Cretaceous–Tertiary extinction event

Artist's rendering of bolide impact
Badlands near Drumheller, Alberta, where erosion has exposed the K–T boundary
A Wyoming (US) 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

The Cretaceous–Tertiary extinction event, which occurred approximately 65.5 million years ago (Ma), was a large-scale mass extinction of animal and plant species in a geologically short period of time. Widely known as the K–T extinction event, it is associated with a geological signature known as the K–T boundary, usually a thin band of sedimentation found in various parts of the world. K is the traditional abbreviation for the Cretaceous Period derived from the German name Kreidezeit, and T is the abbreviation for the Tertiary Period (a historical term for the period of time now covered by the Paleogene and Neogene periods). The event marks the end of the Mesozoic Era and the beginning of the Cenozoic Era.[1] With "Tertiary" being discouraged as a formal time or rock unit by the International Commission on Stratigraphy, the K–T event is now called the Cretaceous–Paleogene (or K–Pg) extinction event by many researchers.[2]

Non-avian dinosaur fossils are found only below the K–T boundary, indicating that non-avian dinosaurs became extinct immediately before, or during the event.[3] A very small number of dinosaur fossils have been found above the K–T boundary, but they have been explained as reworked, that is, fossils that have been eroded from their original locations then preserved in later sedimentary layers.[4][5][6] Mosasaurs, plesiosaurs, pterosaurs and many species of plants and invertebrates also became extinct. Mammalian and bird clades passed through the boundary with few extinctions, and evolutionary radiation from those Maastrichtian clades occurred well past the boundary. Rates of extinction and radiation varied across different clades of organisms.[7]

Scientists theorize that the K–T extinctions were caused by one or more catastrophic events, such as massive asteroid impacts (like the Chicxulub impact), or increased volcanic activity. Several impact craters and massive volcanic activity, such as that in the Deccan traps, have been dated to the approximate time of the extinction event. These geological events may have reduced sunlight and hindered photosynthesis, leading to a massive disruption in Earth's ecology. Other researchers believe the extinction was more gradual, resulting from slower changes in sea level or climate.[7] On March 4, 2010, a panel of 41 scientists agreed that the Chicxulub asteroid impact triggered the mass extinction.[8][9]

Contents

Extinction patterns

Extinction intensity.svg Cambrian Ordovician Silurian Devonian Carboniferous Permian Triassic Jurassic Cretaceous Paleogene Neogene
K–T
Tr–J
Late D
O–S
Millions of years ago
Extinction intensity.svg Cambrian Ordovician Silurian Devonian Carboniferous Permian Triassic Jurassic Cretaceous Paleogene Neogene
Marine extinction intensity through time. The blue graph shows the apparent percentage (not the absolute number) of marine animal genera becoming extinct during any given time interval. It does not represent all marine species, just those that are readily fossilized. The labels of the "Big Five" extinction events are clickable hyperlinks; see Extinction event for more details. (source and image info)

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.[10] 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 on which they depended 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.[11]

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 seem 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).[7][12][13]

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.[14] 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.[7]

The largest air-breathing survivors of the event, crocodilians and champsosaurs, were semi-aquatic and had access to detritus. Modern crocodilians can live as scavengers and can survive for months without food, and their young are small, grow slowly, and feed largely on invertebrates and dead organisms or fragments of organisms for their first few years. These characteristics have been linked to crocodilian survival at the end of the Cretaceous.[12]

After the K–T event, biodiversity required substantial time to recover, despite the existence of abundant vacant ecological niches.[7]

Microbiota

The K–T 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.[15][16] 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.[17] The K–T 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.[7] Recent studies indicate that there were no major shifts in dinoflagellates through the boundary layer.[18]

Radiolaria have left a geological record since at least the Ordovician times, and their mineral fossil skeletons can be tracked across the K–T 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.[7] 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–T boundary.[7][19]

The occurrence of planktonic foraminifera across the K–T boundary has been studied since the 1930s.[20][21] Research spurred by the possibility of an impact event at the K–T boundary resulted in numerous publications detailing planktonic foraminiferal extinction at the boundary.[7] However, there is debate ongoing between groups that believe the evidence indicates substantial extinction of these species at the K–T boundary,[22] and those who believe the evidence supports multiple extinctions and expansions through the boundary.[23][24]

Numerous species of benthic foraminifera became extinct during the K–T 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.[7] 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.[25][26]

Marine invertebrates

An ammonite fossil

There is variability in the fossil record as to the extinction rate of marine invertebrates across the K–T boundary. The apparent rate is influenced by the lack of fossil records rather than actual extinction.[7]

Ostracodes, 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 Tertiary. However, current research cannot ascertain whether the extinctions occurred prior to or during the boundary interval itself.[27][28]

Approximately 60% of late-Cretaceous Scleractinia coral genera failed to cross the K–T boundary into the Paleocene. Further analysis of the coral extinctions shows that approximately 98% of colonial species, ones that inhabit warm, shallow tropical waters, became extinct. The solitary corals, which generally do not form reefs and inhabit colder and deeper (below the photic zone) areas of the ocean were less impacted by the K–T boundary. Colonial coral species rely upon symbiosis with photosynthetic algae, which collapsed due to the events surrounding the K–T boundary.[29][30] However, the use of data from coral fossils to support K–T extinction and subsequent Paleocene recovery must be weighed against the changes that occurred in coral ecosystems through the K–T boundary.[7]

The numbers of cephalopod, echinoderm, and bivalve genera exhibited significant diminution after the K–T boundary.[7] Most species of brachiopods, a small phylum of marine invertebrates, survived the K–T event and diversified during the early Paleocene.

Rudist bivalves from the Late Cretaceous of the Omani Mountains, United Arab Emirates. Scale bar is 10 mm.

Except for nautiloids (represented by the modern order Nautilida) and coleoids (which had already diverged into modern octopodes, squids, and cuttlefish) all other species of the molluscan class Cephalopoda became extinct at the K–T boundary. These included the ecologically significant belemnoids, as well as the ammonoids, a group of highly diverse, numerous, and widely distributed shelled cephalopods. Researchers have pointed out that the reproductive strategy of the surviving nautiloids, which rely upon few and larger eggs, played a role in outsurviving their ammonoid counterparts through the extinction event. The ammonoids utilized a planktonic strategy of reproduction (numerous eggs and planktonic larvae), which would have been devastated by the K–T boundary event. Additional research has shown that subsequent to this elimination of ammonoids from the global biota, nautiloids began an evolutionary radiation into shell shapes and complexities theretofore known only from ammonoids.[31][32]

Approximately 35% of echinoderm genera became extinct at the K–T boundary, although taxa that thrived in low-latitude, shallow-water environments during late Cretaceous had the highest extinction rate. Mid-latitude, deep-water echinoderms were much less affected at the K–T boundary. The pattern of extinction points to habitat loss, specifically the drowning of carbonate platforms, the shallow-water reefs in existence at that time, by the extinction event.[33]

Other invertebrate groups, including rudists (reef-building clams) and inoceramids (giant relatives of modern scallops), also became extinct at the K–T boundary.[34][35]

Fish

There are substantial fossil records of jawed fishes across the K–T 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,[7] and more than 90% of teleost fish (bony fish) families survived.[36] There is evidence of a mass kill of bony fishes at a fossil site immediately above the K–T boundary layer on Seymour Island near Antarctica, apparently precipitated by the K–T boundary event.[37] However, the marine and freshwater environments of fishes mitigated environmental effects of the extinction event.[38]

Terrestrial invertebrates

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–T 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.[39][40]

Terrestrial plants

There is overwhelming evidence of global disruption of plant communities at the K–T boundary.[41] However, there were important regional differences in plant succession. In North America, the data suggest massive devastation and mass extinction of plants at the K–T boundary sections, although there were substantial megafloral changes before the boundary.[42]

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.[39][43] In North America, approximately 57% of plant species became extinct. The Paleocene recovery of plants began with recolonizations by fern species, represented as a fern spike in the geologic record; this same type of fern recolonization was observed after the 1980 Mount St. Helens eruption.[44]

Due to the wholesale destruction of plants at the K–T 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.[45] 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 which followed the impact.[46]

Amphibians

There is no evidence of K–T boundary mass extinctions of amphibians, and there is strong evidence that most amphibians survived the event relatively unscathed.[7] Several in-depth studies of salamander genera in fossil beds in Montana show that six of seven genera were unchanged after the event.[47]

Frog species appear to have survived into the Paleocene with few species becoming extinct. However, the fossil record for frog families and genera is uneven.[7] An extensive survey of three genera of frogs in Montana show that they were unaffected by the K–T event and survived apparently unchanged.[47] The data show little or no evidence for extinction of amphibian families that bracket the K–T event. Amphibian survival resulted from the clade's ability to seek shelter in water or to build burrows in sediments, soil, wood, or beneath rocks.[38]

Non-archosaur reptiles

The two living non-archosaurian reptile taxa, testudines (turtles) and lepidosaurs (snakes, lizards, and worm lizards), along with choristoderes (semi-aquatic archosauromorphs which died out in the early Miocene), survived through the K–T boundary.[7] Over 80% of Cretaceous turtle species passed through the K–T boundary. Additionally, all six turtle families in existence at the end of the Cretaceous survived into the Tertiary and are represented by current species.[48]

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.[49]

The order Squamata, which is represented today by lizards, snakes, and amphisbaenia, radiated into various ecological niches during the Jurassic and were successful throughout the Cretaceous. They survived through the K–T 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.[7][48]

Non-archosaurian marine reptiles including mosasaurs and plesiosaurs, giant aquatic reptiles that were the top marine predators, became extinct by the end of the Cretaceous.[50][51]

Archosaurs

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.

Crocodylomorphs

Ten families of crocodilians or their close relatives are represented in the Maastrichtian fossil records, of which five died out prior to the K–T boundary.[52] Five families have both Maastrichtian and Paleocene fossil representatives. All of the surviving families of crocodilians inhabited freshwater and terrestrial environments, except for the Dyrosauridae which lived in freshwater and marine locations. Approximately 50% of crocodilian representatives survived across the K–T boundary, the only apparent trend being that no large crocodiles, such as the giant North American crocodile Deinosuchus, survived.[7] Crocodilian 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.[38] Jouve and colleagues suggested in 2008 that dyrosaurid juveniles 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–T event as marine environments.[53]

Pterosaurs

Only one family of pterosaurs, Azhdarchidae, was definitely present in the Maastrichtian, and it became extinct at the K–T 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. 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.[38][54][55]

Avian dinosaurs (birds)

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.[56] Several analyses of bird fossils show divergence of species prior to the K–T boundary, and that duck, chicken and ratite bird relatives coexisted with non-avian dinosaurs.[57] Neornithine birds survived the K–T boundary as a result of their abilities to dive, swim, or seek shelter in water and marshlands. Many species of birds can build burrows, or nest in tree holes or termite nests, all of which provided shelter from the environmental effects at the K–T boundary. Long-term survival past the boundary was assured as a result of filling ecological niches left empty by extinction of non-avian dinosaurs.[38]

Non-avian dinosaurs

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

More has been published about the extinction of dinosaurs at the K–T boundary than any other group of organisms. Excluding a few controversial claims, scientists agree that all non-avian dinosaurs became extinct at the K–T 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 choices.[58] 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–T 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 to be in short supply.[38] 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 in order to sustain their faster metabolism. Thus, under the circumstances of food chain disruption previously mentioned, non-avian dinosaurs died[10] 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.[59]

Whether the extinction occurred gradually or very suddenly is debatable, as both views have support in the fossil record. A study of 29 fossil sites in Catalan Pyrenees of Europe in 2010 support that dinosaurs there had great diversity until the proposed asteroid impact.[60] Others, like Currie (2001), have interpreted the fossil bearing rocks along Red Deer River in Alberta, Canada, as supporting a 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.[61] Other scientists have pointed out the same.[62]

Several researchers have argued for Paleocene dinosaurs. These arguments are based on the discovery of dinosaur remains in the Hell Creek Formation up to 1.3 metres (4 ft 3 in) above and 40,000 years later than the K–T boundary.[4] 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 Tertiary, approximately 64.5 Ma (about 1 million years after the K–T event). If their existence past the K–T boundary can be confirmed, these hadrosaurids would be considered a Dead Clade Walking.[5] Current research indicates that these fossils were eroded from their original locations and then re-buried in much later sediments (reworked).[6]

Hell Creek formation

Mammals

All major Cretaceous mammalian lineages, including monotremes (egg-laying mammals), multituberculates, marsupials and placentals, dryolestoideans,[63] and gondwanatheres[64] survived the K–T event, although they suffered losses. In particular, marsupials largely disappeared from North America, and the Asian deltatheroidans, primitive relatives of extant marsupials, became extinct.[65] 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.[58]

Mammalian species began diversifying approximately 30 million years prior to the K–T boundary. Diversification of mammals stalled across the boundary.[66] Current research indicates that mammals did not explosively diversify across the K–T boundary, despite the environment niches made available by the extinction of dinosaurs.[67] Several mammalian orders have been interpreted as diversifying immediately after the K–T boundary, including Chiroptera (bats) and Cetartiodactyla (a diverse group that today includes whales and dolphins and even-toed ungulates),[67] although recent research concludes that only marsupial orders diversified after the K–T boundary.[66]

K–T 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–T boundary environmental stresses.[38]

Evidence

North American fossils

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.[41]

At present the most informative sequence of dinosaur-bearing rocks in the world from the K–T 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 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.[58]

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,[68] 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–T boundary. In the sediments below the K–T boundary the dominant plant remains are angiosperm pollen grains, but the actual boundary layer contains little pollen and is dominated by fern spores.[69] 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.[70]

Marine fossils

The mass extinction of marine plankton appears to have been abrupt and right at the K–T boundary.[71] Ammonite genera became extinct at or near the K–T 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–T boundary, and a small, gradual reduction in ammonite diversity occurred throughout the very late Cretaceous.[72] 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.[72]

Duration

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.[73] Scientists have also found very few continuous beds of fossil-bearing rock which cover a time range from several million years before the K–T extinction to a few million years after it.[7]

Causes of extinctions

There have been several theories on the cause of the K–T boundary which led to the massive extinction. These theories have centered on either impact events or increased volcanism; some include elements of both.

Impact event

Main articles: K–T boundary, Alvarez hypothesis, Chicxulub crater, and Shiva crater
The K–T boundary exposure in Trinidad Lake State Park, in the Raton Basin of Colorado, shows an abrupt change from dark- to light-colored rock.
White line added to mark the transition.
Radar topography reveals the 180 kilometers (112 mi) wide ring of the Chicxulub Crater.

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–Tertiary boundary contain a concentration of iridium many times greater than normal (30 times and 130 times background in the two sections originally studied). Iridium is extremely rare in the earth's crust because it is a siderophile, and therefore most of it travelled with the iron as it sank into the 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–T boundary.[74] There were other earlier speculations on the possibility of an impact event, but this was the first evidence uncovered.[75]

Such an impact would have inhibited photosynthesis by generating a dust cloud, which would block sunlight for a year or less, and by injecting sulfuric acid aerosols into the stratosphere, which would reduce 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.[59][71] 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.[38] Global firestorms may have resulted from the heat pulse and the fall back to Earth of incendiary fragments from the blast. High O2 levels during the late Cretaceous would have supported intense combustion. The level of atmospheric O2 plummeted in the early Tertiary Period. If widespread fires occurred, they would have increased the CO2 content of the atmosphere and caused a temporary greenhouse effect once the dust cloud settled, and this would have exterminated the most vulnerable organisms that survived the period immediately after the impact.[76]

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.[71] 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 under ten years.[77]

Subsequent research identified the Chicxulub Crater buried under Chicxulub on the coast of Yucatán, Mexico as the impact crater which matched the Alvarez hypothesis dating. Identified in 1990 based on the work of Glen Penfield done in 1978, this crater is oval, with an average diameter of about 180 kilometers (112 mi), about the size calculated by the Alvarez team.[78] 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 which 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 which 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.[79]

Most paleontologists now agree that an asteroid did hit the Earth about 65 Ma ago, but there is an ongoing dispute whether the impact was the sole cause of the extinctions.[24][80] There is evidence that there was an interval of about 300 ka from the impact to the mass extinction.[81] 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 2007, a hypothesis was put forth that argued the impactor that killed the dinosaurs 65 Ma ago belonged to the Baptistina family of asteroids.[82] Concerns have been raised regarding the reputed link, in part because very few solid observational constraints exist of the asteroid or family.[83] Indeed, it was recently discovered that 298 Baptistina does not share the same chemical signature as the source of the K–T impact.[84] Although this finding may make the link between the Baptistina family and K–T impactor more difficult to substantiate, it does not preclude the possibility.[84]

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 a 10–15 km space rock hurtled into earth at Chicxulub on Mexico's Yucatan Peninsula. The collision would have released the same energy as 100 trillion tonnes of TNT or over a billion times the energy of the bombs dropped on Nagasaki and Hiroshima.[9]

Deccan Traps

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 for over 2 million years. The most recent evidence shows that the traps erupted over 800,000 years spanning the K–T boundary, and therefore may be responsible for the extinction and the delayed biotic recovery thereafter.[85]

The Deccan Traps could have caused extinction through several mechanisms, including the release of dust and sulfuric aerosols into the air which might have blocked sunlight and thereby reduced photosynthesis in plants. In addition, Deccan Trap volcanism might have resulted in carbon dioxide emissions which would have increased the greenhouse effect when the dust and aerosols cleared from the atmosphere.[86]

In the years when the Deccan Traps hypothesis was linked to a slower extinction, Luis Alvarez (who died in 1988) replied that paleontologists were being misled by sparse data. While his assertion was not initially well-received, later intensive field studies of fossil beds lent weight to his claim. Eventually, most paleontologists began to accept the idea that the mass extinctions at the end of the Cretaceous were largely or at least partly due to a massive Earth impact. However, even Walter Alvarez has acknowledged that there were other major changes on Earth even before the impact, such as a drop in sea level and massive volcanic eruptions that produced the Indian Deccan Traps, and these may have contributed to the extinctions.[87]

Multiple impact event

Several other craters also appear to have been formed about the time of the K–T boundary. This suggests the possibility of near simultaneous multiple impacts, perhaps from a fragmented asteroidal object, similar to the Shoemaker-Levy 9 cometary impact with Jupiter. In addition to the 180-km (112 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 (60–65 Ma), and the controversial and much bigger 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.[88][89][90][91][92]

Maastrichtian sea-level regression

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 ones are terrestrial; earlier ones represent shorelines and the earliest 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 which is currently accepted as the most likely is that the mid-ocean ridges became less active and therefore sank under their own weight.[7][93]

A severe regression would have greatly reduced the continental shelf area, which is the most species-rich part of the sea, and therefore could have been enough to cause a marine mass extinction. However research concludes that this change would have been insufficient to cause the observed level of ammonite extinction. The regression would also have caused climate changes, partly by disrupting winds and ocean currents and partly by reducing the Earth's albedo and therefore increasing global temperatures.[72]

Marine regression also resulted in the loss of epeiric seas, such as the Western Interior Seaway of North America. The loss of these seas greatly altered habitats, removing coastal plains that ten million years before had been host to diverse communities such as are found in rocks of the Dinosaur Park Formation. Another consequence was an expansion of freshwater environments, since continental runoff now had longer distances to travel before reaching oceans. While this change was favorable to freshwater vertebrates, those that prefer marine environments, such as sharks, suffered.[58]

Multiple causes

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 to be 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.[58]

See also

Footnotes

  1. ↑ Fortey, R (1999). Life: A Natural History of the First Four Billion Years of Life on Earth. Vintage. pp. 238–260. ISBN 9780375702617. 
  2. ↑ Gradstein, F; Ogg J, Smith A. A Geologic Time Scale 2004. http://www.cambridge.org/uk/catalogue/catalogue.asp?isbn=0521781426. 
  3. ↑ Fastovsky DE, Sheehan PM (2005). "The extinction of the dinosaurs in North America". GSA Today 15 (3): 4–10. doi:10.1130/1052-5173(2005)015<4:TEOTDI>2.0.CO;2. http://www.gsajournals.org/perlserv/?request=get-document&doi=10.1130%2F1052-5173%282005%29015%3C4%3ATEOTDI%3E2.0.CO%3B2. Retrieved 2007-05-18. 
  4. ↑ 4.0 4.1 Sloan RE, Rigby K, Van Valen LM, Gabriel Diane (1986). "Gradual dinosaur extinction and simultaneous ungulate radiation in the Hell Creek formation". Science 232 (4750): 629–633. doi:10.1126/science.232.4750.629. PMID 17781415. http://www.sciencemag.org/cgi/content/abstract/232/4750/629. Retrieved 2007-05-18. 
  5. ↑ 5.0 5.1 Fassett JE, Lucas SG, Zielinski RA, Budahn JR (2001). "Compelling new evidence for Paleocene dinosaurs in the Ojo Alamo Sandstone San Juan Basin, New Mexico and Colorado, USA" (PDF). International Conference on Catastrophic Events and Mass Extinctions: Impacts and Beyond, 9–12 July 2000, Vienna, Austria 1053: 45–46. http://www.lpi.usra.edu/meetings/impact2000/pdf/3139.pdf. Retrieved 2007-05-18. 
  6. ↑ 6.0 6.1 Sullivan RM (2003). "No Paleocene dinosaurs in the San Juan Basin, New Mexico". Geological Society of America Abstracts with Programs 35 (5): 15. http://gsa.confex.com/gsa/2003RM/finalprogram/abstract_47695.htm. Retrieved 2007-07-02. 
  7. ↑ 7.00 7.01 7.02 7.03 7.04 7.05 7.06 7.07 7.08 7.09 7.10 7.11 7.12 7.13 7.14 7.15 7.16 7.17 7.18 7.19 7.20 MacLeod N, Rawson PF, Forey PL, Banner FT, Boudagher-Fadel MK, Bown PR, Burnett JA, Chambers, P, Culver S, Evans SE, Jeffery C, Kaminski MA, Lord AR, Milner AC, Milner AR, Morris N, Owen E, Rosen BR, Smith AB, Taylor PD, Urquhart E, Young JR (1997). "The Cretaceous–Tertiary biotic transition". Journal of the Geological Society 154 (2): 265–292. doi:10.1144/gsjgs.154.2.0265. http://findarticles.com/p/articles/mi_qa3721/is_199703/ai_n8738406/print. 
  8. ↑ Myra MacDonald (March 4, 2010). "It's official: An asteroid wiped out the dinosaurs". Reuters. http://www.reuters.com/article/idUSTRE6233YW20100304?loomia_ow=t0:s0:a49:g43:r3:c0.100000:b31301396:z0. 
  9. ↑ 9.0 9.1 Schulte, Peter; Alegret, Laia; Arenillas, Ignacio; Arz, Jose A.; Barton, Penny J.; Bown, Paul R.; Bralower, Timothy J.; Christeson, Gail L.; Claeys, Philippe; Cockell, Charles S.; Collins, Gareth S.; Deutsch, Alexander; Goldin, Tamara J.; Goto, Kazuhisa; Grajales-Nishimura, José M.; Grieve, Richard A. F.; Gulick, Sean P. S.; Johnson, Kirk R.; Kiessling, Wolfgang; Koeberl, Christian; Kring, David A.; MacLeod, Kenneth G.; Matsui, Takafumi; Melosh, Jay; Montanari, Alessandro; Morgan, Joanna V.; Neal,Clive R.; Nichols, Douglas J.; Norris, Richard D.; Pierazzo, Elisabetta ; Ravizza, Greg; Rebolledo-Vieyra, Mario; Uwe Reimold, Wolf; Robin, Eric ; Salge, Tobias; Speijer, Robert P.; Sweet, Arthur R.; Urrutia-Fucugauchi, Jaime; Vajda, Vivi; Whalen, Michael T.; Willumsen, Pi S. (5 March 2010). "The Chicxulub Asteroid Impact and Mass Extinction at the Cretaceous- Paleogene Boundary". Science 327 (5970): 1214–1218. doi:10.1126/science.1177265. PMID 20203042. http://www.sciencemag.org/cgi/content/abstract/327/5970/1214. Retrieved 2010-03-08. 
  10. ↑ 10.0 10.1 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. 
  11. ↑ 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. http://palaios.geoscienceworld.org/cgi/reprint/19/1/96. Retrieved 2007-06-17. 
  12. ↑ 12.0 12.1 Sheehan Peter M, Hansen Thor A (1986). "Detritus feeding as a buffer to extinction at the end of the Cretaceous". Geology 14 (10): 868–870. doi:10.1130/0091-7613(1986)14<868:DFAABT>2.0.CO;2. http://geology.geoscienceworld.org/cgi/content/abstract/14/10/868. Retrieved 2007-07-04. 
  13. ↑ 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. doi:10.1130/G23197A.1. 
  14. ↑ Sheehan Peter M, Fastovsky DE (1992). "Major extinctions of land-dwelling vertebrates at the Cretaceous–Tertiary boundary, eastern Montana". Geology 20 (6): 556–560. doi:10.1130/0091-7613(1992)020<0556:MEOLDV>2.3.CO;2. http://www.geoscienceworld.org/cgi/georef/1992034409. Retrieved 2007-06-22. 
  15. ↑ Pospichal JJ (1996). "Calcareous nannofossils and clastic sediments at the Cretaceous–Tertiary boundary, northeastern Mexico". Geology 24 (3): 255–258. doi:10.1130/0091-7613(1996)024<0255:CNACSA>2.3.CO;2. http://geology.geoscienceworld.org/cgi/content/abstract/24/3/255. 
  16. ↑ Bown P (2005). "Selective calcareous nannoplankton survivorship at the Cretaceous–Tertiary boundary". Geology 33 (8): 653–656. doi:10.1130/G21566.1. http://geology.geoscienceworld.org/cgi/content/abstract/33/8/653. 
  17. ↑ 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. http://paleobiol.geoscienceworld.org/cgi/content/abstract/30/4/522. 
  18. ↑ 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. doi:10.1144/GSL.SP.2004.230.01.13. 
  19. ↑ MacLeod N (1998). "Impacts and marine invertebrate extinctions". Geological Society, London, Special Publications 140: 217–246. doi:10.1144/GSL.SP.1998.140.01.16. http://sp.lyellcollection.org/cgi/content/abstract/140/1/217. 
  20. ↑ Courtillot, V (1999). Evolutionary Catastrophes: The Science of Mass Extinction. Cambridge University Press. p. 2. ISBN 0521583926. http://books.google.com/?id=qiegJbafYkUC&pg=PA23&lpg=PA23&dq=foraminifera+kt+1930s. 
  21. ↑ Glaessner MF (1937). "Studien Ober Foraminiferen aus der Kreide und dem Tertiar des Kaukasus. I-Die Foraminiferen der altesten Tertifrschichten des Nordwestkaukasus". Problems in Paleontology 2–3: 349–410. 
  22. ↑ 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. 
  23. ↑ 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 9780393966572. 
  24. ↑ 24.0 24.1 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. doi:10.1073/pnas.0400396101. PMID 15004276. 
  25. ↑ 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. http://www.es.ucl.ac.uk/people/m-kaminski/reprints-pdfs/Galeotti_etal2002.pdf. Retrieved 2007-08-19. 
  26. ↑ 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. http://www-odp.tamu.edu/publications/149_SR/VOLUME/CHAPTERS/SR149_08.PDF. Retrieved 2007-08-19. 
  27. ↑ Coles, GP; Ayress MA, and Whatley RC (1990). A comparison of North Atlantic and 20 Pacific deep-sea Ostracoda in Ostracoda and global events (RC Whatley and C Maybury, editors). Chapman & Hall. pp. 287–305. ISBN 9780442311674. 
  28. ↑ Brouwers EM, De Deckker P (1993). "Late Maastrichtian and Danian Ostracode Faunas from Northern Alaska: Reconstructions of Environment and Paleogeography". PALAIOS (PALAIOS, Vol. 8, No. 2) 8 (2): 140–154. doi:10.2307/3515168. http://jstor.org/stable/3515168. 
  29. ↑ 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. 
  30. ↑ Rosen BR, Turnsek D (1989). "Extinction patterns and biogeography of scleractinian corals across the Cretaceous/Tertiary boundary. Fossil Cnidaria 5.P.". Association of Australasian Paleontology Memoir Number 8, Jell A, Pickett JW (eds): 355–370. 
  31. ↑ 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. doi:10.1130/0091-7613(1991)019<1181:AAIBEP>2.3.CO;2. http://geology.geoscienceworld.org/cgi/content/abstract/19/12/1181. 
  32. ↑ 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. doi:10.1130/0091-7613(2002)030<0955:MCTBSI>2.0.CO;2. 
  33. ↑ 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. 
  34. ↑ Raup DM and Jablonski D (1993). "Geography of end-Cretaceous marine bivalve extinctions". Science 260 (5110): 971–973. doi:10.1126/science.11537491. PMID 11537491. 
  35. ↑ 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. 
  36. ↑ Patterson, C (1993). Osteichthyes: Teleostei. In: The Fossil Record 2 (Benton, MJ, editor). Springer. pp. 621–656. ISBN 0412393808. 
  37. ↑ Zinsmeister WJ (1 May 1998). "Discovery of fish mortality horizon at the K–T boundary on Seymour Island: Re-evaluation of events at the end of the Cretaceous". Journal of Paleontology 72 (3): 556–571. http://jpaleontol.geoscienceworld.org/cgi/content/abstract/72/3/556?maxtoshow=&HITS=10&hits=10&RESULTFORMAT=1&author1=zinsmeister&andorexacttitle=and&field_name=fulltext&searchid=1&FIRSTINDEX=0&sortspec=relevance&fdate=7/1/1927&tdate=7/31/2007&resourcetype=HWCIT. Retrieved 2007-08-27. 
  38. ↑ 38.0 38.1 38.2 38.3 38.4 38.5 38.6 38.7 Robertson DS, McKenna MC, Toon OB, Hope S, Lillegraven JA (2004). "Survival in the first hours of the Cenozoic" (PDF). GSA Bulletin 116 (5–6): 760–768. doi:10.1130/B25402.1. http://www.ugcs.caltech.edu/~presto/cenozoic.pdf. Retrieved 2007-08-31. 
  39. ↑ 39.0 39.1 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. doi:10.1073/pnas.042492999. PMID 11854501. PMC 122319. http://www.geosc.psu.edu/~pwilf/LabandeiraJohnsonWilf%202002PNAS.pdf. 
  40. ↑ Wilf P, Labandeira CC, Johnson KR, Ellis B (2006). "Decoupled Plant and Insect Diversity After the End-Cretaceous Extinction". Science 313 (5790): 1112–1115. doi:10.1126/science.1129569. PMID 16931760. 
  41. ↑ 41.0 41.1 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. doi:10.1126/science.1064706. PMID 11721051. http://www.sciencemag.org/cgi/content/abstract/294/5547/1700. 
  42. ↑ 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 9780813722474. 
  43. ↑ 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 9780393966572. 
  44. ↑ Schultz PH, D'Hondt S (1996). "Cretaceous–Tertiary (Chicxulub) impact angle and its consequences". Geology 24 (11): 963–967. doi:10.1130/0091-7613(1996)024<0963:CTCIAA>2.3.CO;2. http://geology.geoscienceworld.org/cgi/content/abstract/24/11/963. Retrieved 2007-07-05. 
  45. ↑ 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. http://www.geol.lu.se/personal/VIV/Vajda%20&McLoughlin%202004.pdf. Retrieved 2007-07-07. 
  46. ↑ doi: 10.1073/pnas.0900906106
    This citation will be automatically completed in the next few minutes. You can jump the queue or expand by hand
  47. ↑ 47.0 47.1 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. 
  48. ↑ 48.0 48.1 Novacek MJ (1999). "100 Million Years of Land Vertebrate Evolution: The Cretaceous-Early Tertiary Transition". Annals of the Missouri Botanical Garden (Annals of the Missouri Botanical Garden, Vol. 86, No. 2) 86 (2): 230–258. doi:10.2307/2666178. http://jstor.org/stable/2666178. 
  49. ↑ Lutz, D (2005). Tuatara: A Living Fossil. DIMI Press. ISBN 0-931625-43-2. 
  50. ↑ Chatterjee S, Small BJ (1989). "New plesiosaurs from the Upper Cretaceous of Antarctica". Geological Society, London, Special Publications 47: 197–215. doi:10.1144/GSL.SP.1989.047.01.15. http://sp.lyellcollection.org/cgi/content/abstract/47/1/197. Retrieved 2007-07-04. 
  51. ↑ O'Keefe FR (2001). "A cladistic analysis and taxonomic revision of the Plesiosauria (Reptilia: Sauropterygia)". Acta Zoologica Fennica 213: 1–63. 
  52. ↑ Brochu CA (2004). "Calibration age and quartet divergence date estimation". Evolution 58 (6): 1375–1382. doi:10.1554/03-509. PMID 15266985. 
  53. ↑ Jouve, Stéphane; Bardet, Nathalie; Jalil, Nour-Eddine; Suberbiola, Xabier Pereda; Bouya, Baâdi; Amaghzaz, Mbarek (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. 
  54. ↑ 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. http://mbe.oxfordjournals.org/cgi/reprint/23/6/1144. 
  55. ↑ 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. 
  56. ↑ 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. doi:10.1126/science.274.5290.1164. PMID 8895459. 
  57. ↑ 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. doi:10.1038/nature03150. PMID 15662422. 
  58. ↑ 58.0 58.1 58.2 58.3 58.4 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. http://www.bio.sdsu.edu/faculty/archibald/ArchFast.pdf. 
  59. ↑ 59.0 59.1 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 (Cockell C, Gilmour I, Koeberl C, editors). SpringerLink. pp. 197–219. ISBN 9783540257356. http://www.springerlink.com/content/vw75014157p2p278/. 
  60. ↑ Discovery News: Dinosaurs did not gradually die out, Jennifer Vegas, 18 March 2010.
  61. ↑ Philip J. Currie on the extinction of dinosaurs in Discovery Channel's program When Dinosaurs Roamed America, 2001. See http://dsc.discovery.com/videos/dinosaurs-the-end-of-the-dinosaurs.html.
  62. ↑ Jake Page & Chales B. Officer, The great dinosaur extinction controversy, 1996.
  63. ↑ 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. 
  64. ↑ 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. doi:10.1144/GSL.SP.2006.258.01.10. 
  65. ↑ McKenna, MC; Bell SK (1997). Classification of Mammals: Above the Species Level. Columbia University Press. ISBN 978-0-231-11012-9. 
  66. ↑ 66.0 66.1 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. doi:10.1038/nature05634. PMID 17392779. http://www.uni-oldenburg.de/molekularesystematik/download/Publications/mammalST.pdf. 
  67. ↑ 67.0 67.1 Springer MS, Murphy WJ, Eizirik E, O'Brien SJ (2003). "Placental mammal diversification and the Cretaceous–Tertiary boundary" (PDF). PNAS 100 (3): 1056–1061. doi:10.1073/pnas.0334222100. PMID 12552136. PMC 298725. http://www.pnas.org/cgi/reprint/100/3/1056.pdf. 
  68. ↑ Dodson, Peter (1996). The Horned Dinosaurs: A Natural History. Princeton: Princeton University Press. pp. 279–281. ISBN 0-691-05900-4. 
  69. ↑ "Online guide to the continental Cretaceous–Tertiary boundary in the Raton basin, Colorado and New Mexico". U.S. Geological Survey. 2004. http://esp.cr.usgs.gov/info/kt/stop2b.html. Retrieved 2007-07-08. 
  70. ↑ 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. http://www.nps.gov/history/history/online_books/science/5/contents.htm. Retrieved 2007-07-09. 
  71. ↑ 71.0 71.1 71.2 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. doi:10.1073/pnas.95.19.11028. PMID 9736679. PMC 33889. http://www.pnas.org/cgi/content/full/95/19/11028. 
  72. ↑ 72.0 72.1 72.2 Marshall CR, Ward PD (1996). "Sudden and Gradual Molluscan Extinctions in the Latest Cretaceous of Western European Tethys". Science 274 (5291): 1360–1363. doi:10.1126/science.274.5291.1360. PMID 8910273. 
  73. ↑ Signor III PW, Lipps JH (1982). "Sampling bias, gradual extinction patterns, and catastrophes in the fossil record. In: Geological implications of impacts of large asteroids and comets on the Earth, Silver LT, Schultz PH (editors)". Geological Society of America Special Publication 190: 291–296. 
  74. ↑ Alvarez LW, Alvarez W, Asaro F, Michel HV (1980). "Extraterrestrial cause for the Cretaceous–Tertiary extinction". Science 208 (4448): 1095–1108. doi:10.1126/science.208.4448.1095. PMID 17783054. 
  75. ↑ De Laubenfels MW (1956). "Dinosaur extinction: One more hypothesis". Journal of Paleontology (Journal of Paleontology, Vol. 30, No. 1) 30 (1): 207–218. http://www.jstor.org/pss/1300393. 
  76. ↑ 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. doi:10.1029/97JE01743. PMID 11541145. http://www.agu.org/pubs/crossref/1997/97JE01743.shtml. 
  77. ↑ Kring DA (2003). "Environmental consequences of impact cratering events as a function of ambient conditions on Earth". Astrobiology 3 (1): 133–152. doi:10.1089/153110703321632471. PMID 12809133. 
  78. ↑ Pope KO, Ocampo AC, Kinsland GL, Smith R (1996). "Surface expression of the Chicxulub crater". 24 (6): 527–530. doi:10.1130/0091-7613(1996)024<0527:SEOTCC>2.3.CO;2. PMID 11539331. 
  79. ↑ 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: 131–135. doi:10.1038/ngeo103. Lay summary. 
  80. ↑ Morgan J, Lana C, Kersley A, Coles B, Belcher C, Montanari S, Diaz-Martinez E, Barbosa A, Neumann V (2006). "Analyses of shocked quartz at the global K-P boundary indicate an origin from a single, high-angle, oblique impact at Chicxulub". Earth and Planetary Science Letters 251 (3–4): 264–279. doi:10.1016/j.epsl.2006.09.009. 
  81. ↑ Keller G, Abramovich S, Berner Z, Adatte T (1 January 2009). "Biotic effects of the Chicxulub impact, K–T catastrophe and sea level change in Texas". Palaeogeography, Palaeoclimatology, Palaeoecology 271 (1–2): 52–68. doi:10.1016/j.palaeo.2008.09.007. 
  82. ↑ Bottke W., Vokrouhlický D., Nesvorný D. (2007) An asteroid breakup 160 Myr ago as the probable source of the K/T impactor. Nature 449, 48–53
  83. ↑ Majaess D., Higgins D., Molnar L., Haegert M., Lane D., Turner D., Nielsen I. (2008). New Constraints on the Asteroid 298 Baptistina, the Alleged Family Member of the K/T Impactor, accepted for publication in the JRASC
  84. ↑ 84.0 84.1 Reddy V., et al. (2008). Composition of 298 Baptistina: Implications for K–T Impactor Link, Asteroids, Comets, Meteors conference.
  85. ↑ Keller G, Adatte T, Gardin S, Bartolini A, Bajpai S (2008). "Main Deccan volcanism phase ends near the K–T boundary: Evidence from the Krishna-Godavari Basin, SE India". Earth and Planetary Science Letters 268: 293–311. doi:10.1016/j.epsl.2008.01.015. 
  86. ↑ Duncan RA, Pyle DG (1988). "Rapid eruption of the Deccan flood basalts at the Cretaceous/Tertiary boundary". Nature 333: 841–843. doi:10.1038/333841a0. 
  87. ↑ Alvarez, W (1997). T. rex and the Crater of Doom. Princeton University Press. pp. 130–146. ISBN 9780691016306. 
  88. ↑ Mullen L (October 13, 2004). "Debating the Dinosaur Extinction". Astrobiology Magazine. http://www.astrobio.net/news/article1243.html. Retrieved 2007-07-11. 
  89. ↑ Mullen L (October 20, 2004). "Multiple impacts". Astrobiology Magazine. http://www.astrobio.net/news/article1253.html. Retrieved 2007-07-11. 
  90. ↑ Mullen L (November 3, 2004). "Shiva: Another K–T impact?". Astrobiology Magazine. http://www.astrobio.net/news/article1281.html. Retrieved 2007-07-11. 
  91. ↑ 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 9789067642545. http://books.google.com/?id=3IORF1Ei3LIC&pg=PA31&dq=Chatterjee+and+Rudra+1996+Shiva. Retrieved 2008-02-22. 
  92. ↑ Teters, Thomas J. (2005-07-28). "Wiping out the Dinosaur with Five Simultaneous Impacts…". Starmon.com. http://starmon.com/KT_craters.html. Retrieved 2008-01-23. 
  93. ↑ Liangquan L, Keller G (1998). "Abrupt deep-sea warming at the end of the Cretaceous". Geology 26: 995–998. doi:10.1130/0091-7613(1998)026<0995:ADSWAT>2.3.CO;2. http://geology.geoscienceworld.org/cgi/content/abstract/26/11/995. 

Further reading

External links

Cretaceous–Tertiary extinction event
Proposed K–T boundary craters: Boltysh crater · Chicxulub crater · Shiva crater · Silverpit crater
Extinction events
Minor events
↓End-Ediacaran?
↓Lau event
↓Toarcian turnover
↓Aptian
↓Cenomanian-Turonian
↓Middle Miocene
    disruption
↓Cambro-Ordovician
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Millions of years before present