Chemical conditions for the end-Permian mass extinction

From an empirical standpoint the mass extinction at the close of the Palaeozoic, 251 Ma ago, links closely with eruption of the largest known flood basalt pile in Siberia, and there is no known extraterrestrial impact that tallies. So it seems likely that the P-T event was generated by the influence of a mighty mantle plume on surface conditions. Careful statistical analysis of the marine faunas that preceded and followed the event give some clues to geochemical conditions associated with the extinctions and slow Triassic recovery of animal diversity (Bottjjer, D.J. et al. 2008. Understanding mechanisms for the end-Permian mass extinction and the protracted Early Triassic aftermath and recovery. GSA Today, v. 18, September 2008 issue, p.4-10). Brachiopods, bivalves and bryozoans, in terms of their respective diversities and abundance relative to one another, changed markedly. On the late Permian seafloor, brachiopods and bryozoa fell in both measures, whereas bivalves exploded in numbers but became dominated by just 4 genera. This ecological lop-sidedness continued in the early Triassic. Such an oddity in itself suggests that some kind of geochemical stress was present in marine environments for a protracted period of time. The most likely stressful agents are increased CO2 and H2S, and decreased oxygen. The faunal review goes on to discuss the need for experimental manipulation of oxygen, carbon dioxide and hydrogen sulfide concentrations to see the effects on modern organisms.

Another approach to the issue of the P-T event is to model the conditions that may have led to anoxia linked with increased CO2 and H2S (Meyer, K.M. et al. 2008. Biochemical controls on photic-zone euxinia during the end-Permian mass extinction. Geology, v. 36, p. 747-750). The authors use an Earth system model of ocean circulation coupled with one for the distribution of atmospheric moisture when the continents were assembled into the Pangaea supercontinent. Chemical constraints were 12 times the current carbon dioxide content for the atmosphere and about one fifth of its present oxygen content (see New twist for end-Permian extinctions in the May 2005 issue of EPN), roughly those accepted for the time. The supply of phosphate to the oceans was varied up to 10 times present values. Specifically, the model examined the likely effects of such conditions on the likelihood of hydrogen sulfide production in the oceans and its transfer to the uppermost ocean water. Increasing supply of phosphate inexorably drives global near-surface conditions towards anoxia and H2S – rich conditions. Even adding sulfide-oxidising bacteria to the surface waters doesn’t prevent runaway toxicity, including export of hydrogen sulfide to the atmosphere that would drive many land animals to extinction. It is hard to think of a more pervasive and effective ‘kill mechanism’, nor one that would have lingered for longer, thereby satisfying the evidence, including the extremely long biota recovery time during the Triassic. The two accounts taken together cast doubt on a determining role for the Siberian flood basalts, which were relatively short-lived, although volcanic emissions of CO.2 and SO2 may have placed a chemical ‘last straw’ on already stressed organisms.

Plant evolution summarised

Papers on palaeobotany, especially the evolution of plants are a lot less frequent than those on many other broad geoscience topics. So to see a review is welcome (O’Donoghue, J. 2008. Petal Power. New Scientist, v. 200 1 November 2008 issue, p. 36-39). O’Donoghue summarises recent publications on the rise of the angiosperms – Darwin’s “abominable mystery” – since the Jurassic. Accepted wisdom has long been that the earliest flowering plants were akin to modern magnolias that seem anatomically primitive. That assumption has much to answer for, because palaeobotanists sought evidence for big, simple flowers. It was a piece of pure luck that resolved the issue, in the form of fossilised debris from an 83 Ma wildfire found in Sweden. The carbon-rich clay contained masses of flowers only a few mm across, which resemble those of walnuts, plane trees and saxifrages. A shift in focus to minute blooms enabled Chinese geologists working on evidence for the habitat of the famous feathered dinosaurs to find the earliest flowers yet in an early Cretaceous (125 Ma) lagerstätte. They are humble indeed, resembling duckweed. Pushing back further the time of separation of the angiosperms from a presumed gymnosperm (cycads, ginkgoes and conifers) has depended on molecular evidence from living primitive flowering plants, and came up with a humble shrub from New Caledonia (Amborella), the srat anise plant (a member of the Austrobaileyales group) and water lilies. A molecular-clock approach suggests an evolutionary jump from gymnosperms took place as far back as the early Jurassic. The peculiar means of sexual reproduction evolved by angiosperms – giving animals a ‘free lunch’ with the perk to plants of their carrying pollen – cut the amount of energy involved in reproduction by massive pollen release for wind fertilisation and production of seeds without guaranteed fertility used by gymnosperms. In turn is resulted in a massive adaptive radiation by insects in particular, seeing the bees evolve from predatory wasps in early Cretaceous times. Now, to a very large extent, angiosperms are dependent on the humble bee. An alarming fact since bee diseases and parasites are currently getting the upper hand, while we become ever dependent on food sources from a  dominantly angiosperm crops.

The strange case of the line-dancing arthropods

Lagerstätten – sites of extraordinarily good fossil preservation – generally throw up surprises and oddities, and those of Cambrian age in China are no exception. Cambrian arthropods, notably the trilobites but also shrimp-like creatures, are not uncommon in them. But any animals that appear to have been engaged in communal activities are cause for both a double-take and a short communication (Hou, X-G. et al. 2008. Collective behaviour in an Early Cambrian arthropod. Science, v. 322, p. 224). About 22 groupings of shrimp-like fossils show individuals linked in ‘nose-to-tail’ chains, the tail (telson) of one in front being lodged in the carapace of that behind. Not only that, but the chains are meandering. ‘Follow-my-leader’ behaviour is seen in modern lobsters bent on migration; perhaps the inspiration for Lewis Carroll’s Lobster Quadrille in Alice in Wonderland. Since no modern arthropods link in such chains for reproductive purposes, and mouth-clenching a partner’s tail is not good evidence for feeding behaviour, the authors’ conclusion is that indeed the diminutive and very ancient creatures were probably hooked-up to go somewhere more conducive to their habits.

Evidence for earliest photosynthesisers takes a knock

The first tangible and isotopic evidence for the permanent presence of oxygen in the Earth’s atmosphere appears in sedimentary rocks dated at about 2.4 Ga. From that we can surmise that some organisms had previously evolved the photosynthetic trick of breaking the hydrogen-oxygen bonds in water: nothing else is known in nature to produce free oxygen on a planetary scale. Frustratingly, the earliest undisputed fossils of such organisms – blue-green bacteria – are a lot younger; around 2 Ga. Structures in sedimentary rocks back to 3.5 Ga, such as stromatolites, which do look a lot like products of living cyanobacteria and may have a biogenic origin, do not contain cellular structures that would constitute proof. So a report in the late 1990s of organic-chemical evidence for cyanobacteria from 2.7 Ga old sediments was greeted with some relief. These oldest biomarkers also included compounds characteristic of eukaryotes; an even more astonishing outcome, given that the oldest undoubted eukaryote fossils are from 1.5 Ga sediments. The ancient biomarkers have been much celebrated, but there is a problem: if cyanobacteria were around at 2.7 Ga in sufficient amounts for their biomarkers to be preserved, how come it took 300 Ma for oxygen to build up in the atmosphere? A novel technology for geochemists has been applied to resolve the issue of the Archaean biomarkers (Rassmussen, B. et al. 2008. Reassessing the first appearance of eukaryotes and cyanobacteria. Nature, v. 455, p. 1101-1104). One of the co-authors, Jochen Brocks of the Australian National University, was an originator of the study on biomarkers, so clearly the new technology has thrown matters into considerable disarray. The oily biomarkers accompany solid kerogen in the late Archaean sediments, in microscopic amounts. Ion-probe mass spectrometry with a 50 nm resolution has provided carbon-isotope measurements of minute samples of several kinds of hydrocarbon in thin sections. These show, with little room for doubt, that the organic compounds thought to have been biomarkers for cyanobacteria and eukaryotes formed by ‘cracking’ of kerogen during thermal metamorphism at about 2.2 Ga. Any other claims based on supposedly specific biomarkers are likely to be ‘tarred with the same brush’. How annoying: complex life clearly was around before 2.4 Ga, some of capable of photosynthesis, but that conjecture cannot be proven!

Much ingenuity has been harnessed to design robotic geochemistry that will be aimed at the popular topic of ‘Life on Mars’ in the coming decades. It would be no surprise if biomarkers are targeted. Yet it is entirely possible that hydrocarbons of inorganic origin can yield such compounds, given some geothermal heating…

See also: Fischer, W.W. 2008. Life before the rise of oxygen. Nature, v. 455, p. 1051-2.


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