What followed the K-Pg extinction event?

A study of boron isotopes in the tests of foraminifera that lived deep in the oceans and near their surface just after the K-Pg boundary event has revealed that ocean water suddenly became more acidic (Henehan, M.J. and 13 others 2019. Rapid ocean acidification and protracted Earth system recovery followed the end-Cretaceous Chicxulub impact. Proceedings of the National Academy of Sciences. Online; DOI: 10.1073/pnas.1905989116). Because the data came from marine sediment sequences exposed in Europe and North America  and from ocean-floor cores beneath the Atlantic and Pacific Oceans, the acidification was global in scope. The sharp fall in pH, almost certainly due to massive release of sulphuric and carbonic acids from thick anhydrite  and limestone beds beneath the Chicxulub impact site was instrumental in the collapse of marine ecosystems. A rebound to higher, more alkaline pH values (overshooting those of the preceding Late Cretaceous) was equally rapid. That is ascribed to the post-extinction dearth of marine organisms that take up calcium in their shells so that dissolved Ca became more abundant. Within less than 100 ka of the Chicxulub impact ocean pH had returned to its pre-impact levels. Since Deccan flood-basalt volcanism was active until long after, Henehan et al. consider that its influence on ocean acidification was minimal and that The Chicxulub impact ‘was key in driving end-Cretaceous mass extinction’.

Records of marine fossils are both more abundant and continuous than are those of land-based organisms. That animal extinctions on the continents were dramatic has been clear for over a century. Entire classes, notably the dinosaurs (except for birds), as well as orders, families, genera and species disappear from the fossil record. The event more than decimated plant taxa too. How and at what pace the vacated ecological niches were reoccupied during the evolutionary radiation among what became modern fauna and flora remain poorly understood. For the first million years of post-impact time fossils of terrestrial and freshwater organisms are very rare. Well-dated sedimentary sequences are patchily distributed, and fossils preserved in them as rare as proverbial hen’s teeth, apart from a few, better endowed strata separated by thick, unproductive sediments. A Lower Palaeocene site near Denver in Colorado, USA extends for 27 km. At first sight it does not impress palaeontologists, but it carries concretions that yield rich hauls of tiny vertebrate fossils. Dating using U-Pb dating of interleaved volcanic ash layers, stratigraphy based on normal and reversed polarity of remanent magnetism, and plant pollen variations. The 250 m thick sedimentary unit can be divided into 150 levels that represent the first million years flowing the Chicxulub impact (Lyson, T.R. and 15 others 2019. Paleogene mass extinction -Exceptional continental record of biotic recovery after the Cretaceous. Science, online first release; DOI: 10.1126/science.aay2268.

Reconstruction of the 35 kg early Palaeocene mammal Taeniolabis (credit: Wikipedia)

The levels contain abundant remains of early Cenozoic mammals, particularly skulls that are vitally important in taxonomy and size estimation. During the last few hundred thousand years of the Cretaceous, mammals about the size of a modern racoon (~8 kg) were abundant. The oldest Palaeocene holds nothing bigger than a 600 g rat, and few of them. Then, remarkably, the numbers, diversity and mean body mass of mammals grow; raccoon-size back within 100 ka then, in a series of steps, beasts around 25, 35 and 45 kg emerged successively during the next 600 ka. Clearly, the local food chain had to support this growth in size as well as numbers. Pollen records reveal a terrain first dominated by ferns – not especially nutritious – then after 200 ka by palms and finally legumes (pulses) appear. The diversification of animals and plants changed in lockstep. Studies of fossil-leaf shapes (toothed = cooler; smooth = warmer) indicated a similarly triple-stepwise amelioration in climate from cool, post-impact to hot by 65 Ma ago. This climatic warming may have been connected to successive pulses of Deccan volcanism that drove up atmospheric CO2 levels. Geologically, that is pretty quick. In the context of a possible, equally rapid mass extinction as a result of anthropogenic factors, such a pace of recovery is hardly reassuring…

Ancient oil migration

In order for petroleum deposits to form, the first requirement is a source of abundant hydrocarbons, most usually from a mudstone that was deposited under highly reducing conditions. In such an environment dead organic matter can accumulate without complete decay and oxidation to form a source rock or black shale. The next step comes from burial and heating until the dead matter matures to release liquid and gaseous hydrocarbons. In turn these fluids, along with heated water, must leave the impermeable source rock and migrate through more porous and permeable strata, such as sandstone or limestone reservoir rocks. Either they reach the surface to escape or become trapped in some kind of geological structure. In migrating, the hydrocarbons induce reducing condition in the rocks through which they flow, often bleaching them as the colouring agents based on insoluble iron-3 compounds are reduced to iron-2 that dissolves and is carried out of the system along with the hydrocarbons.

Throughout the Precambrian, the Earth was lacking in free or dissolved oxygen, even after the Great Oxidation Event at around 2.4 to 2.1 billion years ago; ideal conditions for the formation of black-shale source rocks. And indeed there are huge volumes of them going back to the Palaeoarchaean Era (>3.25 Ga). The Earth’s heat flow having be greater then, due to less decay of radioactive heat-producing elements in the mantle, petroleum must have been generated in volumes at least as large as that released during the Phanerozoic. Yet there are few oilfields of Precambrian age, and geologists usually don’t bother looking for oil in very ancient rocks, largely because the older a rock sequence is the more likely it has been deeply buried and heated above the temperature at which oil breaks down into hydrocarbon gases (~130°C), which in turn are destroyed above about 250°C. Moreover, many such ancient rocks have generally been deformed by many phases of brittle tectonic processes that formed zones of fracturing that give lines of easy escape for pressurised fluids.

Interleaved chert (white) and ironstone of the Palaeoproterozoic Gunflint Iron Formation of Ontario, Canada and Minnesota, USA.

So, looking for telltale signs of oil formation and migration in Precambrian strata is pretty much a matter of academic curiosity. Solid, bituminous hydrocarbons granules and veins are not uncommon in Precambrian sediments, although their relationships do not rule out later introduction into ancient rocks. Birger Rasmussen of the University of Western Australia has been tracking down such signs for over 30 years, his best known discovery – in 2005 – being in Archaean rocks (3.2 to 2.6 Ga) of the Pilbara craton in Western Australia. Recently, he and Janet Muhling of the same institution reported stunning evidence of migration in the Palaeoproterozoic Era (Rasmussen, B. & Muhling, J.R. 2019. Evidence for widespread oil migration in the 1.88 Ga Gunflint Formation, Ontario, Canada. Geology, v. 47, p. 899-903; DOI: 10.1130/G46469.1). The sedimentary unit is a banded iron formation containing interleaved cherts (famous for their content of some of the oldest incontrovertible microfossils), a granular variant of which is pervaded by solid bitumen in both granules and former pore spaces. This is interpreted as the result of oil migration during the actual cementation of the ironstone by silica; i.e. during diagenesis below the seabed rather than through solid sedimentary rock. Bitumen also fills later fractures. Rasmussen and Muhling consider the most likely scenario for this undoubted Palaeoproterozoic reservoir to have formed. They conclude that it coincided with the tectonic burial of the BIF basin beneath an exotic thrust block about 20 Ma after its formation. This generated petroleum from older source rocks, remote from the site of BIF deposition, that migrated away and up-dip from the thrust belt following the unconsolidated BIF formation.

Geochemical background to the Ediacaran explosion

The first clear and abundant signs of multicelled organisms appear in the geological record during the 635 to 541 Ma Ediacaran Period of the Neoproterozoic, named from the Ediacara Hills of South Australia where they were first discovered in the late 19th century. But it wasn’t until 1956, when schoolchildren fossicking in Charnwood Forest north of Leicester in Britain found similar body impressions in rocks that were clearly Precambrian age that it was realised the organism predated the Cambrian Explosion of life. Subsequently they have turned-up on all continents that preserve rocks of that age (see: Larging the Ediacaran, March 2011). The oldest of them, in the form of small discs, date back to about 610 Ma, while suspected embryos of multicelled eukaryotes are as old as the very start of the Edicaran (see; Precambrian bonanza for palaeoembryologists, August 2006).

Artist’s impression of the Ediacaran Fauna (credit: Science)

The Ediacaran fauna appeared soon after the Marinoan Snowball Earth glaciogenic sediments that lies at the top of the preceding Cryogenian Period (650-635 Ma), which began with far longer Sturtian glaciation (715-680 Ma). A lesser climatic event – the 580 Ma old Gaskiers glaciation – just preceded the full blooming of the Ediacaran fauna. Geologists have to go back 400 million years to find an earlier glacial epoch at the outset of the Palaeoproterozoic. Each of those Snowball Earth events was broadly associated with increased availability of molecular oxygen in seawater and the atmosphere. Of course, eukaryote life depends on oxygen. So, is there a connection between prolonged, severe climatic events and leaps in the history of life? It does look that way, but begs the question of how Snowball Earth events were themselves triggered. Continue reading “Geochemical background to the Ediacaran explosion”

A major Precambrian impact in Scotland

The northwest of Scotland has been a magnet to geologists for more than a century. It is easily accessed, has magnificent scenery and some of the world’s most complex geology. The oldest and structurally most tortuous rocks in Europe – the Lewisian Gneiss Complex – which span crustal depths from its top to bottom, dominate much of the coast. These are unconformably overlain by a sequence of mainly terrestrial sediments of Meso- to Neoproterozoic age – the Torridonian Supergroup – laid down by river systems at the edge of the former continent of  Laurentia. They form a series of relic hills resting on a rugged landscape carved into the much older Lewisian. In turn they are capped by a sequence of Cambrian to Lower Ordovician shallow-marine sediments. A more continuous range of hills no more than 20 km eastward of the coast hosts the famous Moine Thrust Belt in which the entire stratigraphy of the region was mangled between 450 and 430 million years ago when the elongated microcontinent of Avalonia collided with and accreted to Laurentia.  Exposures are the best in Britain and, because of the superb geology, probably every geologist who graduated in that country visited the area, along with many international geotourists. The more complex parts of this relatively small area have been mapped and repeatedly examined at scales larger than 1:10,000; its geology is probably the best described on Earth. Yet, it continues to throw up dramatic conclusions. However, the structurally and sedimentologically simple Torridonian was thought to have been done and dusted decades ago, with a few oddities that remained unresolved until recently.

NW Scotland geol
Grossly simplified geological map of NW Scotland (credit: British Geological Survey)

Continue reading “A major Precambrian impact in Scotland”

The effect of surface processes on tectonics

Active sedimentation in the Indus and Upper Ganges plains (green vegetated) derived from rapid erosion of the Himalaya (credit: Google Earth)

The Proterozoic Eon of the Precambrian is subdivided into the Palaeo-, Meso- and Neoproterozoic Eras that are, respectively, 900, 600 and 450 Ma long. The degree to which geoscientists are sufficiently interested in rocks within such time spans is roughly proportional to the number of publications whose title includes their name. Searching the ISI Web of Knowledge using this parameter yields 2000, 840 and 2700 hits in the last two complete decades, that is 2.2, 1.4 and 6.0 hits per million years, respectively. Clearly there is less interest in the early part of the Proterozoic. Perhaps that is due to there being smaller areas over which they are exposed, or maybe simply because what those rocks show is inherently less interesting than those of the Neoproterozoic. The Neoproterozoic is stuffed with fascinating topics: the appearance of large-bodied life forms; three Snowball Earth episodes; and a great deal of tectonic activity, including the Pan-African orogeny. The time that precedes it isn’t so gripping: it is widely known as the ‘boring billion’ – coined by the late Martin Brazier – from about 1.75 to 0.75 Ga. The Palaeoproterozoic draws attention by encompassing the ‘Great Oxygenation Event’ around 2.4 Ga, the massive deposition of banded iron formations up to 1.8 Ga, its own Snowball Earth, emergence of the eukaryotes and several orogenies. The Mesoproterozoic witnesses one orogeny, the formation of a supercontinent (Rodinia) and even has its own petroleum potential (93 billion barrels in place in Australia’s Beetaloo Basin. So it does have its high points, but not a lot. Although data are more scanty than for the Phanerozoic Eon, during the Mesoproterozoic the Earth’s magnetic field was much steadier than in later times. That suggests that motions in the core were in a ‘steady state’, and possibly in the mantle as well. The latter is borne out by the lower pace of tectonics in the Mesoproterozoic. Continue reading “The effect of surface processes on tectonics”

Plants first to succumb to the end-Permian event

We have become accustomed to thinking that up to 90% of organisms were snuffed out by the catastrophe at the Permian-Triassic boundary 252 Ma ago. Those are the figures for marine organisms, whose record in sediments is the most complete. It has also been estimated to have lasted a mere 60 ka, and the recovery in the Early Triassic to have taken as long as 10 Ma. There are hints of three separate pulses of extinction related to: initial gas emission from the Siberian Traps; coal fires; and release of methane from sea-floor gas hydrates at the peak of global warming. Various terrestrial sequences record the collapse of dense woodlands, so that the Early Triassic is devoid of coals that are widespread in the preceding Late Permian. A new detailed study of terrestrial sediments in the Sydney Basin of eastern Australia reveals something new (Fielding, C.R. and 10 others 2019. Age and pattern of the southern high-latitude continental end-Permian extinction constrained by multiproxy analysis. Nature Communications, v. 10, online publications: DOI: 10.1038/s41467-018-07934-z).

The distinctive, tongue-like form of Glossopteris leaves that dominate the coal-bearing Permian strata of the southern coninents. Their occurrence in South America, Africa, India, Australia, New Zealand, and Antarctica prompted Alfred Wegener to suggest that these modern continents had been united in Pangaea by Permian times: a key to continental drift. (Credit: Getty Images)

Christopher Fielding or the University of Nebraska-Lincoln and colleagues focused on pollens, geochemistry and detailed dating of the sedimentary succession across the P-Tr boundary exposed on the New South Wales coast. The stratigraphy is intricately documented by a 1 km deep well core that penetrates a more or less unbroken fluviatile and deltaic sequence that contains eleven beds of volcanic ash. The igneous layers are key to calibrating age throughout the sequence (259.10 ± 0.17 to 247.87 ± 0.11 Ma using zircon U-Pb methods). The pollens change abruptly from those of a Permian flora, dominated by tongue-like glossopterid plants, to a different association that includes conifers. The change coincides with a geochemical ‘spike’ in the abundance of nickel and a brief change in the degree of alteration of detrital fledspars to clay minerals. The first implicates the delivery of massive amounts of nickel to the atmosphere, probably by the eruption of the Siberian Traps , which contain major economic nickel deposits. The second feature suggests a brief period of warmer and more humid climatic conditions. A third geochemical change is the onset of oscillations in the abundance of 13C that are thought to record major changes in plant life across the planet. These features would have been an easily predicted association with the 252 Ma mass extinction were it not for the fact that the radiometric dating places them about 400 thousand years before the well-known changes in global animal life. Detailed dating of the Siberian Traps links the collapse of Glossopteris and coal formation to the earliest extrusion of flood basalts, which suggests that the animal extinctions were driven by cumulative effects of the later outpourings

Related article: Chris Fielding comments on the paper at Nature Research/Ecology and Evolution

Read more on Palaeobiology and Stratigraphy

Calibrating 14C dating

Radiocarbon dating is the most popular tool for assessing the ages of archaeological remains and producing climatic time series, as in lake- and sea-floor cores, provided that organic material can be recovered. Its precision has steadily improved, especially with the development of accelerator mass spectrometry, although it is still limited to the last 50 thousand years or so because of the short half-life of 14C (about 5,730 years,). The problem with dating based on radioactive 14C is its accuracy; i.e. does it always give a true date. This stems from the way in which 14C is produced – by cosmic rays interacting with nitrogen in the atmosphere. Cosmic irradiation varies with time and, consequently, so does the proportion of 14C in the atmosphere. It is the isotope’s proportion in atmospheric CO2 gas at any one time in the past, which is converted by photosynthesis to dateable organic materials, that determines the proportion remaining in a sample after decay through the time since the organism died and became fossilised. Various approaches have been used to allow for variations in 14C production, such as calibration to the time preserved in ancient timber by tree rings which can be independently radiocarbon dated. But that depends on timber from many different species of tree from different climatic zones, and that is affected by fractionation between the various isotopes of carbon in CO2, which varies between species of plant. But there is a better means of calibration.

The carbonate speleothem that forms stalactites and stalagmites by steady precipitation from rainwater, sometimes to produce visible layering, not only locks in 14C dissolved from the atmosphere by rainwater but also environmental radioactive isotopes of uranium and thorium. So, layers in speleothem may be dated by both methods for the period of time over which a stalagmite, for instance, has grown. This seems an ideal means of calibration, although there are snags; one being that the proportion of carbon in carbonates is dominated by that from ancient limestone that has been dissolved by slightly acid rainwater, which dilutes the amount of 14C in samples with so called ‘dead carbon’. Stalagmites in the Hulu Cave near Nanjing in China have particularly low dead-carbon fractions and have been used for the best calibrations so far, going back the current limit for radiocarbon dating of 54 ka (Cheng, H. and 14 others 2018. Atmospheric 14C/12C during the last glacial period from Hulku Cave. Science, v. 362, p. 1293-1297; DOI: 10.1126/science.aau0747). Precision steadily falls off with age because of the progressive reduction to very low amounts of 14C in the samples. Nevertheless, this study resolves fine detail not only of cosmic ray variation, but also of pulses of carbon dioxide release from the oceans which would also affect the availability of 14C for incorporation in organic materials because deep ocean water contains ‘old’ CO2.

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The great Cambrian unconformity

My first field trip from the Geology Department at the University of Birmingham in autumn 1964 was located within hooter distance of the giant British Leyland car plant at Longbridge. It involved a rubbish-filled linear quarry behind a row of shops on the main road through south Birmingham. Not very prepossessing but it clearly exposed a white quartzite, which we were told was a beach deposit laid down by a massive marine transgression at the start of the Cambrian. An hour later we were shown an equally grim exposure of weathered volcanic rocks in the Lickey Hills; they were a sort of purple brown, and said to be Precambrian in age. Not an excellent beginning to a career, but from time to time other Cambrian quartzites sitting unconformably on Precambrian rocks entered our field curriculum: in the West Midlands, Welsh Borders and much further afield in NW Scotland, as it transpired on what had been two separate continental masses of Avalonia and Laurentia. This had possibly been a global marine transgression.

In North America, then the Laurentian continent, what John Wesley Powell dubbed the Great Unconformity in the Grand Canyon has as its counterpart to the Lickey Quartzite the thrillingly named Tonto Group of the Lower Cambrian resting on the Vishnu Schists that are more than a billion years older. Part of the Sauk Sequence, the Tonto Group is, sadly, not accompanied by the Lone Ranger Group, but the Cambrian marine transgression crops out across the continent. In fact it was a phenomenon common to all the modern continents. Global sea level rose relative to the freeboard of the continents then existing. A recent study has established the timing for the Great Unconformity in the Grand Canyon by dating detrital zircons above and below the unconformity (Karlstrom, K, et al. 2018. Cambrian Sauk transgression in the Grand Canyon region redefined by detrital zircons. Nature Geoscience, v. 11, p. 438-443; doi:10.1038/s41561-018-0131-7). Rather than starting at the outset of the Cambria at 542 Ma, the marine transgression was a protracted affair that began around 527 Ma with flooding reaching a maximum at the end of the Cambrian.

Extensive flooding of the continents at the end of the Cambrian (credit: Ron Blakey , Colorado Plateau Geosystems)

It seems most likely that the associated global rise in sea level relative to the continents was a response to the break-up of the Rodinia supercontinent by considerable sea-floor spreading. The young ocean floor, having yet to cool to an equilibrium temperature, would have had reduced density so that the average depth of the ocean basins decreased, thereby flooding the continents. The creation of vast shallow seas across the continents has been suggested to have been a major factor in the explosive evolution of Cambrian shelly faunas, partly by expanding the range of ecological niches and partly due to increased release of calcium ions to to seawater as a result of chemical weathering.

A fully revised edition of Steve Drury’s book Stepping Stones: The Making of Our Home World can now be downloaded as a free eBook

Late Palaeozoic glacial features in Chad

The longest and most extreme glacial epoch during the Phanerozoic took place between 360 and 260 Ma ago, when it dominated the Carboniferous and Permian sedimentary sequences across the planet. On continents that lay athwart the Equator during these times, sedimentation was characterised by cycles between shallow marine and terrestrial conditions. These are epitomised by the recurring ‘Coal-Measure’ cyclothem of, from bottom to top: open-sea limestone; near-shore marine mudstone; riverine sandstone; coal formed in swamps. This sequence represents a rapid rise in sea level as ice sheets melted, sustained during an interglacial episode and then falling sea level as ice once again accumulated on land to culminate in a glacial maximum when coal formed in coastal mires. During the Late Palaeozoic Era a single supercontinent extended from pole to pole. The break-up of Pangaea was charted by Alfred Wegener in 1912, partly by his using glacial deposits and ice-gouged striations on the southern continents. With the present widely separated configuration of major landmasses glacial sediments and the directions of inferred ice movements could only be reconciled by reassembling Africa, India, South America, Antarctica and Australia in the form of a single, congruent southern continent that he called Gondwanaland. In Wegener’s reconstruction the glacial features massed together on Gondwanaland with the striations radiating outwards from what would then have been the centre of a huge ice cap.

There are many localities on the present southern continents where such striations can be seen on the surface of peneplains etched into older rocks that underlie Carboniferous to Permian tillites, but later erosion has removed the continuity of the original glacial landscape. There are, however, some parts of central Africa where it is preserved. By using the high-resolution satellite images (with pixels as small as 1 m square) that are mosaiced together in Google Earth, Daniel Paul Le Heron of Royal Holloway, University of London has revealed a series of 1 to 12 km wide sinuous belts in a 6000 km2 area of eastern Chad that are superimposed unconformably on pre-Carboniferous strata (Le Heron, D.P. 2018. An exhumed Paleozoic glacial landscape in Chad. Geology, v.46(1), p. 91-94; doi:10.1130/G39510.1). They comprise irregular tracts of sandstone to the south of a major Carboniferous sedimentary basin. Zooming in to them (try using 17.5° N 22.25°E as a search term in Google Earth) reveals surfaces dominated by wavy, roughly parallel lines. Le Heron interprets these as mega-scale glacial lineations, formed by ice flow across underlying soft Carboniferous glacial sediments as seen in modern glacial till landforms in Canada. In places they rest unconformably on older rocks, sometimes standing above the level of the sandstone plateaux as relics of what may have been nunataks. There are even signs of elliptical drumlins.

An oblique Google Earth view looking to the south-east shows mega-scale glacial lineations from a glacial flow way in eastern Chad. The lower-right quadrant shows the unconformity atop older bedded strata that are dipping to the west. Click on the image to see a full resolution view. (Credit: Google Earth)

Glacial tillites and glaciofluvial sediments of Late Palaeozoic age are common across the Sahara and in the Sahelian belt, but in areas as remote as those in eastern Chad. So a systematic survey using the resolving power of Google Earth may well yield yet more examples. It is tedious work in such vast areas, unless, of course, one bears in mind Alfred Wegener, the founder of the hypothesis of continental drift and ‘Big’ Earth Science as a whole, who would have been gleeful at the opportunity.

A fully revised edition of Steve Drury’s book Stepping Stones: The Making of Our Home World can now be downloaded as a free eBook

Banded iron formations (BIFs) reviewed

During most of the last hundred years every car body, rebar rod in concrete, ship, bridge and skyscraper frame had its origins in vividly striped red rocks from vast open-pit mines. Comprising mainly iron oxides with some silica, these banded iron formations, or BIFs for short, occur in profitable tonnages on every continent.

This image shows a 2.1 billion years old rock ...
2.1 billion years old boulder of banded ironstone. (credit: Wikipedia)

This article can now be read in full at Earth-logs in the Sedimentology and stratigraphy archive for 2017