippian Río Blanco Basin, Argentina, southwestern Gondwana. Basin analysis and palaeoclimatic implications for the Late Paleozoic Ice Age during the Tournaisian". Journal of the Geological Society. 177 (6): 1107–1128. Bibcode:2020JGSoc.177.1107E. doi:10.1144/jgs2019-214. hdl:2268/295479. ISSN 0016-7649. S2CID 226194983.
  9. ^ López-Gamundí, Oscar; Limarino, Carlos O.; Isbell, John L.; Pauls, Kathryn; Césari, Silvia N.; Alonso-Muruaga, Pablo J. (2021). "The late Paleozoic Ice Age along the southwestern margin of Gondwana: Facies models, age constraints, correlation and sequence stratigraphic framework". Journal of South American Earth Sciences. 107: 103056. Bibcode:2021JSAES.10703056L. doi:10.1016/j.jsames.2020.103056. S2CID 230528910.
  10. ^ Sterren, A.F.; Cisterna, G.A.; Rustán, J.J.; Vaccari, N.E.; Balseiro, D.; Ezpeleta, M.; Prestianni, C. (2021). "New invertebrate peri-glacial faunal assemblages in the Agua de Lucho Formation, Río Blanco Basin, Argentina. The most complete marine fossil record of the early Mississippian in South America". Journal of South American Earth Sciences. 106: 103078. Bibcode:2021JSAES.10603078S. doi:10.1016/j.jsames.2020.103078. S2CID 230863251.
  11. ^ Davies, Neil S.; Gibling, Martin R. (2013-05-01). "The sedimentary record of Carboniferous rivers: Continuing influence of land plant evolution on alluvial processes and Palaeozoic ecosystems". Earth-Science Reviews. 120: 40–79. Bibcode:2013ESRv..120...40D. doi:10.1016/j.earscirev.2013.02.004. ISSN 0012-8252.
  12. ^ a b c d e f Opluštil, Stanislav; Cleal, Christopher J.; Wang, Jun; Wan, Mingli (2022). "Carboniferous macrofloral biostratigraphy: an overview". Geological Society, London, Special Publications. 512 (1): 813–863. Bibcode:2022GSLSP.512..813O. doi:10.1144/SP512-2020-97. ISSN 0305-8719. S2CID 229457094.
  13. ^ Decombeix, Anne-Laure; Meyer-Berthaud, Brigitte; Galtier, Jean (2011). "Transitional changes in arborescent lignophytes at the Devonian–Carboniferous boundary". Journal of the Geological Society. 168 (2): 547–557. Bibcode:2011JGSoc.168..547D. doi:10.1144/0016-76492010-074. ISSN 0016-7649. S2CID 129970719.
  14. ^ a b Prestianni, Cyrille; Rustán, Juan José; Balseiro, Diego; Vaccari, N. Emilio (2022-10-02). "Porongodendron minitensis gen. nov. sp. nov. a new lycopsid from the Mississippian of Argentina with adaptations to tundra-like conditions" (PDF). Botany Letters. 169 (4): 527–539. Bibcode:2022BotL..169..527P. doi:10.1080/23818107.2022.2101515. hdl:2268/302490. ISSN 2381-8107. S2CID 251117143.
  15. ^ a b Prestianni, C.; Rustán, J. J.; Balseiro, D.; Vaccari, E.; Sterren, A. F.; Steemans, P.; Rubinstein, C.; Astini, R. A. (2015-01-01). "Early seed plants from Western Gondwana: Paleobiogeographical and ecological implications based on Tournaisian (Lower Carboniferous) records from Argentina". Palaeogeography, Palaeoclimatology, Palaeoecology. 417: 210–219. Bibcode:2015PPP...417..210P. doi:10.1016/j.palaeo.2014.10.039. hdl:2268/175336. ISSN 0031-0182.
  16. ^ Bault, Valentin; Balseiro, Diego; Monnet, Claude; Crônier, Catherine (2022). "Post-Ordovician trilobite diversity and evolutionary faunas". Earth-Science Reviews. 230: 104035. Bibcode:2022ESRv..23004035B. doi:10.1016/j.earscirev.2022.104035. S2CID 248439050.
  17. ^ Brezinski, David K. (2023). "Biogeographic patterns in Late Paleozoic trilobites". Palaeogeography, Palaeoclimatology, Palaeoecology. 609: 111319. Bibcode:2023PPP...60911319B. doi:10.1016/j.palaeo.2022.111319. S2CID 253560498.

Bibliography

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  • Dumont, A.H.; 1832: Mémoire sur la constitution géologique de la province de Liège, Mémoires couronnés par l'Académie Royale des Sciences et Belles-Lettres de Bruxelles 8 (3), VII. (in French)
  • Gradstein, F.M.; Ogg, J.G. & Smith, A.G.; 2004: A Geologic Time Scale 2004, Cambridge University Press
  • Heckel, P.H. & Clayton, G.; 2006: The Carboniferous system, use of the new official names for the subsystems, series and stages, Geologica Acta 4(3), pp 403–407
  • Kaiser, Sandra (1 April 2009). "The Devonian/Carboniferous boundary stratotype section (La Serre, France) revisited". Newsletters on Stratigraphy. 43 (2): 195–205. doi:10.1127/0078-0421/2009/0043-0195. Retrieved 7 December 2020.
  • Menning, M.; Alekseev, A.S.; Chuvashov, B.I.; Davydov, V.I.; Devuyst, F.-X.; Forke, H.C.; Grunt, T.A.; Hance, L.; Heckel, P.H.; Izokh, N.G.; Jin, Y.-G.; Jones, P.J.; Kotlyar, G.V.; Kozur, H.W.; Nemyrovska, T.I.; Schneider, J.W.; Wang, X.-D.; Weddige, K.; Weyer, D. & Work, D.M.; 2006: Global time scale and regional stratigraphic reference scales of Central and West Europe, East Europe, Tethys, South China, and North America as used in the Devonian–Carboniferous–Permian Correlation Chart 2003 (DCP 2003), Palaeogeography, Palaeoclimatology, Palaeoecology 240 (1-2): pp 318–372
  • Paeckelmann, W. & Schindewolf, O.H.; 1937: Die Devon-Karbon-Grenze, Comptes Rendus (2) du Cinquième Congrès International de Stratigraphie et Géologie du Carbonifère, Heerlen 1935 (2), pp 703–714 (in German)
  • Paproth, Eva; Feist, Raimund; Flajs, Gerd (December 1991). "Decision on the Devonian-Carboniferous boundary stratotype" (PDF). Episodes. 14 (4): 331–336. doi:10.18814/epiiugs/1991/v14i4/004. Archived (PDF) from the original on 2022-10-09.
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43°33′20″N 3°21′26″E / 43.5556°N 3.3572°E / 43.5556; 3.3572

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