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Carboniferous rainforest collapse

Topic: Earth

 From HandWiki - Reading time: 10 min
Short description: Extinction event at the end of the Moscovian in the Carboniferous
Coal forests continued after the Carboniferous rainforest collapse. These plant fossils are from one of those forests from about 5 million years after the CRC. However, the composition of the forests changed from a lepidodendron-dominated forest to one of predominantly tree ferns and seed ferns.

The Carboniferous rainforest collapse (CRC) was a minor extinction event that occurred around 305 million years ago in the Carboniferous period.[1] The event occurred at the end of the Moscovian and continued into the early Kasimovian stages of the Pennsylvanian (Upper Carboniferous).

It altered the vast coal forests that covered the equatorial region of Euramerica (Europe and America). This event may have fragmented the forests into isolated refugia or ecological "islands", which in turn encouraged dwarfism and, shortly after, extinction of many plant and animal species. Following the event, coal-forming tropical forests continued in large areas of the Earth, but their extent and composition were changed.

Extinction patterns on land

In the Carboniferous, the great tropical rainforests of Euramerica supported towering lycopodiophyta, a heterogeneous mix of vegetation, as well as a great diversity of animal life: giant dragonflies, millipedes, blattopterans, and smaller amphibians and the first amniotes.

Plants

The rise of rainforests in the Carboniferous greatly altered the landscapes by eroding low-energy, organic-rich anastomosing (braided) river systems with multiple channels and stable alluvial islands. The continuing evolution of tree-like plants increased floodplain stability (less erosion and movement) by the density of floodplain forests, the production of woody debris, and an increase in complexity and diversity of root assemblages.[2]

Collapse occurred through a series of step changes. First there was a gradual rise in the frequency of opportunistic ferns in late Moscovian times.[3] This was followed in the earliest Kasimovian by a major, abrupt extinction of the dominant lycopsids and a change to tree fern-dominated ecosystems.[4] This is confirmed by a 2011 study showing that the presence of meandering and anabranching streams, occurrences of large woody debris, and records of log jams decrease significantly at the Moscovian-Kasimovian boundary.[2] Rainforests were fragmented, forming shrinking 'islands' further and further apart, and in latest Kasimovian time, rainforests vanished from the fossil record. Little mixing of different plant assemblages occurred throughout this transition; floral assemblages were highly discrete and conservative and gave way to new ones without any transitional floras intermediate in composition with regards to the preceding one and succeeding one.[5]

Invertebrates

The fossil record of insects can be difficult to study, due to the generally smaller and more delicate nature of their bodies. One study tabulate the rates of origination and extinction of over 600 terrestrial and freshwater animal families. Their stratigraphic ranges spanned a geologic interval from the middle Paleozoic biotic invasion of the land to the Permian–Triassic extinction event. Insects comprise more than half of the sampled families, most of which are from tropical Euramerica. This study found a Late Pennsylvanian extinction pulse that reflects drying climates and the transition of lycopod to tree fern-dominated land floras.[6]

Vertebrates

Before the collapse, vertebrate animal species distribution was very cosmopolitan, with the same species existing across tropical Pangaea. After the collapse, each surviving rainforest 'island' developed its own unique mix of species. Many amphibian species became extinct, while the ancestors of reptiles and mammals diversified into more species after the initial crisis.[1] These patterns are explained by the theory of insular biogeography, a concept that explains how evolution progresses when populations are restricted into isolated pockets. This theory was originally developed for oceanic islands, but it can be applied equally well to any other ecosystem that is fragmented, only existing in small patches and surrounded by another unsuitable habitat.

According to this theory, the initial impact of habitat fragmentation is devastating, with most life dying out quickly from lack of resources. Then, as surviving plants and animals reestablish themselves, they adapt to their restricted environment to take advantage of the new allotment of resources, and diversify. After the CRC, each pocket of life evolved in its own way, resulting in a unique species mix that ecologists call "endemism". A 2018 paper challenged this theory, however, finding evidence for increased cosmopolitanism rather than endemism following the demise of Carboniferous rainforests.[7]

Biotic recovery and evolutionary consequences

Plants

The fragmentation of wetlands left a few isolated refugia in Europe. However, even these were unable to maintain the diversity of Moscovian flora.[8] By the Asselian, many families of seed ferns that characterized the Moscovian tropical wetlands had disappeared including Flemingitaceae, Diaphorodendraceae, Tedeleaceae, Urnatopteridaceae, Cyclopteridaceae, and Neurodontopteridaceae.[8]

Invertebrates

Carboniferous rainforest collapse is sometimes treated as an extinction factor for large Carboniferous arthropods such as giant griffinfly Meganeura and millipede Arthropleura. It is common theory that high oxygen levels have led to larger arthropods, and these organisms have been thought to live in forests. It was said that rainforest collapse led to a decrease in oxygen concentration and a decrease in the habitat of these arthropods, leading them to extinction.[9] However, later study shows that both griffinflies and Arthropleura more likely lived a forest-independent life, and fossil records of both large griffinflies and Arthropleura are known after rainforest collapse.[10][11][12] This means that rainforest collapse and reduced oxygen levels were less involved in their extinction.

Vertebrates

Terrestrially adapted synapsids, the predecessors of the mammal lineage, like Archaeothyris were among the groups who quickly recovered after the collapse.

The sudden collapse affected several large groups. Labyrinthodont amphibians were particularly devastated, while the amniotes (the first members of the sauropsid and synapsid groups) fared better, being physiologically better adapted to the drier conditions.[1]

Amphibians can survive cold conditions by decreasing metabolic rates and resorting to overwintering strategies (i.e. spending most of the year inactive in burrows or under logs). However, this is not an effective way to deal with prolonged unfavourable conditions, especially desiccation. Amphibians must return to water to lay eggs, while amniotes have eggs that have a membrane that retains water and allows gas exchange out of water. Because amphibians had a limited capacity to adapt to the drier conditions that dominated Permian environments, many amphibian families failed to occupy new ecological niches and became extinct.[13] Amphibians also removed the scales of their aquatic ancestors, and breathed with both lungs and skin (as long as the skin was kept wet). But amniotes re-evolved scales, now more keratinized, allowing them to conserve water but losing their cutaneous respiration.

Synapsids and sauropsids acquired new niches faster than amphibians, and new feeding strategies, including herbivory and carnivory, previously only having been insectivores and piscivores.[1] Synapsids in particular became substantially larger than before and this trend would continue until the Permian–Triassic extinction event, after which their cynodont (mammal ancestors) descendants became smaller and nocturnal.

Possible causes

Atmosphere and climate

There are several hypotheses about the nature and cause of the Carboniferous rainforest collapse, some of which include climate change.[14][15][16] After the late Bashkirian glacial maximum of the Late Paleozoic Ice Age I, around 318 Ma, frequent shifts in seasonality from humid to arid times began.[17]

The Carboniferous period is characterised by the formation of coal deposits which were formed within a context of the removal of atmospheric carbon. In the latest Middle Pennsylvanian (late Moscovian) a cycle of aridification began, coinciding with abrupt faunal changes in marine and terrestrial species.[18] This change was recorded in paleosols, which reflect a period of overall decreased hydromorphy, increased free-drainage and landscape stability, and a shift in the overall regional climate to drier conditions in the Upper Pennsylvanian (Missourian). This is consistent with climate interpretations based on contemporaneous paleo-floral assemblages and geological evidence.[18][19][20]

At the time of the Carboniferous rainforest collapse, the climate became cooler and drier. This is reflected in the rock record as the Earth entered a short, intense ice age. Sea levels dropped by about 100 metres (330 ft), and glacial ice covered most of the southern continent of Gondwana.[21] The climate was unfavourable to rainforests and much of the biodiversity in them. Rainforests shrank into isolated patches mostly confined to wet valleys further and further apart. Little of the original lycopsid rainforest biome survived this initial climate crisis. The concentration of carbon dioxide in the atmosphere crashed to one of its all time global lows in the Pennsylvanian and early Permian.[17][21] As the climate aridified through the Late Paleozoic, rainforests were eventually replaced by seasonally dry biomes.[22]

Volcanism

After restoring the middle of the Skagerrak-Centered Large Igneous Province using a new reference frame, it has been shown that the Skagerrak plume rose from the core–mantle boundary to its ~300 Ma position.[23] The major eruption interval took place in very narrow time interval, of 297 Ma ± 4 Ma. The rift formation coincides with the Moskovian/Kasimovian boundary and the Carboniferous rainforest collapse.[24]

Geography

While the CRC affected the equatorial region of Euramerica, the collapse had no effect in the region of Cathaysia to the east (which mostly corresponds to modern China), where Carboniferous-like rainforests persisted until the end of the Permian, around 252 million years ago.

Fossil sites

Fossil lycopsid, probably Sigillaria, from Joggins, with attached stigmarian roots

Many fossil sites around the world reflect the changing conditions of the Carboniferous rainforest collapse.

  • Hamilton, Kansas, US
  • Jarrow Tyne & Wear, UK
  • former Linton Mine in Saline Township, Jefferson County, Ohio, US
  • Nýřany, Czech Republic
  • Joggins, Nova Scotia, Canada

The Joggins Fossil Cliffs on Nova Scotia's Bay of Fundy, a UNESCO World Heritage Site, is a particularly well-preserved fossil site. Fossil skeletons embedded in the crumbling sea cliffs were discovered by Sir Charles Lyell in 1852. In 1859, his colleague William Dawson discovered the oldest known reptile-ancestor, Hylonomus lyelli, and since then hundreds more skeletons have been found, including the oldest synapsid, Protoclepsydrops.[25]

References

  1. ↑ 1.0 1.1 1.2 1.3 Sahney, S., Benton, M.J. & Falcon-Lang, H.J. (2010). "Rainforest collapse triggered Pennsylvanian tetrapod diversification in Euramerica" (PDF). Geology 38 (12): 1079–1082. doi:10.1130/G31182.1. Bibcode: 2010Geo....38.1079S. http://geology.geoscienceworld.org/cgi/content/abstract/38/12/1079. 
  2. ↑ 2.0 2.1 Davies, N.S.; Gibling, M. R. (2011). "Evolution of fixed-channel alluvial plains in response to Carboniferous vegetation". Nature Geoscience 21 (9): 629–633. doi:10.1038/ngeo1237. Bibcode: 2011NatGe...4..629D. 
  3. ↑ Pfefferkorn, H.W.; Thomson, M.C. (1982). "Changes in dominance patterns in Upper Carboniferous plant fossil assemblages". Geology 10 (12): 641. doi:10.1130/0091-7613(1982)10<641:CIDPIU>2.0.CO;2. Bibcode: 1982Geo....10..641P. 
  4. ↑ DiMichele, W.A.; Phillips, T.L. (1996). "Climate change, plant extinctions and vegetational recovery during the Middle-Late Pennsylvanian transition: The case of tropical peat-forming environments in North America". Biotic Recovery from Mass Extinction Events: Geological Society of London Special Publication 102 (1): 201–221. doi:10.1144/GSL.SP.1996.001.01.14. Bibcode: 1996GSLSP.102..201D. 
  5. ↑ DiMichele, William A.; Pfefferkorn, Hermann W.; Gastaldo, Robert A. (May 2001). "Response of Late Carboniferous and Early Permian Plant Communities to Climate Change". Annual Review of Earth and Planetary Sciences 29: 461–487. doi:10.1146/annurev.earth.29.1.461. Bibcode: 2001AREPS..29..461D. https://www.annualreviews.org/doi/abs/10.1146/annurev.earth.29.1.461. Retrieved 31 March 2023. 
  6. ↑ Rivera, Alexei A. (2017-07-16). "Sluggish Rates of Evolution for Land Animals During the Late Paleozoic Ice Age: A Geobiological Interpretation" (in en). The Paleontological Society Special Publications 13: 91. doi:10.1017/S2475262200011965. ISSN 2475-2622. https://www.cambridge.org/core/journals/paleontological-society-special-publications/article/abs/sluggish-rates-of-evolution-for-land-animals-during-the-late-paleozoic-ice-age-a-geobiological-interpretation/4D1B6404B4B538D3A96125D6DF0DFB98. 
  7. ↑ Dunne, Emma M.; Close, Roger A.; Button, David J.; Brocklehurst, Neil; Cashmore, Daniel D.; Lloyd, Graeme T.; Butler, Richard J. (7 February 2018). "Diversity change during the rise of tetrapods and the impact of the 'Carboniferous rainforest collapse'". Proceedings of the Royal Society B 285 (1872): 1–8. doi:10.1098/rspb.2017.2730. PMID 29436503. 
  8. ↑ 8.0 8.1 Borja Cascales-Miñana; Christopher J. Cleal (2013). "The plant fossil record reflects just two great extinction events". Terra Nova 26 (3): 195–200. doi:10.1111/ter.12086. Bibcode: 2014TeNov..26..195C. 
  9. ↑ Holmes, Thom (2008) (in en). March Onto Land: The Silurian Period to the Middle Triassic Epoch. Infobase Publishing. ISBN 978-0-8160-5959-1. https://books.google.com/books?id=j-sOYynMAAMC&pg=PA59. 
  10. ↑ Nel, André; Prokop, Jakub; Pecharová, Martina; Engel, Michael S.; Garrouste, Romain (2018-08-14). "Palaeozoic giant dragonflies were hawker predators". Scientific Reports 8 (1): 12141. doi:10.1038/s41598-018-30629-w. ISSN 2045-2322. PMID 30108284. Bibcode: 2018NatSR...812141N. 
  11. ↑ Nel, Andre; Fleck, Gunther; GARROUSTE, Romain; Gand, Georges (2008-08-10). "The Odonatoptera of the Late Permian Lodève Basin (Insecta)". Journal of Iberian Geology. https://www.researchgate.net/publication/27594087. 
  12. ↑ Davies, Neil S.; Garwood, Russell J.; McMahon, William J.; Schneider, Joerg W.; Shillito, Anthony P. (2022-05-01). "The largest arthropod in Earth history: insights from newly discovered Arthropleura remains (Serpukhovian Stainmore Formation, Northumberland, England)" (in en). Journal of the Geological Society 179 (3). doi:10.1144/jgs2021-115. ISSN 0016-7649. Bibcode: 2022JGSoc.179..115D. https://jgs.lyellcollection.org/content/179/3/jgs2021-115. 
  13. ↑ Miguel Á. Olalla-Tárraga1, Lynsey McInnes, Luis M. Bini, José A. F. Diniz-Filho, Susanne A. Fritz, Bradford A. Hawkins, Joaquín Hortal, C. David L. Orme1, Carsten Rahbek, Miguel Á. Rodríguez, Andy Purvis (2010). "Climatic niche conservatism and the evolutionary dynamics in species range boundaries: global congruence across mammals and amphibians". Journal of Biogeography 38 (12): 2237–2247. doi:10.1111/j.1365-2699.2011.02570.x. 
  14. ↑ Fielding, C.R.; Frank, T.D.; Birgenheier, L.P.; Rygel, M.C.; Jones, A.T.; Roberts, J. (2008). "Stratigraphic imprint of the Late Palaeozoic Ice Age in eastern Australia: A record of alternating glacial and nonglacial climate regime". Geological Society of London Journal 165 (1): 129–140. doi:10.1144/0016-76492007-036. Bibcode: 2008JGSoc.165..129F. 
  15. ↑ Heckel, P.H. (1991). "Lost Branch Formation and revision of upper Desmoinesian stratigraphy along midcontinent Pennsylvanian outcrop belt". Geological Survey Geology Series 4. 
  16. ↑ DiMichele, W.A.; Cecil, B.; Montanez, I.P.; Falcon-Lang, H.J. (2010). "Cyclic changes in Pennsylvanian paleoclimate and effects on floristic dynamics in tropical Pangaea". International Journal of Coal Geology 83 (2–3): 329–344. doi:10.1016/j.coal.2010.01.007. Bibcode: 2010IJCG...83..329D. 
  17. ↑ 17.0 17.1 Gulbransona, Montañezb; Taborc, Limarinod (2014). "Late Pennsylvanian aridification on the southwestern margin of Gondwana (Paganzo Basin, NW Argentina): A regional expression of a global climate perturbation". Palaeogeography, Palaeoclimatology, Palaeoecology 417: 220–235. doi:10.1016/j.palaeo.2014.10.029. Bibcode: 2015PPP...417..220G. 
  18. ↑ 18.0 18.1 Gulbranson, EL; Montanez, IP; Tabor, NJ; Limarino, CO (2015). "Late Pennsylvanian aridification on the southwestern margin of Gondwana (Paganzo Basin, NW Argentina): A regional expression of a global climate perturbation". Palaeogeography, Palaeoclimatology, Palaeoecology 417: 220–235. doi:10.1016/j.palaeo.2014.10.029. Bibcode: 2015PPP...417..220G. 
  19. ↑ Rosenau, Nicholasd; Neil J. Tabor (2013). "Oxygen and hydrogen isotope composition of paleosol phyllosilicates: Differential burial histories and determination of Middle–Late Pennsylvanian low-latitude terrestrial paleotemperatures". Palaeogeography, Palaeoclimatology, Palaeoecology 392: 382–397. doi:10.1016/j.palaeo.2013.09.020. Bibcode: 2013PPP...392..382R. 
  20. ↑ Rosenau, Nicholas; Tabor, Neil J.; Elrick, Scott D.; Nelson, W. John (2013). "Polygenetic History of Paleosols In Middle–Upper Pennsylvanian Cyclothems of the Illinois Basin, U.S.A.: Part II. Integrating Geomorphology, Climate, and Glacioeustasy". Journal of Sedimentary Research 83 (8): 637–668. doi:10.2110/jsr.2013.51. Bibcode: 2013JSedR..83..637R.  See "Dinosaur Extinction" chapter.
  21. ↑ 21.0 21.1 Polly, D.P. (2011). The Carboniferous Crisis. http://www.indiana.edu/~g404/Lectures/Lecture%201%20-%20Carboniferous%20Crisis%20and%20Introduction%20to%20Vertebrate%20Geobiology.pdf. Retrieved 2011-09-04. 
  22. ↑ Montañez, I.P.; Tabor, N.J.; Niemeier, D.; DiMichele, W.A.; Frank, T.D.; Fielding, C.R.; Isbell, J.L.; Birgenheier, L.P. et al. (2007). "CO2-forced climate and vegetation instability during late Paleozoic deglaciation". Science 315 (5808): 87–91. doi:10.1126/science.1134207. PMID 17204648. Bibcode: 2007Sci...315...87M. http://digitalcommons.unl.edu/cgi/viewcontent.cgi?article=1103&context=geosciencefacpub. 
  23. ↑ T.H. Torsvik; M.A. Smethurst; K. Burke; B. Steinberger (2008). "Long term stability in deep mantle structure: evidence from the 300 Ma Skagerrak-Centered Large Igneous Province (the SCLIP)". Earth and Planetary Science Letters 267 (3–4): 444–452. doi:10.1016/j.epsl.2007.12.004. Bibcode: 2008E&PSL.267..444T. 
  24. ↑ Vadim A. Kravchinsky (2012). "Paleozoic large igneous provinces of Northern Eurasia: Correlation with mass extinction events". Global and Planetary Change 86-87: 31–36. doi:10.1016/j.gloplacha.2012.01.007. Bibcode: 2012GPC....86...31K. 
  25. ↑ Falcon-Lang, H. J., Benton, M.J., Braddy, S. J. and Davies, S.J. (2006). "The Pennsylvanian tropical biome reconstructed from the Joggins Formation of Nova Scotia, Canada". Journal of the Geological Society, London 163 (3): 561–576. doi:10.1144/0016-764905-063. Bibcode: 2006JGSoc.163..561F. 

Further reading

Extinction events v · d · e

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