Cretaceous–Paleogene extinction event

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Artist's rendering of a bolide impact
A Wyoming (U.S.) rock with an intermediate claystone layer that contains 1000 times more iridium than the upper and lower layers. Picture taken at the San Diego Natural History Museum
Complex Cretaceous–Paleogene clay layer (gray) in the Geulhemmergroeve tunnels near Geulhem, The Netherlands. Finger is on the actual Cretaceous-Paleogene boundary.

The Cretaceous–Paleogene (K–Pg) extinction event,[a] formerly known as the Cretaceous–Tertiary (K–T) extinction,[b] was a mass extinction of some three-quarters of plant and animal species on Earth—including all non-avian dinosaurs—that occurred over a geologically short period of time 66 million years (Ma) ago.[2][3] It marked the end of the Cretaceous period and with it, the entire Mesozoic Era, opening the Cenozoic Era which continues today.


As originally proposed by a team of scientists led by Luis Alvarez, it is now generally believed that the K–Pg extinction was triggered by a massive comet/asteroid impact and its catastrophic effects on the global environment, including a lingering impact winter that made it impossible for plants and plankton to carry out photosynthesis.[4] The impact hypothesis was bolstered by the discovery of the 180-kilometre-wide (112 mi) Chicxulub crater in the Gulf of Mexico in the early 1990s,[5] which provided conclusive evidence that the K–Pg boundary clay represented debris from an asteroid impact.[6] The fact that the extinctions occurred at the same time as the impact provides strong situational evidence that the K–Pg extinction was caused by the asteroid.[6] However, some scientists maintain the extinction was caused or exacerbated by other factors, such as volcanic eruptions,[7] climate change, and/or sea level change.

A wide range of species perished in the K–Pg extinction. The most well-known victims are the non-avian dinosaurs. However, the extinction also destroyed a plethora of other terrestrial organisms, including but not limited to; mammals, pterosaurs, birds,[8] lizards,[9] insects,[10][11] and plants.[12] In the oceans, the K–Pg extinction devastated the giant marine lizards (Mosasauridae), plesiosaurs, fish,[13] sharks, mollusks (especially ammonites) and many species of plankton. It is estimated that 75% or more of all species on Earth vanished.[14] Yet the devastation caused by the extinction also provided evolutionary opportunities. In the wake of the extinction, many groups underwent remarkable adaptive radiations — a sudden and prolific divergence into new forms and species within the disrupted and emptied ecological niches resulting from the event. Mammals in particular diversified in the Paleogene,[15] producing new forms such as horses, whales, bats, and primates. Birds,[16] fish[17] and perhaps lizards[9] also radiated.

Extinction patterns[edit]

Marine extinction intensity during the Phanerozoic eon
Millions of years ago

The K–Pg extinction event was severe, global, rapid, and selective. In terms of severity, the event eliminated a vast number of species. Based on marine fossils, it is estimated that 75% or more of all species were wiped out by the K–Pg extinction.[18] This is a rough estimate. It is difficult to estimate diversity for modern ecosystems, let alone for fossil ones, and the data are derived primarily from marine invertebrates. Terrestrial organisms, especially insects, represent much of the diversity, but have a poorer record. Despite this, the high levels of extinction seen in terrestrial and marine fossils indicate that the K–Pg extinction is the most severe extinction in the past 250 million years.

The K–Pg extinction was a global event. The event appears to have hit all continents at the same time. Dinosaurs, for example, are known from the Maastrichtian of North America, Europe, Asia, Africa, South America and Antarctica,[19] but are unknown from the Cenozoic anywhere in the world. Similarly, fossil pollen show devastation of the plant communities in areas as far flung as New Mexico, Alaska, China, and New Zealand.[12] The event also affected all seas and oceans. Widespread groups such as mosasaurs and ammonites disappeared around the world. Furthermore, the extinctions occurred at the same time on land and in the sea.

The fossil record shows that the tempo of the K–Pg extinction was extremely rapid, occurring on a scale of thousands of years or less.[citation needed] In some cases, it is possible to study fossils on a very fine scale - centimeter-by-centimeter - through the K–Pg rocks. Examples include marine microfossils, such as calcareous nanoplankton and foraminifera, and terrestrial plant pollen. Here, the fossils show that the ecosystem remained relatively stable up to the K–Pg boundary, at which point many species suddenly vanish. For groups with a poorer fossil record, such as dinosaurs, fossils are unlikely to be preserved just below the K–Pg boundary. For example, only a few dozen Tyrannosaurus skeletons are known, and so the odds of finding one a few centimeters below the boundary are low. This effect, called the Signor–Lipps effect, causes many species to appear to vanish before the K–Pg boundary, creating the illusion of gradual extinction. Nevertheless, improved sampling shows that groups once thought to undergo a slow decline, such as dinosaurs, actually disappear suddenly near the K–Pg boundary. Reworking—when fossils are eroded from older rocks and deposited into younger rocks—can also make extinction appear gradual. For example, in the Bug Creek Anthills beds in Montana, dinosaur fossils occur alongside mammals from the earliest Paleocene, which created the illusion that dinosaurs dwindled as mammals radiated. Reworked fossils are recognized because they tend to be rare and are often damaged by the reworking.

The patterns are critical to understanding the cause of the extinctions. The fact that the extinction is severe, global, and rapid suggests that the extinctions result from a severe, global, and rapid environmental disturbance: an environmental catastrophe. In the 1970s and 1980s, this led scientists to seriously consider catastrophic mechanisms such as supernovas, volcanic eruptions, and asteroids, and sparked new interest in catastrophism in geology and paleontology.

The extinction was also highly selective. Some groups were relatively unaffected, others were devastated, and some were eliminated entirely. Many species of alligator, turtle, and salamander survived, for example. Mammals, birds, and lizards suffered high rates of extinction. Non-avian dinosaurs and pterosaurs were wiped out entirely.

Even though the boundary event was severe, there was significant variability in the rate of extinction between and within different clades. Species that depended on photosynthesis declined or became extinct as atmospheric particles blocked sunlight and reduced the solar energy reaching the Earth's surface. This plant extinction caused a major reshuffling of the dominant plant groups.[20] Photosynthesizing organisms, including phytoplankton and land plants, formed the foundation of the food chain in the late Cretaceous as they do today. Evidence suggests that herbivorous animals died out when the plants they depended on for food became scarce. Consequently, top predators such as Tyrannosaurus rex also perished.

Coccolithophorids and molluscs (including ammonites, rudists, freshwater snails and mussels), and those organisms whose food chain included these shell builders, became extinct or suffered heavy losses. For example, it is thought that ammonites were the principal food of mosasaurs, a group of giant marine reptiles that became extinct at the boundary.[21]

Omnivores, insectivores and carrion-eaters survived the extinction event, perhaps because of the increased availability of their food sources. At the end of the Cretaceous there seems to have been no purely herbivorous or carnivorous mammals. Mammals and birds that survived the extinction fed on insects, worms, and snails, which in turn fed on dead plant and animal matter. Scientists hypothesize that these organisms survived the collapse of plant-based food chains because they fed on detritus (non-living organic material).[22][23][24]

In stream communities few animal groups became extinct because stream communities rely less directly on food from living plants and more on detritus that washes in from land, buffering them from extinction.[25] Similar, but more complex patterns have been found in the oceans. Extinction was more severe among animals living in the water column than among animals living on or in the sea floor. Animals in the water column are almost entirely dependent on primary production from living phytoplankton while animals living on or in the ocean floor feed on detritus or can switch to detritus feeding.[22]




The K–Pg boundary represents one of the most dramatic turnovers in the fossil record for various calcareous nanoplankton that formed the calcium deposits that gave the Cretaceous its name. The turnover in this group is clearly marked at the species level.[26][27] Statistical analysis of marine losses at this time suggests that the decrease in diversity was caused more by a sharp increase in extinctions than by a decrease in speciation.[28] The K–Pg boundary record of dinoflagellates is not as well-understood, mainly because only microbial cysts provide a fossil record, and not all dinoflagellate species have cyst-forming stages, thereby likely causing diversity to be underestimated.[22] Recent studies indicate that there were no major shifts in dinoflagellates through the boundary layer.[29]

Radiolaria have left a geological record since at least the Ordovician times, and their mineral fossil skeletons can be tracked across the K–Pg boundary. There is no evidence of mass extinction of these organisms, and there is support for high productivity of these species in southern high latitudes as a result of cooling temperatures in the early Paleocene.[22] Approximately 46% of diatom species survived the transition from the Cretaceous to the Upper Paleocene. This suggests a significant turnover in species, but not a catastrophic extinction of diatoms, across the K–Pg boundary.[22][30]

The occurrence of planktonic foraminifera across the K–Pg boundary has been studied since the 1930s.[31][32] Research spurred by the possibility of an impact event at the K–Pg boundary resulted in numerous publications detailing planktonic foraminiferal extinction at the boundary.[22] However, there is debate ongoing between groups that believe the evidence indicates substantial extinction of these species at the K–Pg boundary,[33] and those who believe the evidence supports multiple extinctions and expansions through the boundary.[34][35]

Numerous species of benthic foraminifera became extinct during the K–Pg extinction event, presumably because they depend on organic debris for nutrients, since the biomass in the ocean is thought to have decreased. However, as the marine microbiota recovered, it is thought that increased speciation of benthic foraminifera resulted from the increase in food sources.[22] Phytoplankton recovery in the early Paleocene provided the food source to support large benthic foraminiferal assemblages, which are mainly detritus-feeding. Ultimate recovery of the benthic populations occurred over several stages lasting several hundred thousand years into the early Paleocene.[36][37]

Marine invertebrates[edit]


There is variability in the fossil record as to the extinction rate of marine invertebrates across the K–Pg boundary. The apparent rate is influenced by the lack of fossil records rather than actual extinction.[22]

Ostracods, a class of small crustaceans that were prevalent in the upper Maastrichtian, left fossil deposits in a variety of locations. A review of these fossils shows that ostracode diversity was lower in the Paleocene than any other time in the Cenozoic. However, current research cannot ascertain whether the extinctions occurred prior to or during the boundary interval itself.[38][39]


The numbers of cephalopod, echinoderm, and bivalve genera exhibited significant diminution after the K–Pg boundary.[22] Most species of brachiopods, a small phylum of marine invertebrates, survived the K–Pg extinction event and diversified during the early Paleocene.






There are substantial fossil records of jawed fishes across the K–Pg boundary, which provides good evidence of extinction patterns of these classes of marine vertebrates. Within cartilaginous fish, approximately 80% of the sharks, rays, and skates families survived the extinction event,[22] and more than 90% of teleost fish (bony fish) families survived.[47] There is evidence of a mass kill of bony fishes at a fossil site immediately above the K–Pg boundary layer on Seymour Island near Antarctica, apparently precipitated by the K–Pg extinction event.[48] However, the marine and freshwater environments of fishes mitigated environmental effects of the extinction event.[49]

Terrestrial invertebrates[edit]

Insect damage to the fossilized leaves of flowering plants from fourteen sites in North America were used as a proxy for insect diversity across the K–Pg boundary and analyzed to determine the rate of extinction. Researchers found that Cretaceous sites, prior to the extinction event, had rich plant and insect-feeding diversity. However, during the early Paleocene, flora were relatively diverse with little predation from insects, even 1.7 million years after the extinction event.[50][51]

Terrestrial plants[edit]

There is overwhelming evidence of global disruption of plant communities at the K–Pg boundary.[12][12][52][53] Extinctions are seen both in studies of fossil pollen, and fossil leaves.[12] In North America, the data suggest massive devastation and mass extinction of plants at the K–Pg boundary sections, although there were substantial megafloral changes before the boundary.[12][54] In North America, approximately 57% of plant species became extinct. In high southern hemisphere latitudes, such as New Zealand and Antarctica the mass die-off of flora caused no significant turnover in species, but dramatic and short-term changes in the relative abundance of plant groups.[50][55] In some regions, Paleocene recovery of plants began with recolonizations by fern species, represented as a fern spike in the geologic record; this same pattern of fern recolonization was observed after the 1980 Mount St. Helens eruption.[56] However the patterns of recovery were quite variable. Different fern species were responsible for the fern spike in different areas, and in some regions, no fern spike is evident.

Due to the wholesale destruction of plants at the K–Pg boundary there was a proliferation of saprotrophic organisms such as fungi that do not require photosynthesis and use nutrients from decaying vegetation. The dominance of fungal species lasted only a few years while the atmosphere cleared and there was plenty of organic matter to feed on. Once the atmosphere cleared, photosynthetic organisms like ferns and other plants returned.[57] Polyploidy appears to have enhanced the ability of flowering plants to survive the extinction, probably because the additional copies of the genome such plants possessed allowed them to more readily adapt to the rapidly changing environmental conditions that followed the impact.[58]


There is limited evidence for extinction of amphibians at the K–Pg boundary. A study of fossil vertebrates across the K–Pg boundary in Montana concluded that no species of amphibian became extinct.[59] Yet there are several species of Maastrichtian amphibian, not included as part of this study, which are unknown from the Paleocene. These include the frog Theatonius lancensis [60] and the albanerpetontid Albanerpeton galaktion;[61] therefore some amphibians do seem to have become extinct at the boundary. The relatively low levels of extinction seen among amphibians probably reflect the low extinction rates seen in freshwater animals.[62]

Non-archosaur reptiles[edit]

Large marine reptiles such as mosasaurs and plesiosaurs died out by the end of the Cretaceous.

The two living non-archosaurian reptile taxa, testudines (turtles) and lepidosaurs (snakes, lizards, and amphisbaenians (worm lizards)), along with choristoderes (semi-aquatic archosauromorphs that died out in the early Miocene), survived through the K–Pg boundary.[22] Over 80% of Cretaceous turtle species passed through the K–Pg boundary. Additionally, all six turtle families in existence at the end of the Cretaceous survived into the Paleogene and are represented by current species.[63] Living lepidosaurs include Rhynchocephalia (tuataras) and Squamata. The Rhynchocephalia were a widespread and relatively successful group of lepidosaurs in the early Mesozoic, but began to decline by the mid-Cretaceous. They are represented today by a single genus located exclusively in New Zealand.[64]

The order Squamata, which is represented today by lizards, snakes, and amphisbaenians, radiated into various ecological niches during the Jurassic and were successful throughout the Cretaceous. They survived through the K–Pg boundary and are currently the most successful and diverse group of living reptiles with more than 6,000 extant species. No known family of terrestrial squamates became extinct at the boundary, and fossil evidence indicates they did not suffer any significant decline in numbers. Their small size, adaptable metabolism, and ability to move to more favorable habitats were key factors in their survivability during the late Cretaceous and early Paleocene.[22][63] Giant non-archosaurian aquatic reptiles such as mosasaurs and plesiosaurs, which were the top marine predators of their time, became extinct by the end of the Cretaceous.[65][66] This is most likely due to their size, which meant they were less able to adapt during the aftermath of the extinction event.


The archosaur clade includes two living orders, crocodilians (of which Alligatoridae, Crocodylidae and Gavialidae are the only surviving families) and dinosaurs (of which birds are the sole surviving members), along with the extinct non-avian dinosaurs and pterosaurs.


Ten families of crocodilians or their close relatives are represented in the Maastrichtian fossil records, of which five died out prior to the K–Pg boundary.[67] Five families have both Maastrichtian and Paleocene fossil representatives. All of the surviving families of crocodyliforms inhabited freshwater and terrestrial environments—except for the Dyrosauridae, which lived in freshwater and marine locations. Approximately 50% of crocodyliform representatives survived across the K–Pg boundary, the only apparent trend being that no large crocodiles survived.[22] Crocodyliform survivability across the boundary may have resulted from their aquatic niche and ability to burrow, which reduced susceptibility to negative environmental effects at the boundary.[49] Jouve and colleagues suggested in 2008 that juvenile marine crocodyliforms lived in freshwater environments like modern marine crocodile juveniles, which would have helped them survive where other marine reptiles became extinct; freshwater environments were not as strongly affected by the K–Pg extinction event as marine environments.[68]

The Choristodera, a generally crocodile-like group of uncertain phylogeny (possibly archosaurian) also survived the event, only to go extinct in the Miocene.[69]


One family of pterosaurs, Azhdarchidae, was definitely present in the Maastrichtian, and it became extinct at the K–Pg boundary. These large pterosaurs were the last representatives of a declining group that contained 10 families during the mid-Cretaceous. Smaller pterosaurs became extinct prior to the Maastrichtian during a period that saw a decline in smaller animal species while larger species became more prevalent. Recently, several pterosaur taxa have been discovered dating to the Campanian/Maastrichtian, such as the ornithocheirids Piksi and "Ornithocheirus", possible pteranodontids and nyctosaurids, and a tapejarid.[70] While this was occurring, modern birds were undergoing diversification and replacing archaic birds and pterosaur groups, possibly due to direct competition, or they simply filled empty niches.[49][71][72] However, ecological overlap between birds and pterosaurs seems to have been minimal,[73][74][75] and it appears that pterosaur extinction seems to coincide with a bizarre "diversity freeze", with the sudden radiation of species in the Lower Cretaceous apparently simply ceasing to diversify, leaving them vulnerable to minor extinction events like the Cretaceous Thermal Maximum[76]


Most paleontologists regard birds as the only surviving dinosaurs (see Origin of birds). However, all non-neornithean birds became extinct, including flourishing groups like enantiornithines and hesperornithiforms.[77] Several analyses of bird fossils show divergence of species prior to the K–Pg boundary, and that duck, chicken and ratite bird relatives coexisted with non-avian dinosaurs.[78] Large collections of bird fossils representing a range of different species provides definitive evidence for the persistence of archaic birds to within 300,000 years of the K–Pg boundary. None of them are known to survive into the Paleogene, and their persistence into the latest Maastrichtian therefore provides strong evidence for a mass extinction of archaic birds coinciding with the Chicxulub asteroid impact. A small fraction of the Cretaceous bird species survived the impact, giving rise to today's birds.[79][80] So far, only a single bird species, which has not been named, has been confidently identified from both above and below the K–Pg boundary (it is present in the Maastrichtian Hell Creek Formation and Danian Fort Union Formation).[79] The only bird group known for certain to have survived the K–Pg boundary is the Neornithines (though one Paleogene species, Qinornis paleocenica, may represent a surviving non-neornithine bird).[79] Neornithines may have been able to survive the extinction as a result of their abilities to dive, swim, or seek shelter in water and marshlands. Many species of neornithines can build burrows, or nest in tree holes or termite nests, all of which provided shelter from the environmental effects at the K–Pg boundary. Long-term survival past the boundary was assured as a result of filling ecological niches left empty by extinction of non-avian dinosaurs.[49]

Non-avian dinosaurs[edit]

Tyrannosaurus was one of the last dinosaurs to live on Earth before the extinction.

Excluding a few controversial claims, scientists agree that all non-avian dinosaurs became extinct at the K–Pg boundary. The dinosaur fossil record has been interpreted to show both a decline in diversity and no decline in diversity during the last few million years of the Cretaceous, and it may be that the quality of the dinosaur fossil record is simply not good enough to permit researchers to distinguish between the options.[81] Since there is no evidence that late Maastrichtian nonavian dinosaurs could burrow, swim or dive, they were unable to shelter themselves from the worst parts of any environmental stress that occurred at the K–Pg boundary. It is possible that small dinosaurs (other than birds) did survive, but they would have been deprived of food as both herbivorous dinosaurs would have found plant material scarce, and carnivores would have quickly found prey in short supply.[49]

The growing consensus about the endothermy of dinosaurs (see dinosaur physiology) helps to understand their full extinction in contrast with their close relatives, the crocodilians. Ectothermic ("cold-blooded") crocodiles have very limited needs for food (they can survive several months without eating) while endothermic ("warm-blooded") animals of similar size need much more food to sustain their faster metabolism. Thus, under the circumstances of food chain disruption previously mentioned, non-avian dinosaurs died,[20] while some crocodiles survived. In this context, the survival of other endothermic animals, such as some birds and mammals, could be due, among other reasons, to their smaller needs for food, related to their small size at the extinction epoch.[82]

Whether the extinction occurred gradually or very suddenly has been debated, as both views have support in the fossil record. A study of 29 fossil sites in Catalan Pyrenees of Europe in 2010 supports that dinosaurs there had great diversity until the asteroid impact, with over 100 living species.[83] However, more recent research indicates that this figure is obscured by taphonomical biases and the scarcity of the continental fossil record. The results of this study, which were based on estimated real global biodiversity, showed that between 628 and 1078 non-avian dinosaur species were alive at the end of the Cretaceous and underwent sudden extinction after the Cretaceous–Paleogene extinction event.[84] Alternatively, interpretation based on the fossil bearing rocks along the Red Deer River in Alberta, Canada, supports the gradual extinction of non-avian dinosaurs; during the last 10 million years of the Cretaceous layers there, the number of dinosaur species seems to have decreased from about 45 to about 12. Other scientists have pointed out the same.[85]

Several researchers support the existence of Paleocene dinosaurs. Evidence of this existence is based on the discovery of dinosaur remains in the Hell Creek Formation up to 1.3 m (4.3 ft) above and 40,000 years later than the K–Pg boundary.[86] Pollen samples recovered near a fossilized hadrosaur femur recovered in the Ojo Alamo Sandstone at the San Juan River indicate that the animal lived during the Cenozoic, approximately 64.5 Ma (about 1 million years after the K–Pg extinction event). If their existence past the K–Pg boundary can be confirmed, these hadrosaurids would be considered a dead clade walking.[87] Scientific consensus is that these fossils were eroded from their original locations and then re-buried in much later sediments (also known as reworked fossils).[88]

Hell Creek formation


All major Cretaceous mammalian lineages, including monotremes (egg-laying mammals), multituberculates, marsupials and placentals, dryolestoideans,[89] and gondwanatheres[90] survived the K–Pg extinction event, although they suffered losses. In particular, marsupials largely disappeared from North America, and the Asian deltatheroidans, primitive relatives of extant marsupials, became extinct.[91] In the Hell Creek beds of North America, at least half of the ten known multituberculate species and all eleven marsupial species are not found above the boundary.[81]

Mammalian species began diversifying approximately 30 million years prior to the K–Pg boundary. Diversification of mammals stalled across the boundary.[92] Current research indicates that mammals did not explosively diversify across the K–Pg boundary, despite the environment niches made available by the extinction of dinosaurs.[93] Several mammalian orders have been interpreted as diversifying immediately after the K–Pg boundary, including Chiroptera (bats) and Cetartiodactyla (a diverse group that today includes whales and dolphins and even-toed ungulates),[93] although recent research concludes that only marsupial orders diversified after the K–Pg boundary.[92]

K–Pg boundary mammalian species were generally small, comparable in size to rats; this small size would have helped them to find shelter in protected environments. In addition, it is postulated that some early monotremes, marsupials, and placentals were semiaquatic or burrowing, as there are multiple mammalian lineages with such habits today. Any burrowing or semiaquatic mammal would have had additional protection from K–Pg boundary environmental stresses.[49]


North American fossils[edit]

In North American terrestrial sequences, the extinction event is best represented by the marked discrepancy between the rich and relatively abundant late-Maastrichtian palynomorph record and the post-boundary fern spike.[52]

At present the most informative sequence of dinosaur-bearing rocks in the world from the K–Pg boundary is found in western North America, particularly the late Maastrichtian-age Hell Creek Formation of Montana, US. This formation, when compared with the older (approximately 75 Ma) Judith River/Dinosaur Park Formations (from Montana, USA, and Alberta, Canada, respectively) provides information on the changes in dinosaur populations over the last 10 million years of the Cretaceous. These fossil beds are geographically limited, covering only part of one continent.[81]

The middle–late Campanian formations show a greater diversity of dinosaurs than any other single group of rocks. The late Maastrichtian rocks contain the largest members of several major clades: Tyrannosaurus, Ankylosaurus, Pachycephalosaurus, Triceratops and Torosaurus,[94] which suggests food was plentiful immediately prior to the extinction.

In addition to rich dinosaur fossils, there are also plant fossils that illustrate the reduction in plant species across the K–Pg boundary. In the sediments below the K–Pg boundary the dominant plant remains are angiosperm pollen grains, but the actual boundary layer contains little pollen and is dominated by fern spores.[95] Normal pollen levels gradually resume above the boundary layer. This is reminiscent of areas blighted by modern volcanic eruptions, where the recovery is led by ferns, which are later replaced by larger angiosperm plants.[96]

Marine fossils[edit]

The mass extinction of marine plankton appears to have been abrupt and right at the K–Pg boundary.[97] Ammonite genera became extinct at or near the K–Pg boundary; however, there was a smaller and slower extinction of ammonite genera prior to the boundary that was associated with a late Cretaceous marine regression. The gradual extinction of most inoceramid bivalves began well before the K–Pg boundary, and a small, gradual reduction in ammonite diversity occurred throughout the very late Cretaceous.[98] Further analysis shows that several processes were in progress in the late Cretaceous seas and partially overlapped in time, then ended with the abrupt mass extinction.[98]


The scientific consensus is that bolide impact at the K–Pg boundary left tsunami deposits and sediments around the area of the Caribbean Sea and Gulf of Mexico.[99] These deposits have been identified in the La Popa basin in northeastern Mexico,[100] platform carbonates in northeastern Brazil,[101] and Atlantic deep-sea sediments.[102]


The length of time taken for the extinction to occur is a controversial issue, because some theories about the extinction's causes require a rapid extinction over a relatively short period (from a few years to a few thousand years) while others require longer periods. The issue is difficult to resolve because of the Signor–Lipps effect; that is, the fossil record is so incomplete that most extinct species probably died out long after the most recent fossil that has been found.[103] Scientists have also found very few continuous beds of fossil-bearing rock which cover a time range from several million years before the K–Pg extinction to a few million years after it.[22]

Chicxulub asteroid impact[edit]

Artist's impression of an asteroid striking Earth at the end of the Cretaceous

Evidence for impact[edit]

In 1980, a team of researchers consisting of Nobel prize-winning physicist Luis Alvarez, his son geologist Walter Alvarez, and chemists Frank Asaro and Helen Michel discovered that sedimentary layers found all over the world at the Cretaceous–Paleogene boundary contain a concentration of iridium many times greater than normal (30, 160 and 20 times in three sections originally studied). Iridium is extremely rare in Earth's crust because it is a siderophile element, and therefore most of it travelled with the iron as it sank into Earth's core during planetary differentiation. As iridium remains abundant in most asteroids and comets, the Alvarez team suggested that an asteroid struck the Earth at the time of the K–Pg boundary.[4] There were earlier speculations on the possibility of an impact event, but this was the first hard evidence of an impact.[104]


This hypothesis was viewed as radical when first proposed, but additional evidence soon emerged. The boundary clay was found to be full of minute spherules of rock, crystallized from droplets of molten rock formed by the impact.[105] Shocked quartz and other minerals were also identified in the K–Pg boundary.[106][107] Shocked minerals have their internal structure deformed, and are created by intense pressures such as those associated with nuclear blasts or meteorite impacts. The identification of giant tsunami beds along the Gulf Coast and the Caribbean also provided evidence for impact,[108] and suggested that the impact may have occurred nearby—as did the discovery that the K–Pg boundary became thicker in the southern United States, with meter-thick beds of debris occurring in northern New Mexico.[12]

* Impact site
* Impact site
* Impact site
K/T impact site on a contemporary world map (65 mya)[109]
Radar topography reveals the 180 km-wide (112 mi) ring of the Chicxulub Crater.

Further research identified the giant Chicxulub crater, buried under Chicxulub on the coast of Yucatán, Mexico as the source of the K–Pg boundary clay. Identified in 1990[5] based on work by geophysicist Glen Penfield in 1978, the crater is oval, with an average diameter of roughly 180 kilometres (110 mi), about the size calculated by the Alvarez team.[110] The discovery of the crater – a necessary prediction of the impact hypothesis – provided conclusive evidence for a K–Pg impact, and strengthened the hypothesis that the extinction was caused by an impact.

In 2007, a hypothesis was put forth that argued the impactor that killed the dinosaurs belonged to the Baptistina family of asteroids.[111] Concerns have been raised regarding the reputed link, in part because very few solid observational constraints exist of the asteroid or family.[112] Indeed, it was recently discovered that 298 Baptistina does not share the same chemical signature as the source of the K–Pg impact.[113] Although this finding may make the link between the Baptistina family and K–Pg impactor more difficult to substantiate, it does not preclude the possibility.[113] A 2011 WISE study of reflected light from the asteroids of the family estimated the break-up at 80 Ma, giving it insufficient time to shift orbits and impact the Earth by 65 Ma.[114]

Paul Renne of the Berkeley Geochronology Center has reported that the date of the asteroid event is 65.043±0.011 million years ago, based on argon–argon dating. He further posits that the mass extinction occurred within 33,000 years of this date.[2][115]

Effects of impact[edit]

Such an impact would have inhibited photosynthesis by generating a dust cloud that blocked sunlight for a year or less, and by injecting sulfuric acid aerosols into the stratosphere, which would have reduced sunlight reaching the Earth's surface by 10–20%. It would take at least ten years for those aerosols to dissipate, which would account for the extinction of plants and phytoplankton, and of organisms dependent on them (including predatory animals as well as herbivores). Small creatures whose food chains were based on detritus would have a reasonable chance of survival.[82][97] The consequences of reentry of ejecta into Earth's atmosphere would include a brief (hours long) but intense pulse of infrared radiation, killing exposed organisms.[49] Global firestorms likely resulted from the heat pulse and the fall back to Earth of incendiary fragments from the blast. Recent research indicates that the global debris layer deposited by the impact contained enough soot to suggest that the entire terrestrial biosphere had burned.[116] The high O
levels during the late Cretaceous would have supported intense combustion. The level of atmospheric O
plummeted in the early Cenozoic era. If widespread fires occurred, they would have increased the CO

The impact may also have produced acid rain, depending on what type of rock the asteroid struck. However, recent research suggests this effect was relatively minor, lasting for approximately 12 years.[97] The acidity was neutralized by the environment, and the survival of animals vulnerable to acid rain effects (such as frogs) indicate this was not a major contributor to extinction. Impact theories can only explain very rapid extinctions, since the dust clouds and possible sulfuric aerosols would wash out of the atmosphere in a fairly short time—possibly within 10 years.[118]

The shape and location of the crater indicate further causes of devastation in addition to the dust cloud. The asteroid landed in the ocean and would have caused megatsunamis, for which evidence has been found in several locations in the Caribbean and eastern United States—marine sand in locations that were then inland, and vegetation debris and terrestrial rocks in marine sediments dated to the time of the impact. The asteroid landed in a bed of gypsum (calcium sulfate), which would have produced a vast sulfur dioxide aerosol. This would have further reduced the sunlight reaching the Earth's surface and then precipitated as acid rain, killing vegetation, plankton, and organisms that build shells from calcium carbonate (coccolithophores and molluscs). In February 2008, a team of researchers used seismic images of the crater to determine that the impactor landed in deeper water than was previously assumed. They argued that this would have resulted in increased sulfate aerosols in the atmosphere, which could have made the impact deadlier by altering climate and by generating acid rain.[119]

Most paleontologists now agree that an asteroid did hit the Earth at approximately the end of the Cretaceous, but there is an ongoing dispute whether the impact was the sole cause of the extinctions.[35][120] There is evidence that there was an interval of about 300 ka from the impact to the mass extinction.[121] In 1997, paleontologist Sankar Chatterjee drew attention to the proposed and much larger 600 km (370 mi) Shiva crater and the possibility of a multiple-impact scenario.

In March 2010 an international panel of scientists endorsed the asteroid hypothesis, specifically the Chicxulub impact, as being the cause of the extinction. A team of 41 scientists reviewed 20 years of scientific literature and in so doing also ruled out other theories such as massive volcanism. They had determined that a 10-to-15-kilometre (6.2 to 9.3 mi) space rock hurtled into Earth at Chicxulub on Mexico's Yucatán Peninsula. The collision would have released the same energy as 100 teratonnes of TNT (420 ZJ), over a billion times the energy of the bombs dropped on Nagasaki and Hiroshima.[6]

Alternative hypotheses[edit]

The fact that the extinctions occur at the same time as the Chicxulub asteroid impact strongly supports the impact hypothesis of extinction. However, some scientists continue to dispute the role of the Chicxulub impact in driving the extinction, and to suggest that other events may have contributed to the end-Cretaceous mass extinction. In particular, volcanic eruptions, climate change, sea level change, and other impact events have been suggested to play a role in driving the K–Pg extinction.

Deccan Traps[edit]

Before 2000, arguments that the Deccan Traps flood basalts caused the extinction were usually linked to the view that the extinction was gradual, as the flood basalt events were thought to have started around 68 Ma and lasted more than 2 million years. The most recent evidence shows that the traps erupted over a period of 800,000 years spanning the K–Pg boundary, and therefore may be responsible for the extinction and the delayed biotic recovery thereafter.[122]



Multiple impact event[edit]

Several other craters also appear to have been formed about the time of the K–Pg boundary. This suggests the possibility of near simultaneous multiple impacts, perhaps from a fragmented asteroidal object, similar to the Shoemaker–Levy 9 impact with Jupiter. In addition to the 180 km (110 mi) Chicxulub Crater, there is the 24 km (15 mi) Boltysh crater in Ukraine (65.17±0.64 Ma), the 20 km (12 mi) Silverpit crater, a suspected impact crater in the North Sea (62.5±2.5 Ma), and the controversial and much larger 600 km (370 mi) Shiva crater. Any other craters that might have formed in the Tethys Ocean would have been obscured by tectonic events like the relentless northward drift of Africa and India.[125][126][127][128]

Maastrichtian sea-level regression in the north and ingression in the south[edit]

There is clear evidence that sea levels fell in the final stage of the Cretaceous by more than at any other time in the Mesozoic era. In some Maastrichtian stage rock layers from various parts of the world, the later layers are terrestrial; earlier layers represent shorelines and the earliest layers represent seabeds. These layers do not show the tilting and distortion associated with mountain building, therefore, the likeliest explanation is a "regression", that is, a drop in sea level. There is no direct evidence for the cause of the regression, but the explanation currently accepted as most likely is that the mid-ocean ridges became less active and therefore sank under their own weight.[22][129]



An interesting aspect, very poorly studied up to now, is that in coincidence with the regression in the northern hemisphere, southern continents experienced a massive marine ingression, the first related to the Atlantic Ocean, that formed at least three vast epeiric seas in South America. One of them, over the Austral Basin, flooded southernmost Patagonia. Another one flooded Central Patagonia, reaching the Andes foothills, and the northernmost, entering across central Argentina (Buenos Aires Province) flooded the center of the country and reached southern Bolivia in the Potosi Basin.

Multiple causes[edit]

In a review article, J. David Archibald and David E. Fastovsky discussed a scenario combining three major postulated causes: volcanism, marine regression, and extraterrestrial impact. In this scenario, terrestrial and marine communities were stressed by the changes in and loss of habitats. Dinosaurs, as the largest vertebrates, were the first affected by environmental changes, and their diversity declined. At the same time, particulate materials from volcanism cooled and dried areas of the globe. Then, an impact event occurred, causing collapses in photosynthesis-based food chains, both in the already-stressed terrestrial food chains and in the marine food chains. The major difference between this hypothesis and the single-cause hypotheses is that its proponents view the suggested single causes as either not sufficient in strength to cause the extinctions or not likely to produce the taxonomic pattern of the extinction.[81]

Recovery and radiation[edit]

The K–Pg extinction had a profound effect on the evolution of life on earth. The elimination of dominant Cretaceous groups allowed other organisms to take their place, spurring a remarkable series of adaptive radiations in the Paleogene.[15] The most striking example is the replacement of dinosaurs by mammals. After the K–Pg extinction, mammals evolved rapidly to fill the niches left vacant by the dinosaurs. Within mammalian genera, new species were approximately 9.1% larger after the K–Pg boundary.[130]

Other groups also underwent major radiations. Based on molecular sequencing and fossil dating, Neoaves appeared to radiate after the K–Pg boundary.[16][131] They even produced giant, flightless forms, such as the herbivorous Gastornis and Dromornithidae, and the predatory Phorusrhacidae. The extinction of Cretaceous lizards and snakes may have led to the radiation of modern groups such as iguanas, monitor lizards, and boas.[9] On land, giant boid and enormous madtsoiid snakes appeared, and in the seas, giant sea snakes radiated. Teleost fish diversified explosively,[17] filling the niches left vacant by the extinction. Groups appearing in the Paleocene and Eocene include billfish, tunas, eels, and flatfish. Major changes are also seen in Paleogene insect communities. Many groups of ants were present in the Cretaceous, but in the Eocene ants became dominant and diverse, with larger colonies. Butterflies diversified as well, perhaps to take the place of leaf-eating insects wiped out by the extinction. The advanced mound-building termites, Termitidae, also rose to prominence.[132]

See also[edit]

References and notes[edit]

  2. ^ a b Renne, Paul R.; Deino, Alan L.; Hilgen, Frederik J.; Kuiper, Klaudia F.; Mark, Darren F.; Mitchell III, William S.; Morgan, Leah E.; Mundil, Roland; Smit, Jan (7 February 2013). "Time Scales of Critical Events Around the Cretaceous-Paleogene Boundary". Science 339 (6120): 684–687. Bibcode:2013Sci...339..684R. doi:10.1126/science.1230492. 
  4. ^ a b Alvarez LW, Alvarez W, Asaro F, Michel HV (1980). "Extraterrestrial cause for the Cretaceous–Tertiary extinction". Science 208 (4448): 1095–1108. Bibcode:1980Sci...208.1095A. doi:10.1126/science.208.4448.1095. PMID 17783054. 
  5. ^ a b Hildebrand, A. R., G. T. Penfield, et al. (1991). "Chicxulub crater: a possible Cretaceous/Tertiary boundary impact crater on the Yucatán peninsula, Mexico." Geology 19: 867-871.
  7. ^ Keller, G. (2012). The Cretaceous--Tertiary Mass Extinction, Chicxulub Impact, and Deccan Volcanism. Earth and Life, Springer: 759--793.
  8. ^ Longrich N. R., Tokaryk T. T. et al. (2011). "Mass extinction of birds at the Cretaceous-Paleogene (K–Pg) boundary". Proceedings of the National Academy of Sciences 108 (37): 15253–15257. 
  9. ^ a b c Longrich, N. R., A.-B. S. Bhullar, et al. (2012). "Mass extinction of lizards and snakes at the Cretaceous-Paleogene boundary." Proceedings of the National Academy of Sciences doi:10.1073/pnas.1211526110
  10. ^ Labandeira, C. C., K. R. Johnson, et al. (2002). "Preliminary assessment of insect herbivory across the Cretaceous-Tertiary boundary: major extinction and minimum rebound." Geological Society of America Special Paper 361: 297-327.
  11. ^ Rehan, Sandra M.; Leys, Remko; Schwarz, Michael P. (2013). "First Evidence for a Massive Extinction Event Affecting Bees Close to the K-T Boundary". PLoS ONE 8 (10): e76683. doi:10.1371/journal.pone.0076683. ISSN 1932-6203. 
  12. ^ a b c d e f g Nichols, D. J. and K. R. Johnson (2008). Plants and the K–T Boundary. Cambridge, Cambridge University Press.
  13. ^ Friedman M (2009). "Ecomorphological selectivity among marine teleost fishes during the end-Cretaceous extinction". PNAS 106: 5218–5223. 
  14. ^ Jablonski, D., 1994. Extinctions in the fossil record (and discussion). Philosophical Transactions of the Royal Society of London, Series B. 344, 11-17.
  15. ^ a b Alroy J (1999). "The fossil record of North American Mammals: evidence for a Palaeocene evolutionary radiation". Systematic Biology 48 (1): 107–118. 
  16. ^ a b Feduccia A (1995). "Explosive evolution in Tertiary birds and mammals". Science 267: 637–638. 
  17. ^ a b Friedman M (2010). "Explosive morphological diversification of spiny-finned teleost fishes in the aftermath of the end-Cretaceous extinction". Proceedings of the Royal Society B 277: 1675–1683. 
  18. ^ Jablonski, D. (1994). "Extinctions in the fossil record (and discussion)." Philosophical Transactions of the Royal Society of London, Series B. 344(1307) 11-17.
  19. ^ Weishampel, D. B., P. M. Barrett, et al. (2004). Dinosaur Distribution. The Dinosauria. D. B. Weishampel, P. Dodson and H. Osmolska. Berkeley, University of California Press: 517-606.
  20. ^ a b Wilf P, Johnson KR (2004). "Land plant extinction at the end of the Cretaceous: a quantitative analysis of the North Dakota megafloral record". Paleobiology 30 (3): 347–368. doi:10.1666/0094-8373(2004)030<0347:LPEATE>2.0.CO;2. ISSN 0094-8373. 
  21. ^ Kauffman E (2004). "Mosasaur Predation on Upper Cretaceous Nautiloids and Ammonites from the United States Pacific Coast". PALAIOS (Society for Sedimentary Geology) 19 (1): 96–100. doi:10.1669/0883-1351(2004)019<0096:MPOUCN>2.0.CO;2. ISSN 0883-1351. Retrieved 2007-06-17. 
  24. ^ Aberhan M, Weidemeyer S, Kieesling W, Scasso RA, Medina FA (2007). "Faunal evidence for reduced productivity and uncoordinated recovery in Southern Hemisphere Cretaceous-Paleogene boundary sections". Geology 35 (3): 227–230. Bibcode:2007Geo....35..227A. doi:10.1130/G23197A.1. 
  25. ^ Sheehan Peter M, Fastovsky DE (1992). "Major extinctions of land-dwelling vertebrates at the Cretaceous–Tertiary boundary, eastern Montana". Geology 20 (6): 556–560. Bibcode:1992Geo....20..556S. doi:10.1130/0091-7613(1992)020<0556:MEOLDV>2.3.CO;2. Retrieved 2007-06-22. 
  26. ^ Pospichal JJ (1996). "Calcareous nannofossils and clastic sediments at the Cretaceous–Tertiary boundary, northeastern Mexico". Geology 24 (3): 255–258. Bibcode:1996Geo....24..255P. doi:10.1130/0091-7613(1996)024<0255:CNACSA>2.3.CO;2. 
  27. ^ Bown P (2005). "Selective calcareous nannoplankton survivorship at the Cretaceous–Tertiary boundary". Geology 33 (8): 653–656. Bibcode:2005Geo....33..653B. doi:10.1130/G21566.1. 
  28. ^ Bambach RK, Knoll AH, Wang SC (2004). "Origination, extinction, and mass depletions of marine diversity". Paleobiology 30 (4): 522–542. doi:10.1666/0094-8373(2004)030<0522:OEAMDO>2.0.CO;2. ISSN 0094-8373. 
  29. ^ Gedl P (2004). "Dinoflagellate cyst record of the deep-sea Cretaceous-Tertiary boundary at Uzgru, Carpathian Mountains, Czech Republic". Geological Society, London, Special Publications 230: 257–273. Bibcode:2004GSLSP.230..257G. doi:10.1144/GSL.SP.2004.230.01.13. 
  30. ^ MacLeod N (1998). "Impacts and marine invertebrate extinctions". Geological Society, London, Special Publications 140 (1): 217–246. Bibcode:1998GSLSP.140..217M. doi:10.1144/GSL.SP.1998.140.01.16. 
  31. ^ Courtillot, V (1999). Evolutionary Catastrophes: The Science of Mass Extinction. Cambridge University Press. p. 2. ISBN 0-521-58392-6. 
  32. ^ Glaessner MF (1937). "Studien über Foraminiferen aus der Kreide und dem Tertiär des Kaukasus: die Foraminiferen der ältesten Tertiärschichten des Nordwestkaukasus". Проблемс оф палеонтологий - Problems of Paleontology (in German) 2–3: 349–410. OCLC 776158910. 
  33. ^ Arenillas I, Arz JA, Molina E and Dupuis C (2000). "An independent test of planktic foraminiferal turnover across the Cretaceous/Paleogene (K/P) boundary at El Kef, Tunisia: catastrophic mass extinction and possible survivorship". Micropaleontology 46 (1): 31–49. JSTOR 1486024. 
  34. ^ MacLeod, N (1996). Nature of the Cretaceous-Tertiary (K–T) planktonic foraminiferal record: stratigraphic confidence intervals, Signor–Lipps effect, and patterns of survivorship. In: Cretaceous–Tertiary Mass Extinctions: Biotic and Environmental Changes (MacLeod N, Keller G, editors). WW Norton. pp. 85–138. ISBN 978-0-393-96657-2. 
  35. ^ a b Keller G, Adatte T, Stinnesbeck W, Rebolledo-Vieyra, Fucugauchi JU, Kramar U, Stüben D (2004). "Chicxulub impact predates the K–T boundary mass extinction". PNAS 101 (11): 3753–3758. Bibcode:2004PNAS..101.3753K. doi:10.1073/pnas.0400396101. PMC 374316. PMID 15004276. 
  36. ^ Galeotti S, Bellagamba M, Kaminski MA, and Montanari A (2002). "Deep-sea benthic foraminiferal recolonisation following a volcaniclastic event in the lower Campanian of the Scaglia Rossa Formation (Umbria-Marche Basin, central Italy)" (PDF). Marine Micropaleontology 44: 57–76. Retrieved 2007-08-19. 
  37. ^ Kuhnt W, Collins ES (1996). "8. Cretaceous to Paleogene benthic foraminifers from the Iberia abyssal plain" (PDF). Proceedings of the Ocean Drilling Program, Scientific Results 149: 203–216. Retrieved 2007-08-19. 
  38. ^ Coles, GP; Ayress MA, and Whatley RC (1990). "A comparison of North Atlantic and 20 Pacific deep-sea Ostracoda". In RC Whatley and C Maybury. Ostracoda and global events. Chapman & Hall. pp. 287–305. ISBN 978-0-442-31167-4. 
  39. ^ Brouwers EM, De Deckker P (1993). "Late Maastrichtian and Danian Ostracode Faunas from Northern Alaska: Reconstructions of Environment and Paleogeography". Palaios 8 (2): 140–154. doi:10.2307/3515168. JSTOR 3515168. 
  40. ^ Vescsei A, Moussavian E (1997). "Paleocene reefs on the Maiella Platform Margin, Italy: An example of the effects of the cretaceous/tertiary boundary events on reefs and carbonate platforms". Facies 36 (1): 123–139. doi:10.1007/BF02536880. 
  41. ^ Rosen BR, Turnšek D (1989). Extinction patterns and biogeography of scleractinian corals across the Cretaceous/Tertiary boundary. In Jell A; Pickett JW. "Proceedings of the Fifth International Symposium on Fossil Cnidaria including Archaeocyatha and Spongiomorphs". Memoir of the Association of Australasian Paleontology (Brisbane, Queensland) (8): 355–370. 
  42. ^ Ward PD, Kennedy WJ, MacLeod KG, Mount JF (1991). "Ammonite and inoceramid bivalve extinction patterns in Cretaceous/Tertiary boundary sections of the Biscay region (southwestern France, northern Spain)". Geology 19 (12): 1181–1184. Bibcode:1991Geo....19.1181W. doi:10.1130/0091-7613(1991)019<1181:AAIBEP>2.3.CO;2. 
  43. ^ Harries PJ, Johnson KR, Cobban WA, Nichols DJ (2002). "Marine Cretaceous-Tertiary boundary section in southwestern South Dakota: Comment and Reply". Geology 30 (10): 954–955. Bibcode:2002Geo....30..954H. doi:10.1130/0091-7613(2002)030<0955:MCTBSI>2.0.CO;2. ISSN 0091-7613. 
  44. ^ Neraudeau D, Thierry J, Moreau P (1997). "Variation in echinoid biodiversity during the Cenomanian–early Turonian transgressive episode in Charentes (France)". Bulletin de la Société Géologique de France 168: 51–61. 
  46. ^ MacLeod KG (1994). "Extinction of Inoceramid Bivalves in Maastrichtian Strata of the Bay of Biscay Region of France and Spain". Journal of Paleontology 68 (5): 1048–1066. 
  50. ^ a b Labandeira Conrad C, Johnson Kirk R, Wilf Peter (2002). "Impact of the terminal Cretaceous event on plant–insect associations" (PDF). Proceedings of the National Academy of Sciences of the United States of America 99 (4): 2061–2066. Bibcode:2002PNAS...99.2061L. doi:10.1073/pnas.042492999. PMC 122319. PMID 11854501. 
  51. ^ Wilf P, Labandeira CC, Johnson KR, Ellis B (2006). "Decoupled Plant and Insect Diversity After the End-Cretaceous Extinction". Science 313 (5790): 1112–1115. Bibcode:2006Sci...313.1112W. doi:10.1126/science.1129569. PMID 16931760. 
  52. ^ a b Vajda Vivi, Raine J Ian, Hollis Christopher J (2001). "Indication of Global Deforestation at the Cretaceous–Tertiary Boundary by New Zealand Fern Spike". Science 294 (5547): 1700–1702. Bibcode:2001Sci...294.1700V. doi:10.1126/science.1064706. PMID 11721051. 
  53. ^ Wilf P., Johnson K. R. (2004). "Land plant extinction at the end of the Cretaceous: a quantitative analysis of the North Dakota megafloral record". Paleobiology 30 (3): 347–368. 
  54. ^ Johnson, KR; Hickey LJ (1991). Megafloral change across the Cretaceous Tertiary boundary in the northern Great Plains and Rocky Mountains. In: Global Catastrophes in Earth History: An Interdisciplinary Conference on Impacts, Volcanism, and Mass Mortality, Sharpton VI and Ward PD (editors). Geological Society of America. ISBN 978-0-8137-2247-4. 
  55. ^ Askin, RA; Jacobson SR (1996). Palynological change across the Cretaceous–Tertiary boundary on Seymour Island, Antarctica: environmental and depositional factors. In: Cretaceous–Tertiary Mass Extinctions: Biotic and Environmental Changes, Keller G, MacLeod N (editors). WW Norton. ISBN 978-0-393-96657-2. 
  56. ^ Schultz PH, D'Hondt S (1996). "Cretaceous–Tertiary (Chicxulub) impact angle and its consequences". Geology 24 (11): 963–967. Bibcode:1996Geo....24..963S. doi:10.1130/0091-7613(1996)024<0963:CTCIAA>2.3.CO;2. Retrieved 2007-07-05. 
  57. ^ Vajda V, McLoughlin S (2004). "Fungal Proliferation at the Cretaceous–Tertiary Boundary" (PDF). Science 303 (5663): 1489–1490. doi:10.1126/science.1093807. PMID 15001770. Retrieved 2007-07-07. 
  58. ^ Fawcett, J. A.; Maere, S.; Van de Peer, Y. (April 2009). "Plants with double genomes might have had a better chance to survive the Cretaceous–Tertiary extinction event". Proceedings of the National Academy of Sciences of the United States of America 106 (14): 5737–5742. Bibcode:2009PNAS..106.5737F. doi:10.1073/pnas.0900906106. ISSN 0027-8424. PMC 2667025. PMID 19325131.  edit
  59. ^ Archibald JD, Bryant LJ (1990). "Differential Cretaceous–Tertiary extinction of nonmarine vertebrates; evidence from northeastern Montana. In: Global Catastrophes in Earth History: an Interdisciplinary Conference on Impacts, Volcanism, and Mass Mortality (Sharpton VL and Ward PD, editors)". Geological Society of America, Special Paper 247: 549–562. 
  60. ^ Estes, R. (1964). "Fossil vertebrates from the Late Cretaceous Lance Formation, Eastern Wyoming." University of California Publications, Department of Geological Sciences 49: 1-180.
  61. ^ Gardner J. D. (2000). "Albanerpetontid amphibians from the Upper Cretaceous (Campanian and Maastrichtian) of North America". Geodiversitas 22 (3): 349–388. 
  62. ^ Sheehan P. M., Fastovsky D. E. (1992). "Major extinctions of land-dwelling vertebrates at the Cretaceous-Tertiary boundary, Eastern Montana". Geology 20: 556–560. 
  63. ^ a b Novacek MJ (1999). "100 Million Years of Land Vertebrate Evolution: The Cretaceous-Early Tertiary Transition". Annals of the Missouri Botanical Garden 86 (2): 230–258. doi:10.2307/2666178. JSTOR 2666178. 
  64. ^ Lutz, D (2005). Tuatara: A Living Fossil. DIMI Press. ISBN 0-931625-43-2. 
  65. ^ Chatterjee S, Small BJ (1989). "New plesiosaurs from the Upper Cretaceous of Antarctica". Geological Society, London, Special Publications 47 (1): 197–215. Bibcode:1989GSLSP..47..197C. doi:10.1144/GSL.SP.1989.047.01.15. Retrieved 2007-07-04. 
  66. ^ O'Keefe FR (2001). "A cladistic analysis and taxonomic revision of the Plesiosauria (Reptilia: Sauropterygia)". Acta Zoologica Fennica 213: 1–63. 
  67. ^ Brochu CA (2004). "Calibration age and quartet divergence date estimation". Evolution 58 (6): 1375–1382. doi:10.1554/03-509. PMID 15266985. 
  68. ^ Jouve S, Bardet, N, Jalil N-E, Suberbiola XP, Bouya B, Amaghzaz M (2008). "The oldest African crocodylian: phylogeny, paleobiogeography, and differential survivorship of marine reptiles through the Cretaceous-Tertiary Boundary". Journal of Vertebrate Paleontology 28 (2): 409–421. doi:10.1671/0272-4634(2008)28[409:TOACPP]2.0.CO;2. ISSN 0272-4634. 
  70. ^ Agnolin, F. L. (2012), "Systematic reinterpretation of Piksi barbarulna Varricchio, 2002 from Two Medicine Formation (Upper Cretaceous) of Western USA (Montana) as a pterosaur rather than a bird))", Varricchio, D. (Muséum national d'histoire naturelle, Paris): 891&892, doi:10.5252/g2012n4a10, retrieved December 31, 2012 
  71. ^ Slack KE, Jones CM, Ando T, Harrison GL, Fordyce RE, Arnason U, Penny D (2006). "Early Penguin Fossils, Plus Mitochondrial Genomes, Calibrate Avian Evolution". Molecular Biology and Evolution 23 (6): 1144–1155. doi:10.1093/molbev/msj124. PMID 16533822. 
  72. ^ Penny D, Phillips MJ (2004). "The rise of birds and mammals: are microevolutionary processes sufficient for macroevolution". Trends Ecol Evol 19 (10): 516–522. doi:10.1016/j.tree.2004.07.015. PMID 16701316. 
  73. ^ Slack et al. (2006) 
  74. ^ Butler, Barret, Nowbath, Upchurch (2009) 
  75. ^ Dyke et al. (2009) 
  76. ^ Pterosaurs: Natural History, Evolution, Anatomy, Mark P. Wilton (2013) 
  77. ^ Hou L, Martin M, Zhou Z, Feduccia A (1996). "Early Adaptive Radiation of Birds: Evidence from Fossils from Northeastern China". Science 274 (5290): 1164–1167. Bibcode:1996Sci...274.1164H. doi:10.1126/science.274.5290.1164. PMID 8895459. 
  78. ^ Clarke JA, Tambussi CP, Noriega JI, Erickson GM, Ketcham RA (2005). "Definitive fossil evidence for the extant avian radiation in the Cretaceous". Nature 433 (7023): 305–308. Bibcode:2005Natur.433..305C. doi:10.1038/nature03150. PMID 15662422. 
  79. ^ a b c Longrich, Nicholas R.; Tokaryk, Tim; Field, Daniel J. (2011). "Mass extinction of birds at the Cretaceous–Paleogene (K–Pg) boundary.". Proceedings of the National Academy of Sciences 108 (37): 15253–15257. Bibcode:2011PNAS..10815253L. doi:10.1073/pnas.1110395108. 
  80. ^ "Primitive Birds Shared Dinosaurs' Fate". Science Daily. 20 September 2011. Retrieved 20 September 2011. 
  81. ^ a b c d e David, Archibald; David Fastovsky (2004). "Dinosaur Extinction". In Weishampel David B, Dodson Peter, Osmólska Halszka (eds.). The Dinosauria (2nd ed.). Berkeley: University of California Press. pp. 672–684. ISBN 0-520-24209-2. 
  82. ^ a b Ocampo, A; Vajda V, Buffetaut E (2006). "Unravelling the Cretaceous–Paleogene (K–T) turnover, evidence from flora, fauna and geology in biological processes associated with impact events". In Cockell C, Gilmour I, Koeberl C. Biological Processes Associated with Impact Events. SpringerLink. pp. 197–219. ISBN 978-3-540-25735-6. 
  83. ^ Rieraa V, Marmib J, Omsa O, Gomez B (March 2010). "Orientated plant fragments revealing tidal palaeocurrents in the Fumanya mudflat (Maastrichtian, southern Pyrenees): Insights in palaeogeographic reconstructions". Palaeogeography, Palaeoclimatology, Palaeoecology 288 (1–4): 82–92. doi:10.1016/j.palaeo.2010.01.037. 
  84. ^ Loeuff Le, J. (2012) Paleobiogeography and biodiversity of Late Maastrichtian dinosaurs: how many dinosaur species went extinct at the Cretaceous-Tertiary boundary? Bulletin de la Société Géologique de France 183(6) 547-559 doi:10.2113/gssgfbull.183.6.547
  85. ^ Ryan MJ, Russell AP, Eberth DA, Currie PJ (2001). "The taphonomy of a Centrosaurus (Ornithischia: Ceratopsidae) bone bed from the Dinosaur Park Formation (Upper Campanian), Alberta, Canada, with comments on cranial ontogeny". PALAIOS 16: 482–506. 
  89. ^ Gelfo JN and Pascual R (2001). "Peligrotherium tropicalis (Mammalia, Dryolestida) from the early Paleocene of Patagonia, a survival from a Mesozoic Gondwanan radiation". Geodiversitas 23: 369–379. 
  90. ^ Goin FJ, Reguero MA, Pascual R, von Koenigswald W, Woodburne MO, Case JA, Marenssi SA, Vieytes C, Vizcaíno SF (2006). "First gondwanatherian mammal from Antarctica". Geological Society, London, Special Publications 258: 135–144. Bibcode:2006GSLSP.258..135G. doi:10.1144/GSL.SP.2006.258.01.10. 
  91. ^ McKenna, MC; Bell SK (1997). Classification of mammals: above the species level. Columbia University Press. ISBN 978-0-231-11012-9. 
  92. ^ a b Bininda-Emonds ORP, Cardillo M, Jones KE, MacPhee RDE, Beck RMD, Grenyer R, Price SA, Vos RA, Gittleman JLY, Purvis A (2007). "The delayed rise of present-day mammals" (PDF). Nature 446 (7135): 507–512. Bibcode:2007Natur.446..507B. doi:10.1038/nature05634. PMID 17392779. 
  93. ^ a b Springer MS, Murphy WJ, Eizirik E, O'Brien SJ (2003). "Placental mammal diversification and the Cretaceous–Tertiary boundary" (PDF). PNAS 100 (3): 1056–1061. Bibcode:2003PNAS..100.1056S. doi:10.1073/pnas.0334222100. PMC 298725. PMID 12552136. 
  94. ^ Dodson, Peter (1996). The Horned Dinosaurs: A Natural History. Princeton: Princeton University Press. pp. 279–281. ISBN 0-691-05900-4. 
  95. ^ "Online guide to the continental Cretaceous–Tertiary boundary in the Raton basin, Colorado and New Mexico". U.S. Geological Survey. 2004. Retrieved 2007-07-08. 
  96. ^ Smathers, GA; Mueller-Dombois D (1974). Invasion and Recovery of Vegetation after a Volcanic Eruption in Hawaii, Scientific Monograph Number 5. United States National Park Service. Retrieved 2007-07-09. 
  97. ^ a b c Pope KO, D'Hondt SL, Marshall CR (1998). "Meteorite impact and the mass extinction of species at the Cretaceous/Tertiary boundary". PNAS 95 (19): 11028–11029. Bibcode:1998PNAS...9511028P. doi:10.1073/pnas.95.19.11028. PMC 33889. PMID 9736679. 
  99. ^ Bourgeois J (2009). "Chapter 3. GEOLOGIC EFFECTS AND RECORDS OF TSUNAMIS" (pdf). In Robinson, A.R. and Bernard, E.N. The Sea, Volume 15: Tsunamis (Sea: Ideas and Observations on Progress in the Study of the Seas). Boston: Harvard University. ISBN 978-0-674-03173-9. Retrieved 2012-03-29. 
  100. ^ Lawton, T. F., K. W. Shipley, J. L. Aschoff, K. A. Giles and F. J.Vega (2005). "Basinward transport of Chicxulub ejecta by tsunami-induced backflow, La Popa basin, northeastern Mexico, and its implications for distribution of impact-related deposits flanking the Gulf of Mexico". Geology 33 (2): 81–84. Bibcode:2005Geo....33...81L. doi:10.1130/G21057.1. Retrieved 2012-03-29. 
  101. ^ Albertão, G. A. and P. P. Martins Jr. (1996). "A possible tsunami deposit at the Cretaceous-Tertiary boundary in Pernambuco, northeastern Brazil". Sed. Geol. 104: 189–201. Bibcode:1996SedG..104..189A. doi:10.1016/0037-0738(95)00128-X. 
  102. ^ Norris, R. D., J. Firth, J. S. Blusztajn and G. Ravizza (2000). "Mass failure of the North Atlantic margin triggered by the Cretaceous-Paleogene bolide impact". Geology 28 (12): 1119–1122. Bibcode:2000Geo....28.1119N. doi:10.1130/0091-7613(2000)28<1119:MFOTNA>2.0.CO;2. Retrieved 2012-03-29. 
  103. ^ Signor III, PW; Lipps, JH (1982). "Sampling bias, gradual extinction patterns, and catastrophes in the fossil record.". In Silver LT; Schultz PH (editors). Geological implications of impacts of large asteroids and comets on the Earth. Special Publication 190. Boulder, Colorado: Geological Society of America. pp. 291–296. OCLC 4434434112. 
  104. ^ De Laubenfels MW (1956). "Dinosaur extinction: One more hypothesis". Journal of Paleontology 30 (1): 207–218. JSTOR 1300393. 
  105. ^ Smit J., Klaver J. (1981). "Sanidine spherules at the Cretaceous-Tertiary boundary indicate a large impact event". Nature 292: 47–49. 
  106. ^ Bohor B. F., Foord E. E. et al. (1984). "Mineralogic evidence for an impact event at the Cretaceous-Tertiary boundary". Science 867: 869. 
  107. ^ Bohor B. F., Modreski P. J. et al. (1987). "Shocked Quartz in the Cretaceous-Tertiary Boundary Clays: Evidence for a Global Distribution". Science 236 (4802): 705–709. 
  108. ^ Bourgeois J., Hansen T. A. et al. (1988). "A tsunami deposit at the Cretaceous-Tertiary boundary in Texas". Science 241 (4865): 567–570. 
  109. ^ K/T extinction
  111. ^ Bottke WF, Vokrouhlický D, Nesvorný D (September 2007). "An asteroid breakup 160 Myr ago as the probable source of the K/T impactor". Nature 449 (7158): 48–53. Bibcode:2007Natur.449...48B. doi:10.1038/nature06070. PMID 17805288. 
  112. ^ Majaess DJ, Higgins D, Molnar LA, Haegert MJ, Lane DJ, Turner DG, Nielsen I (February 2009). "New Constraints on the Asteroid 298 Baptistina, the Alleged Family Member of the K/T Impactor". The Journal of the Royal Astronomical Society of Canada 103 (1): 7–10. arXiv:0811.0171. Bibcode:2009JRASC.103....7M. 
  113. ^ a b Reddy V, Emery JP, Gaffey, MJ, Bottke, WF, Cramer A, Kelley MS (December 2009). "Composition of 298 Baptistina: Implications for the K/T impactor link". Meteoritics & Planetary Science 44 (12): 1917–1927. Bibcode:2009M&PS...44.1917R. doi:10.1111/j.1945-5100.2009.tb02001.x. 
  114. ^ "NASA's WISE Raises Doubt About Asteroid Family Believed Responsible for Dinosaur Extinction". ScienceDaily. 20 September 2011. Retrieved 21 September 2011. 
  115. ^ David Perlman, "Dinosaur extinction battle flares," accessed 2013-02-08
  116. ^ Robertson, D.S., Lewis, W.M., Sheehan, P.M. & Toon, O.B. (2013) K/Pg Extinction: Re-evaluation of the Heat/Fire Hypothesis.Journal of Geophysical Research: Biogeosciences
  117. ^ Pope KO, Baines KH, Ocampo AC, Ivanov BA (1997). "Energy, volatile production, and climatic effects of the Chicxulub Cretaceous/Tertiary impact". Journal of Geophysical Research 102 (E9): 21645–21664. Bibcode:1997JGR...10221645P. doi:10.1029/97JE01743. PMID 11541145. 
  119. ^ Gulick; Barton, Penny J.; Christeson, Gail L.; Morgan, Joanna V.; McDonald, Matthew; Mendoza-Cervantes, Keren; Pearson, Zulmacristina F.; Surendra, Anusha et al. (13 January 2008). "Importance of pre-impact crustal structure for the asymmetry of the Chicxulub impact crater". Nature Geoscience 1 (2): 131–135. Bibcode:2008NatGe...1..131G. doi:10.1038/ngeo103. 
  121. ^ Keller G, Abramovich S, Berner Z, Adatte T (1 January 2009). "Biotic effects of the Chicxulub impact, K–Pg catastrophe and sea level change in Texas". Palaeogeography, Palaeoclimatology, Palaeoecology 271 (1–2): 52–68. doi:10.1016/j.palaeo.2008.09.007. 
  125. ^ Mullen L (October 13, 2004). "Debating the Dinosaur Extinction". Astrobiology Magazine. Retrieved 2012-03-29. 
  126. ^ Mullen L (October 20, 2004). "Multiple impacts". Astrobiology Magazine. Retrieved 2012-03-29. 
  127. ^ Mullen L (November 3, 2004). "Shiva: Another K–T impact?". Astrobiology Magazine. Retrieved 2012-03-29. 
  128. ^ Chatterjee, Sankar (August 1997). "Multiple Impacts at the KT Boundary and the Death of the Dinosaurs". 30th International Geological Congress 26. pp. 31–54. ISBN 978-90-6764-254-5. Retrieved 2008-02-22. 
  130. ^ Alroy J (May 1998). "Cope's rule and the dynamics of body mass evolution in North American fossil mammals". Science 280 (5364): 731–4. Bibcode:1998Sci...280..731A. doi:10.1126/science.280.5364.731. PMID 9563948. 
  131. ^ Ericson PG, Anderson CL, Britton T, et al. (December 2006). "Diversification of Neoaves: integration of molecular sequence data and fossils". Biol. Lett. 2 (4): 543–7. doi:10.1098/rsbl.2006.0523. PMC 1834003. PMID 17148284. Retrieved 2013-01-17. 
  132. ^ Grimaldi, David A. (2007). Evolution of the Insects. Cambridge Univ Pr (E). ISBN 0-511-12388-4. 

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