Jump to content

Carboniferous rainforest collapse

From Wikipedia, the free encyclopedia

This is an old revision of this page, as edited by Plantsurfer (talk | contribs) at 10:51, 4 April 2020 (→Plants: seed ferns). The present address (URL) is a permanent link to this revision, which may differ significantly from the current revision.

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] 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 'islands', which in turn caused 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.

The event occurred at the end of the Moscovian and continued into the early Kasimovian stages of the Pennsylvanian (Upper Carboniferous).

Extinction patterns on land

Ferns and tree ferns from Mount Field National Park, giving an impression of how a Carboniferous rainforest might have looked

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, cockroaches, 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 recent study showing that the presence of meandering and anabranching rivers, 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.

Animals

Before the collapse, animal species distribution was very cosmopolitan—the same species existed everywhere across tropical Pangaea—but 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 Carboniferous Rainforest Collapse, each pocket of life evolved in its own way, resulting in a unique species mix that ecologists call "endemism".

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.[5] By the Asselian many families of seed ferns that characterized the Moscovian tropical wetlands had disappeared including Flemingitaceae, Diaphorodendraceae, Tedeleaceae, Urnatopteridaceae, Alethopteridaceae,[verification needed] Cyclopteridaceae, and Neurodontopteridaceae.[5]

Invertebrates

The depletion of plant life contributed to declining concentrations of oxygen in the atmosphere. High oxygen levels had made the enormous arthropods of the time possible. Due to the decreasing oxygen, these sizes could no longer be accommodated, and thus between this and the loss of habitat, the giant arthropods were wiped out in this event, most notably the giant dragonflies (Meganeura) and millipedes (Arthropleura).[citation needed]

Vertebrates

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

This 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.

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.[6]

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]

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.[7][8][9] After a late Bashkirian interval of glaciation, high-frequency shifts in seasonality from humid to arid times began.[10]

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. 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 100 m, and glacial ice covered most of the southern continent of Gondwana.[11] 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.[10][11]

Then a succeeding period of global warming reversed the climatic trend; the remaining rainforests, unable to survive the rapidly changing conditions, were finally wiped out.[vague][citation needed]

As the climate aridified again through the later Paleozoic, rainforests were eventually replaced by seasonally dry biomes.[12] Though the exact speed and nature of the collapse is not clear, it is thought to have occurred relatively quickly in geologic terms, only a few thousand years at most.[citation needed]

Volcanism

After restoring the middle of the Skagerrak-Centered Large Igneous Province (SCLIP) using a new reference frame, it has been shown that the Skagerrak plume rose from the core–mantle boundary (CMB) to its ~300 Ma position.[13] 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.[14]

Climate and geology

A paleoclimate change of global nature occurred during the Moscovian and Kasimovian. An atmospheric drying (aridification) happened in the Middle to Late Pennsylvanian, coinciding with abrupt faunal changes in marine and terrestrial species.[15] 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.[15][16][17]

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.

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.[18]

References

  1. ^ a b c Sahney, S., Benton, M.J. & Falcon-Lang, H.J. (2010). "Rainforest collapse triggered Pennsylvanian tetrapod diversification in Euramerica" (PDF). Geology. 38 (12): 1079–1082. Bibcode:2010Geo....38.1079S. doi:10.1130/G31182.1.{{cite journal}}: CS1 maint: multiple names: authors list (link)
  2. ^ a b Davies, N.S.; Gibling, M. R. (2011). "Evolution of fixed-channel alluvial plains in response to Carboniferous vegetation". Nature Geoscience. 21 (9): 629–633. Bibcode:2011NatGe...4..629D. doi:10.1038/ngeo1237.
  3. ^ Pfefferkorn, H.W.; Thomson, M.C. (1982). "Changes in dominance patterns in Upper Carboniferous plant fossil assemblages". Geology. 10 (12): 641. Bibcode:1982Geo....10..641P. doi:10.1130/0091-7613(1982)10<641:CIDPIU>2.0.CO;2.
  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. Bibcode:1996GSLSP.102..201D. doi:10.1144/GSL.SP.1996.001.01.14.
  5. ^ a b Borja Cascales-Miñana; Christopher J. Cleal (2013). "The plant fossil record reflects just two great extinction events". Terra Nova. 26 (3): 195–200. Bibcode:2014TeNov..26..195C. doi:10.1111/ter.12086.
  6. ^ 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.{{cite journal}}: CS1 maint: multiple names: authors list (link) CS1 maint: numeric names: authors list (link)
  7. ^ 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. Bibcode:2008JGSoc.165..129F. doi:10.1144/0016-76492007-036. {{cite journal}}: Unknown parameter |last-author-amp= ignored (|name-list-style= suggested) (help)
  8. ^ Heckel, P.H. (1991). "Lost Branch Formation and revision of upper Desmoinesian stratigraphy along midcontinent Pennsylvanian outcrop belt". Geological Survey Geology Series. 4.
  9. ^ 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. {{cite journal}}: Unknown parameter |last-author-amp= ignored (|name-list-style= suggested) (help)
  10. ^ a b 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.
  11. ^ a b Polly, D.P (2011). "The Carboniferous Crisis" (PDF). {{cite journal}}: Cite journal requires |journal= (help)
  12. ^ Montañez, I.P.; Tabor, N.J.; Niemeier, D.; DiMichele, W.A.; Frank, T.D.; Fielding, C.R.; Isbell, J.L.; Birgenheier, L.P.; Rygel, M.C. (2007). "CO2-forced climate and vegetation instability during late Paleozoic deglaciation". Science. 315 (5808): 87–91. Bibcode:2007Sci...315...87M. doi:10.1126/science.1134207. PMID 17204648. {{cite journal}}: Unknown parameter |last-author-amp= ignored (|name-list-style= suggested) (help)
  13. ^ 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. Bibcode:2008E&PSL.267..444T. doi:10.1016/j.epsl.2007.12.004.
  14. ^ Vadim A. Kravchinsky (2012). "Paleozoic large igneous provinces of Northern Eurasia: Correlation with mass extinction events". Global and Planetary Change. 86–87: 31–36. Bibcode:2012GPC....86...31K. doi:10.1016/j.gloplacha.2012.01.007.
  15. ^ a b 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. Bibcode:2015PPP...417..220G. doi:10.1016/j.palaeo.2014.10.029.
  16. ^ 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. Bibcode:2013PPP...392..382R. doi:10.1016/j.palaeo.2013.09.020.
  17. ^ 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. Bibcode:2013JSedR..83..637R. doi:10.2110/jsr.2013.51. See "Dinosaur Extinction" chapter.
  18. ^ 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. Bibcode:2006JGSoc.163..561F. doi:10.1144/0016-764905-063.{{cite journal}}: CS1 maint: multiple names: authors list (link)

Further reading

Retrieved from "https://en.wikipedia.org/w/index.php?title=Carboniferous_rainforest_collapse&oldid=949042039"