Cretaceous–Paleogene Extinction Event: Comparison
View Latest Version
Please note this is a comparison between Version 2 by Camila Xu and Version 1 by Camila Xu.

The Cretaceous–Paleogene (K–Pg) extinction event,[lower-alpha 1] also known as the Cretaceous–Tertiary (K–T) extinction,[lower-alpha 2] was a sudden mass extinction of three-quarters of the plant and animal species on Earth, approximately 66  million years ago. With the exception of some ectothermic species such as the sea turtles and crocodilians, no tetrapods weighing more than 25 kilograms (55 pounds) survived. It marked the end of the Cretaceous period, and with it the end of the entire Mesozoic Era, opening the Cenozoic Era that continues today. In the geologic record, the K–Pg event is marked by a thin layer of sediment called the K–Pg boundary, which can be found throughout the world in marine and terrestrial rocks. The boundary clay shows high levels of the metal iridium, which is rare in the Earth's crust, but abundant in asteroids. As originally proposed in 1980 by a team of scientists led by Luis Alvarez and his son Walter, it is now generally thought that the K–Pg extinction was caused by the impact of a massive comet or asteroid 10 to 15  km (6 to 9  mi) wide, 66  million years ago, which devastated the global environment, mainly through a lingering impact winter which halted photosynthesis in plants and plankton. The impact hypothesis, also known as the Alvarez hypothesis, was bolstered by the discovery of the 180  km (112  mi) Chicxulub crater in the Gulf of Mexico's Yucatán Peninsula in the early 1990s, which provided conclusive evidence that the K–Pg boundary clay represented debris from an asteroid impact. The fact that the extinctions occurred simultaneously provides strong evidence that they were caused by the asteroid. A 2016 drilling project into the Chicxulub peak ring confirmed that the peak ring comprised granite ejected within minutes from deep in the earth, but contained hardly any gypsum, the usual sulfate-containing sea floor rock in the region: The gypsum would have vaporized and dispersed as an aerosol into the atmosphere, causing longer-term effects on the climate and food chain. In October  2019, researchers reported that the event rapidly acidified the oceans producing ecological collapse and, in this way as well, produced long-lasting effects on the climate, and accordingly was a key reason for the end-Cretaceous mass extinction. In January 2020, scientists reported new evidence that the extinction event was mostly a result of the meteorite impact and not volcanism. Other causal or contributing factors to the extinction may have been the Deccan Traps and other volcanic eruptions, climate change, and sea level change. A wide range of species perished in the K–Pg extinction, the best-known being the non-avian dinosaurs. It also destroyed a myriad of other terrestrial organisms, including some mammals, pterosaurs, birds, lizards, insects, and plants. In the oceans, the K–Pg extinction killed off plesiosaurs and mosasaurs and devastated teleost fish, sharks, mollusks (especially ammonites, which became extinct), and many species of plankton. It is estimated that 75% or more of all species on Earth vanished. Yet the extinction also provided evolutionary opportunities: In its wake, many groups underwent remarkable adaptive radiation — sudden and prolific divergence into new forms and species within the disrupted and emptied ecological niches. Mammals in particular diversified in the Paleogene, evolving new forms such as horses, whales, bats, and primates. The surviving group of dinosaurs were avians, ground and water fowl who radiated into all modern species of bird. Teleost fish, and perhaps lizards also radiated.

  • ecological collapse
  • meteorite impact
  • crocodilians

1. Extinction Patterns

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 traditional "Big Five" extinction events and the more recently recognised End-Capitanian extinction event are clickable hyperlinks; see Extinction event for more details. 

The K–Pg extinction event was severe, global, rapid, and selective, eliminating a vast number of species. Based on marine fossils, it is estimated that 75% or more of all species were made extinct.[1]

The event appears to have affected all continents at the same time. Non-avian dinosaurs, for example, are known from the Maastrichtian of North America, Europe, Asia, Africa, South America, and Antarctica,[2] but are unknown from the Cenozoic anywhere in the world. Similarly, fossil pollen shows devastation of the plant communities in areas as far apart as New Mexico, Alaska, China , and New Zealand.[3]

Despite the event's severity, 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 ground. This plant extinction caused a major reshuffling of the dominant plant groups.[4] Omnivores, insectivores, and carrion-eaters survived the extinction event, perhaps because of the increased availability of their food sources. No purely herbivorous or carnivorous mammals seem to have survived. Rather, the surviving mammals and birds fed on insects, worms, and snails, which in turn fed on detritus (dead plant and animal matter).[5][6][7]

In stream communities, few animal groups became extinct, because such communities rely less directly on food from living plants, and more on detritus washed in from the land, protecting them from extinction.[8] 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 on the ocean floor always or sometimes feed on detritus.[5] Coccolithophorids and mollusks (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.[9] The largest air-breathing survivors of the event, crocodyliforms and champsosaurs, were semi-aquatic and had access to detritus. Modern crocodilians can live as scavengers and survive for months without food, and their young are small, grow slowly, and feed largely on invertebrates and dead organisms for their first few years. These characteristics have been linked to crocodilian survival at the end of the Cretaceous.[6]

After the K–Pg extinction event, biodiversity required substantial time to recover, despite the existence of abundant vacant ecological niches.[5]

1.1. Microbiota

The K–Pg boundary represents one of the most dramatic turnovers in the fossil record for various calcareous nanoplankton that formed the calcium deposits for which the Cretaceous is named. The turnover in this group is clearly marked at the species level.[10][11] 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.[12] The K–Pg boundary record of dinoflagellates is not so well understood, mainly because only microbial cysts provide a fossil record, and not all dinoflagellate species have cyst-forming stages, which likely causes diversity to be underestimated.[5] Recent studies indicate that there were no major shifts in dinoflagellates through the boundary layer.[13]

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.[5] Approximately 46% of diatom species survived the transition from the Cretaceous to the Upper Paleocene, a significant turnover in species but not a catastrophic extinction.[5][14]

The occurrence of planktonic foraminifera across the K–Pg boundary has been studied since the 1930s.[15] 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;[5] there is ongoing debate between groups which think the evidence indicates substantial extinction of these species at the K–Pg boundary,[16] and those who think the evidence supports multiple extinctions and expansions through the boundary.[17][18]

Numerous species of benthic foraminifera became extinct during the event, presumably because they depend on organic debris for nutrients, while biomass in the ocean is thought to have decreased. As the marine microbiota recovered, it is thought that increased speciation of benthic foraminifera resulted from the increase in food sources.[5] 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.[19][20]

1.2. Marine Invertebrates

Discoscaphites iris ammonite from the Owl Creek Formation (Upper Cretaceous), Owl Creek, Ripley, Mississippi

There is significant variation in the fossil record as to the extinction rate of marine invertebrates across the K–Pg boundary. The apparent rate is influenced by a lack of fossil records, rather than extinctions.[5]

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 ostracod diversity was lower in the Paleocene than any other time in the Cenozoic. Current research cannot ascertain whether the extinctions occurred prior to, or during, the boundary interval.[21][22]

Approximately 60% of late-Cretaceous Scleractinia coral genera failed to cross the K–Pg 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–Pg boundary. Colonial coral species rely upon symbiosis with photosynthetic algae, which collapsed due to the events surrounding the K–Pg boundary,[23][24] but the use of data from coral fossils to support K–Pg extinction and subsequent Paleocene recovery, must be weighed against the changes that occurred in coral ecosystems through the K–Pg boundary.[5]

The numbers of cephalopod, echinoderm, and bivalve genera exhibited significant diminution after the K–Pg boundary.[5] Most species of brachiopods, a small phylum of marine invertebrates, survived the K–Pg extinction 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–Pg 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–Pg extinction 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.[25][26]

Approximately 35% of echinoderm genera became extinct at the K–Pg boundary, although taxa that thrived in low-latitude, shallow-water environments during the late Cretaceous had the highest extinction rate. Mid-latitude, deep-water echinoderms were much less affected at the K–Pg 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.[27]

Other invertebrate groups, including rudists (reef-building clams) and inoceramids (giant relatives of modern scallops), also became extinct at the K–Pg boundary.[28][29]

1.3. Fish

There are substantial fossil records of jawed fishes across the K–Pg boundary, which provide good evidence of extinction patterns of these classes of marine vertebrates. While the deep sea realm was able to remain seemingly unaffected, there was an equal loss between the open marine apex predators and the durophagous demersal feeders on the continental shelf.

Within cartilaginous fish, approximately 7 out of the 41 families of neoselachians (modern sharks, skates, and rays) disappeared after this event and batoids (skates and rays) lost nearly all the identifiable species, while more than 90% of teleost fish (bony fish) families survived.[30][31]

In the Maastrichtian age, 28 shark families and 13 batoid families thrived, of which 25 and 9, respectively, survived the K–T boundary event. Forty-seven of all neoselachian genera cross the K–T boundary, with 85% being sharks. Batoids display with 15% a comparably low survival rate.[30][32]

There is evidence of a mass extinction 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;[33] the marine and freshwater environments of fishes mitigated the environmental effects of the extinction event.[34]

1.4. Terrestrial Invertebrates

Insect damage to the fossilized leaves of flowering plants from fourteen sites in North America was 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. During the early Paleocene, flora were relatively diverse with little predation from insects, even 1.7 million years after the extinction event.[35][36]

1.5. Terrestrial Plants

There is overwhelming evidence of global disruption of plant communities at the K–Pg boundary.[3][3][37][38] Extinctions are seen both in studies of fossil pollen, and fossil leaves.[3] In North America, the data suggests massive devastation and mass extinction of plants at the K–Pg boundary sections, although there were substantial megafloral changes before the boundary.[3][39] 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.[35][40] In some regions, the 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.[41]

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 plenty of organic matter to feed on was present. Once the atmosphere cleared, photosynthetic organisms, initially ferns and other ground-level plants, returned.[42] Just two species of fern appear to have dominated the landscape for centuries after the event.[43]

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.[44]

1.6. Fungi

While it appears that many fungi were wiped out at the KT boundary, it's noteworthy that evidence has been found of a "world of fungus" dominating for a few years after the event. Microfossils from that period indicate a great increase in fungal spores, long before the resumption of plentiful fern spores in the recovery after the impact.[45] Monoporisporites and hypha are almost exclusive microfossils for a short span during and after the iridium boundary. These saprophytes would not need sunlight, during the period where the atmosphere may have been clogged with dust and sulfur aerosols.

This "fungal world" appears to happen during many such extinction events, including the Permian-Triassic boundary, the largest known in earth's history, losing 90% of all species.[46]

1.7. Amphibians

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.[47] 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[48] and the albanerpetontid Albanerpeton galaktion;[49] 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.[50]

1.8. Non-Archosaurs

Turtles

More than 80% of Cretaceous turtle species passed through the K–Pg boundary. All six turtle families in existence at the end of the Cretaceous survived into the Paleogene and are represented by living species.[51]

Lepidosauria

The living non-archosaurian reptile taxa, lepidosaurians (snakes, lizards and tuataras), survived across the K–Pg boundary.[5] Living lepidosaurs include the tuataras (the only living rhynchocephalians) and the squamates.

The rhynchocephalians were a widespread and relatively successful group of lepidosaurians during the early Mesozoic, but began to decline by the mid-Cretaceous, although they were very successful in the Late Cretaceous of South America.[52] They are represented today by a single genus, located exclusively in New Zealand.[53]

Kronosaurus Hunt, a rendering by Dmitry Bogdanov in 2008. Large marine reptiles, including plesiosaurians such as these, became extinct at the end of the Cretaceous.

The order Squamata, which is represented today by lizards, snakes and amphisbaenians (worm lizards), radiated into various ecological niches during the Jurassic and was 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. Many families of terrestrial squamates became extinct at the boundary, such as monstersaurians and polyglyphanodonts, and fossil evidence indicates they suffered very heavy losses in the K–T event, only recovering 10 million years after it.[54]

Non-archosaurian marine reptiles

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.[55][56] The ichthyosaurs had disappeared from fossil records before the mass extinction occurred.

1.9. Archosaurs

The archosaur clade includes two surviving groups, crocodilians and birds, along with the various extinct groups of non-avian dinosaurs and pterosaurs.[57]

Crocodyliforms

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.[58] 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.[5] 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.[34] Jouve and colleagues suggested in 2008 that juvenile marine crocodyliforms lived in freshwater environments as do modern marine crocodile juveniles, which would have helped them survive where other marine reptiles became extinct; freshwater environments were not so strongly affected by the K–Pg extinction event as marine environments were.[59]

Pterosaurs

One family of pterosaurs, Azhdarchidae, was definitely present in the Maastrichtian, and it likely became extinct at the K–Pg boundary. These large pterosaurs were the last representatives of a declining group that contained ten families during the mid-Cretaceous. Several other pterosaur lineages may have been present during the Maastrichtian, such as the ornithocheirids, pteranodontids, nyctosaurids, as well as a possible tapejarid, though they are represented by fragmentary remains that are difficult to assign to any given group.[60][61] While this was occurring, modern birds were undergoing diversification; traditionally it was thought that they replaced archaic birds and pterosaur groups, possibly due to direct competition, or they simply filled empty niches,[34][62][63] but there is no correlation between pterosaur and avian diversities that are conclusive to a competition hypothesis,[64] and small pterosaurs were present in the Late Cretaceous.[65] At least some niches previously held by birds were reclaimed by pterosaurs prior to the K–Pg event.[66]

Birds

Most paleontologists regard birds as the only surviving dinosaurs (see Origin of birds). It is thought that all non-avian theropods became extinct, including then-flourishing groups such as enantiornithines and hesperornithiforms.[67] 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.[68] 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. The absence of these birds in the Paleogene is evidence that a mass extinction of archaic birds took place there.

The most successful and dominant group of birds, enantiornithes, were wiped out. Only a small fraction of ground and water-dwelling Cretaceous bird species survived the impact, giving rise to today's birds.[69][70] The only bird group known for certain to have survived the K–Pg boundary is the Aves.[69] Avians 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 avians 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.[34] The open niche space and relative scarcity of predators following the K-Pg extinction allowed for adaptive radiation of various avian groups. Ratites, for example, rapidly diversified in the early Paleogene and are believed to have convergently developed flightlessness at least three to six times, often fulfilling the niche space for large herbivores once occupied by non-avian dinosaurs.[71][72][73]

Non-avian dinosaurs

Tyrannosaurus was among the dinosaurs living 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.[74] There is no evidence that late Maastrichtian non-avian dinosaurs could burrow, swim, or dive, which suggests 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 herbivorous dinosaurs would have found plant material scarce and carnivores would have quickly found prey in short supply.[34]

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 out,[4] 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.[75]

Whether the extinction occurred gradually or suddenly has been debated, as both views have support from the fossil record. A study of 29 fossil sites in Catalan Pyrenees of Europe in 2010 supports the view that dinosaurs there had great diversity until the asteroid impact, with more than 100 living species.[76] More recent research indicates that this figure is obscured by taphonomic biases and the sparsity of the continental fossil record. The results of this study, which were based on estimated real global biodiversity, showed that between 628 and 1,078 non-avian dinosaur species were alive at the end of the Cretaceous and underwent sudden extinction after the Cretaceous–Paleogene extinction event.[77] 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 approximately 12. Other scientists have made the same assessment following their research.[78]

Several researchers support the existence of Paleocene non-avian dinosaurs. Evidence of this existence is based on the discovery of dinosaur remains in the Hell Creek Formation up to 1.3 m (4 ft 3.2 in) above and 40,000 years later than the K–Pg boundary.[79] Pollen samples recovered near a fossilized hadrosaur femur recovered in the Ojo Alamo Sandstone at the San Juan River in Colorado, 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.[80] The 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).[81]

Choristodere

The choristoderes (semi-aquatic archosauromorphs) survived across the K–Pg boundary[5] but would die out in the early Miocene.[82] Studies on Champsosaurus' palatal teeth suggest that there were dietary changes among the various species across the KT event.[83]

1.10. Mammals

All major Cretaceous mammalian lineages, including monotremes (egg-laying mammals), multituberculates, metatherians, eutherians, dryolestoideans,[84] and gondwanatheres[85] survived the K–Pg extinction event, although they suffered losses. In particular, metatherians largely disappeared from North America, and the Asian deltatheroidans became extinct (aside from the lineage leading to Gurbanodelta).[86] In the Hell Creek beds of North America, at least half of the ten known multituberculate species and all eleven metatherians species are not found above the boundary.[74] Multituberculates in Europe and North America survived relatively unscathed and quickly bounced back in the Paleocene, but Asian forms were devastated, never again to represent a significant component of mammalian fauna.[87] A recent study indicates that metatherians suffered the heaviest losses at the K–T event, followed by multituberculates, while eutherians recovered the quickest.[88]

Mammalian species began diversifying approximately 30 million years prior to the K–Pg boundary. Diversification of mammals stalled across the boundary.[89] 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.[90] 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),[90] although recent research concludes that only marsupial orders diversified soon after the K–Pg boundary.[89]

K–Pg boundary mammalian species were generally small, comparable in size to rats; this small size would have helped them find shelter in protected environments. 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.[34]

2. Evidence

2.1. North American Fossils

Hell Creek Formation

In North American terrestrial sequences, the extinction event is best represented by the marked discrepancy between the rich and relatively abundant late-Maastrichtian pollen record and the post-boundary fern spike.[37]

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. Comparison with the older Judith River Formation (Montana) and Dinosaur Park Formation (Alberta), which both date from approximately 75  Ma, 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.[74]

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,[91] 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 boundary layer contains little pollen and is dominated by fern spores.[92] More usual 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.[93]

2.2. Marine Fossils

The mass extinction of marine plankton appears to have been abrupt and right at the K–Pg boundary.[94] Ammonite genera became extinct at or near the K–Pg boundary; there was a smaller and slower extinction of ammonite genera prior to the boundary 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.[95]

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.[95] The diversity of marine life decreased when the climate near the K–Pg boundary increased in temperature. The temperature increased about three to four degrees very rapidly between 65.4–65.2 million years ago, which is very near the time of the extinction event. Not only did the climate temperature increase, but the water temperature decreased, causing a drastic decrease in marine diversity.[96]

2.3. Megatsunamis

The scientific consensus is that the asteroid impact at the K–Pg boundary left megatsunami deposits and sediments around the area of the Caribbean Sea and Gulf of Mexico, from the colossal waves created by the impact.[97] These deposits have been identified in the La Popa basin in northeastern Mexico,[98] platform carbonates in northeastern Brazil,[99] in Atlantic deep-sea sediments,[100] and in the form of the thickest-known layer of graded sand deposits, around 100 m (330 ft), in the Chicxulub crater itself, directly above the shocked granite ejecta.

The megatsunami has been estimated at more than 100 m (330 ft) tall, as the asteroid fell into relatively shallow seas; in deep seas it would have been 4.6 km (2.9 mi) tall.[101]

2.4. Fossils in Sedimentary Rocks Deposited during the Impact

Fossiliferous sedimentary rocks deposited during the K–Pg impact have been found in the Gulf of Mexico area, including tsunami wash deposits carrying remains of a mangrove-type ecosystem, evidence that after the impact water sloshed back and forth repeatedly in the Gulf of Mexico, and dead fish left in shallow water but not disturbed by scavengers.[102][103][104][105][106]

3. Duration

The rapidity of the extinction is a controversial issue, because some theories about the extinction's causes imply a rapid extinction over a relatively short period (from a few years to a few thousand years) while others imply 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.[107] Scientists have also found very few continuous beds of fossil-bearing rock that cover a time range from several million years before the K–Pg extinction to a few million years after it.[5] The sedimentation rate and thickness of K–Pg clay from three sites suggest rapid extinction, perhaps less than 10,000 years.[108] At one site in the Denver Basin of Colorado, the 'fern spike' lasted about 1,000 years (no more than 71 thousand years); the earliest Cenozoic mammals appeared about 185,000 years (no more than 570,000 years) after the K–Pg boundary layer was deposited.[109]

4. Chicxulub Impact

4.1. Evidence for Impact

Location of Chicxulub crater, Mexico

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 which mostly sank along with iron 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.[110] There were earlier speculations on the possibility of an impact event, but this was the first hard evidence.[111]

The K–Pg 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.

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.[112] Shocked quartz[113] and other minerals were also identified in the K–Pg boundary.[114][115] The identification of giant tsunami beds along the Gulf Coast and the Caribbean provided more evidence,[116] 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.[3]

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, as the source of the K–Pg boundary clay. Identified in 1990[117] based on work by geophysicist Glen Penfield in 1978, the crater is oval, with an average diameter of roughly 180 km (110 mi), about the size calculated by the Alvarez team.[118] The discovery of the crater—a prediction of the impact hypothesis—provided conclusive evidence for a K–Pg impact, and strengthened the hypothesis that it caused the extinction.

In a 2013 paper, Paul Renne of the Berkeley Geochronology Center dated the impact at 66.043±0.011 million years ago, based on argon–argon dating. He further posits that the mass extinction occurred within 32,000 years of this date.[119][120]

In 2007, it was proposed that the impactor belonged to the Baptistina family of asteroids.[121] This link has been doubted, though not disproved, in part because of a lack of observations of the asteroid and its family.[122] It was reported in 2009 that 298 Baptistina does not share the chemical signature of the K–Pg impactor.[123] Further, a 2011 Wide-field Infrared Survey Explorer (WISE) study of reflected light from the asteroids of the family estimated their break-up at 80 Ma, giving them insufficient time to shift orbits and impact Earth by 66 Ma.[124]

4.2. Effects of Impact

In March 2010, an international panel of 41 scientists reviewed 20 years of scientific literature and endorsed the asteroid hypothesis, specifically the Chicxulub impact, as the cause of the extinction, ruling out other theories such as massive volcanism. They had determined that a 10-to-15-kilometer (6 to 9 mi) asteroid hurtled into Earth at Chicxulub on Mexico's Yucatán Peninsula. The collision would have released the same energy as 100 teratonnes of TNT (420 zettajoules)—more than a billion times the energy of the atomic bombings of Hiroshima and Nagasaki.[125]

The Chicxulub impact caused a global catastrophe. Some of the phenomena were brief occurrences immediately following the impact, but there were also long-term geochemical and climatic disruptions that devastated the ecology.

The re-entry of ejecta into Earth's atmosphere would include a brief (hours-long) but intense pulse of infrared radiation, cooking exposed organisms.[34] This is debated, with opponents arguing that local ferocious fires, probably limited to North America, fall short of global firestorms. This is the "Cretaceous–Paleogene firestorm debate". A paper in 2013 by a prominent modeler of nuclear winter suggested that, based on the amount of soot in the global debris layer, the entire terrestrial biosphere might have burned, implying a global soot-cloud blocking out the sun and creating an impact winter effect.[126]

Aside from the hypothesized fire and/or impact winter effects, the impact would have created a dust cloud that blocked sunlight for up to a year, inhibiting photosynthesis.[94] The asteroid hit an area of carbonate rock containing a large amount of combustible hydrocarbons and sulphur,[127] much of which was vaporized, thereby injecting sulfuric acid aerosols into the stratosphere, which might have reduced sunlight reaching the Earth's surface by more than 50%, and would have caused acid rain.[94][128] The resulting acidification of the oceans would kill many organisms that grow shells of calcium carbonate. At Brazos section, the sea surface temperature dropped as much as 7 °C (13 °F) for decades after the impact.[129] It would take at least ten years for such aerosols to dissipate, and would account for the extinction of plants and phytoplankton, and subsequently herbivores and their predators. Creatures whose food chains were based on detritus would have a reasonable chance of survival.[75][94] Freezing temperatures probably lasted for at least three years.[130]

If widespread fires occurred, they would have increased the CO2 content of the atmosphere and caused a temporary greenhouse effect once the dust clouds and aerosol settled; this would have exterminated the most vulnerable organisms that survived the period immediately after the impact.[131]

Most paleontologists now agree that an asteroid did hit the Earth at approximately the end of the Cretaceous, but there was still an ongoing dispute for some time on whether the impact was the sole cause of the extinctions.[18][132]

Several studies in 2020, like Hull et al.[133][134] and Chiarenza et al.[135][136] show quantitatively that the Cretaceous–Paleogene Mass Extinction about 66 million years ago was mostly a result of a meteorite impact (the Chicxulub impactor) and not a result of volcanism.[133][134]

The river bed at the Moody Creek Mine, 7 Mile Creek / Waimatuku, Dunollie, New Zealand contains evidence of a devastating event on terrestrial plant communities at the Cretaceous–Paleogene boundary, confirming the severity and global nature of the event.[37]

4.3. 2016 Chicxulub Crater Drilling Project

In 2016, a scientific drilling project obtained deep rock-core samples from the peak ring around the Chicxulub impact crater. The discoveries confirmed that the rock comprising the peak ring had been shocked by immense pressure and melted in just minutes from its usual state into its present form. Unlike sea-floor deposits, the peak ring was made of granite originating much deeper in the earth, which had been ejected to the surface by the impact. Gypsum is a sulfate-containing rock usually present in the shallow seabed of the region; it had been almost entirely removed, vaporized into the atmosphere. Further, the event was immediately followed by a megatsunami[137] sufficient to lay down the largest known layer of sand separated by grain size directly above the peak ring.

These findings strongly support the impact's role in the extinction event. The impactor was large enough to create a 190-kilometer-wide (120 mi) peak ring, to melt, shock, and eject deep granite, to create colossal water movements, and to eject an immense quantity of vaporized rock and sulfates into the atmosphere, where they would have persisted for several years. This worldwide dispersal of dust and sulfates would have affected climate catastrophically, led to large temperature drops, and devastated the food chain.[138][139]

5. Alternative Hypotheses

Although the concurrence of the end-Cretaceous extinctions with the Chicxulub asteroid impact strongly supports the impact hypothesis, some scientists continue to support other contributing causes: volcanic eruptions, climate change, sea level change, and other impact events. The end-Cretaceous event is the only mass extinction known to be associated with an impact, and other large impacts, such as the Manicouagan Reservoir impact, do not coincide with any noticeable extinction events.[140]

5.1. 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 Mya and lasted more than 2 million years. The most recent evidence shows that the traps erupted over a period of only 800,000 years spanning the K–Pg boundary, and therefore may be responsible for the extinction and the delayed biotic recovery thereafter.[141]

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 that increased the greenhouse effect when the dust and aerosols cleared from the atmosphere.[142][143]

In the years when the Deccan Traps hypothesis was linked to a slower extinction, Luis Alvarez (d. 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. Even Walter Alvarez acknowledged that other major changes may have contributed to the extinctions.[144]

Combining these theories, some geophysical models suggest that the impact contributed to the Deccan Traps. These models, combined with high-precision radiometric dating, suggest that the Chicxulub impact could have triggered some of the largest Deccan eruptions, as well as eruptions at active volcanoes anywhere on Earth.[145][146]

5.2. Multiple Impact Event

Other crater-like topographic features have also been proposed as impact craters formed in connection with Cretaceous–Paleogene extinction. 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 in the North Sea (59.5±14.5 Ma) possibly formed by bolide impact, 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 the northward tectonic drift of Africa and India.[147][148][149][150]

5.3. 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 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, a drop in sea level. There is no direct evidence for the cause of the regression, but the currently accepted explanation is that the mid-ocean ridges became less active and sank under their own weight.[5][151]

A severe regression would have greatly reduced the continental shelf area, the most species-rich part of the sea, and therefore could have been enough to cause a marine mass extinction, but this change would not have caused the extinction of the ammonites. The regression would also have caused climate changes, partly by disrupting winds and ocean currents and partly by reducing the Earth's albedo and increasing global temperatures.[95]

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.[74]

5.4. Multiple Causes

Proponents of multiple causation view the suggested single causes as either too small to produce the vast scale of the extinction, or not likely to produce its observed taxonomic pattern.[74] 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.

Recent work led by Sierra Peterson at Seymour Island, Antarctica, showed two separate extinction events near the Cretaceous–Paleogene boundary, with one correlating to Deccan Trap volcanism and one correlated with the Chicxulub impact.[152] The team analyzed combined extinction patterns using a new clumped isotope temperature record from a hiatus-free, expanded K–Pg boundary section. They documented a 7.8±3.3 °C warming synchronous with the onset of Deccan Traps volcanism and a second, smaller warming at the time of meteorite impact. They suggest local warming may have been amplified due to simultaneous disappearance of continental or sea ice. Intra-shell variability indicates a possible reduction in seasonality after Deccan eruptions began, continuing through the meteorite event. Species extinction at Seymour Island occurred in two pulses that coincide with the two observed warming events, directly linking the end-Cretaceous extinction at this site to both volcanic and meteorite events via climate change.[152]

6. Recovery and Radiation

An artist's rendering of Thescelosaurus shortly after the K–Pg mass extinction. It survived by burrowing, but would soon die of starvation.

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.[153] 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. Also significant, within the mammalian genera, new species were approximately 9.1% larger after the K–Pg boundary.[154]

Other groups also underwent major radiations. Based on molecular sequencing and fossil dating, Neoaves appeared to radiate after the K–Pg boundary.[71][155] 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.[156] On land, giant boid and enormous madtsoiid snakes appeared, and in the seas, giant sea snakes radiated. Teleost fish diversified explosively,[157] 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 appear to have risen in importance.[158]

References

  1. Jablonski, D.; Chaloner, W. G. (1994). "Extinctions in the fossil record (and discussion)". Philosophical Transactions of the Royal Society of London B 344 (1307): 11–17. doi:10.1098/rstb.1994.0045.  https://dx.doi.org/10.1098%2Frstb.1994.0045
  2. Weishampel, D. B.; Barrett, P. M. (2004). "Dinosaur distribution". The Dinosauria (2nd ed.). Berkeley, CA: University of California Press. pp. 517–606. OCLC 441742117. https://archive.org/details/dinosauriandedit00weis. 
  3. Nichols, D. J.; Johnson, K. R. (2008). Plants and the K–T Boundary. Cambridge, England: Cambridge University Press.  https://www.wikipedia.org/wiki/Cambridge%20University%20Press
  4. 2.0.CO;2. ISSN 0094-8373.  https://dx.doi.org/10.1666%2F0094-8373%282004%29030%3C0347%3ALPEATE%3E2.0.CO%3B2" id="ref_4">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. doi:10.1666/0094-8373(2004)030<0347:LPEATE>2.0.CO;2. ISSN 0094-8373.  https://dx.doi.org/10.1666%2F0094-8373%282004%29030%3C0347%3ALPEATE%3E2.0.CO%3B2
  5. MacLeod, N.; Rawson, P.F.; Forey, P.L.; Banner, F.T.; Boudagher-Fadel, M.K.; Bown, P.R.; Burnett, J.A.; Chambers, P. et al. (1997). "The Cretaceous–Tertiary biotic transition". Journal of the Geological Society 154 (2): 265–292. doi:10.1144/gsjgs.154.2.0265. Bibcode: 1997JGSoc.154..265M. http://jgs.lyellcollection.org/content/154/2/265.short. Retrieved 2012-12-23. 
  6. 2.0.CO;2. ISSN 0091-7613. Bibcode: 1986Geo....14..868S. http://geology.geoscienceworld.org/cgi/content/abstract/14/10/868. Retrieved 2007-07-04. " id="ref_6">"Detritus feeding as a buffer to extinction at the end of the Cretaceous". Geology 14 (10): 868–870. 1986. doi:10.1130/0091-7613(1986)14<868:DFAABT>2.0.CO;2. ISSN 0091-7613. Bibcode: 1986Geo....14..868S. http://geology.geoscienceworld.org/cgi/content/abstract/14/10/868. Retrieved 2007-07-04. 
  7. Aberhan, M.; Weidemeyer, S.; Kieesling, W.; Scasso, R.A.; Medina, F.A. (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. Bibcode: 2007Geo....35..227A.  https://dx.doi.org/10.1130%2FG23197A.1
  8. 2.3.CO;2. Bibcode: 1992Geo....20..556S. http://www.geoscienceworld.org/cgi/georef/1992034409. Retrieved 2007-06-22. " id="ref_8">Sheehan, Peter M.; Fastovsky, D.E. (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. Bibcode: 1992Geo....20..556S. http://www.geoscienceworld.org/cgi/georef/1992034409. Retrieved 2007-06-22. 
  9. 2.0.CO;2. ISSN 0883-1351. Bibcode: 2004Palai..19...96K. http://palaios.geoscienceworld.org/cgi/reprint/19/1/96. Retrieved 2007-06-17. " id="ref_9">Kauffman, E. (2004). "Mosasaur predation on upper Cretaceous nautiloids and ammonites from the United States Pacific Coast". PALAIOS 19 (1): 96–100. doi:10.1669/0883-1351(2004)019<0096:MPOUCN>2.0.CO;2. ISSN 0883-1351. Bibcode: 2004Palai..19...96K. http://palaios.geoscienceworld.org/cgi/reprint/19/1/96. Retrieved 2007-06-17. 
  10. 2.3.CO;2. Bibcode: 1996Geo....24..255P. http://geology.geoscienceworld.org/cgi/content/abstract/24/3/255. Retrieved 2007-08-02. " id="ref_10">Pospichal, J.J. (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. Bibcode: 1996Geo....24..255P. http://geology.geoscienceworld.org/cgi/content/abstract/24/3/255. Retrieved 2007-08-02. 
  11. Bown, P (2005). "Selective calcareous nannoplankton survivorship at the Cretaceous–Tertiary boundary". Geology 33 (8): 653–656. doi:10.1130/G21566.1. Bibcode: 2005Geo....33..653B. http://geology.geoscienceworld.org/cgi/content/abstract/33/8/653. Retrieved 2007-08-02. 
  12. 2.0.CO;2. ISSN 0094-8373. http://paleobiol.geoscienceworld.org/cgi/content/abstract/30/4/522. Retrieved 2007-06-23. " id="ref_12">Bambach, R.K.; Knoll, A.H.; Wang, S.C. (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. http://paleobiol.geoscienceworld.org/cgi/content/abstract/30/4/522. Retrieved 2007-06-23. 
  13. Gedl, P. (2004). "Dinoflagellate cyst record of the deep-sea Cretaceous-Tertiary boundary at Uzgru, Carpathian Mountains, Czech Republic". Special Publications of the Geological Society of London 230 (1): 257–273. doi:10.1144/GSL.SP.2004.230.01.13. Bibcode: 2004GSLSP.230..257G.  https://dx.doi.org/10.1144%2FGSL.SP.2004.230.01.13
  14. MacLeod, N. (1998). "Impacts and marine invertebrate extinctions". Special Publications of the Geological Society of London 140 (1): 217–246. doi:10.1144/GSL.SP.1998.140.01.16. Bibcode: 1998GSLSP.140..217M. http://sp.lyellcollection.org/cgi/content/abstract/140/1/217. Retrieved 2007-08-02. 
  15. Courtillot, V (1999). Evolutionary Catastrophes: The science of mass extinction. Cambridge, UK: Cambridge University Press. p. 2. ISBN 978-0-521-58392-3. https://books.google.com/books?id=qiegJbafYkUC&pg=PA23&lpg=PA23. 
  16. Arenillas, I; Arz, J.A.; Molina, E.; 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. 
  17. MacLeod, N (1996). Cretaceous–Tertiary Mass Extinctions: Biotic and environmental changes. W.W. Norton. pp. 85–138. ISBN 978-0-393-96657-2. 
  18. Keller, G.; Adatte, T.; Stinnesbeck, W.; Rebolledo-Vieyra, _; Fucugauchi, J.U.; Kramar, U.; Stüben, D. (2004). "Chicxulub impact predates the K–T boundary mass extinction". Proceedings of the National Academy of Sciences (Washington, DC) 101 (11): 3753–3758. doi:10.1073/pnas.0400396101. PMID 15004276. Bibcode: 2004PNAS..101.3753K.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=374316
  19. "Deep-sea benthic foraminiferal recolonisation following a volcaniclastic event in the lower Campanian of the Scaglia Rossa Formation (Umbria-Marche Basin, central Italy)". Marine Micropaleontology 44 (1–2): 57–76. 2002. doi:10.1016/s0377-8398(01)00037-8. Bibcode: 2002MarMP..44...57G. http://www.es.ucl.ac.uk/people/m-kaminski/reprints-pdfs/Galeotti_etal2002.pdf. Retrieved 2007-08-19. 
  20. Kuhnt, W.; Collins, E.S. (1996). "8. Cretaceous to Paleogene benthic foraminifers from the Iberia abyssal plain". Proceedings of the Ocean Drilling Program, Scientific Results. Proceedings of the Ocean Drilling Program 149: 203–216. doi:10.2973/odp.proc.sr.149.254.1996. http://www-odp.tamu.edu/publications/149_SR/VOLUME/CHAPTERS/SR149_08.PDF. Retrieved 2007-08-19. 
  21. Coles, G.P.; Ayress, M.A.; Whatley, R.C. (1990). "A comparison of North Atlantic and 20 Pacific deep-sea Ostracoda". Ostracoda and Global Events. Chapman & Hall. pp. 287–305. ISBN 978-0-442-31167-4. 
  22. Brouwers, E.M.; 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. Bibcode: 1993Palai...8..140B.  https://dx.doi.org/10.2307%2F3515168
  23. 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.  https://dx.doi.org/10.1007%2FBF02536880
  24. Rosen, B R; Turnšek, D (1989). "Extinction patterns and biogeography of scleractinian corals across the Cretaceous/Tertiary boundary". Memoir of the Association of Australasian Paleontology. Proceedings of the Fifth International Symposium on Fossil Cnidaria including Archaeocyatha and Spongiomorphs (Brisbane, Queensland) (8): 355–370. 
  25. 2.3.CO;2. Bibcode: 1991Geo....19.1181W. http://geology.geoscienceworld.org/cgi/content/abstract/19/12/1181. Retrieved 2007-08-02. " id="ref_25">Ward, P.D.; Kennedy, W.J.; MacLeod, K.G.; Mount, J.F. (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. Bibcode: 1991Geo....19.1181W. http://geology.geoscienceworld.org/cgi/content/abstract/19/12/1181. Retrieved 2007-08-02. 
  26. 2.0.CO;2. ISSN 0091-7613. Bibcode: 2002Geo....30..954H.  https://dx.doi.org/10.1130%2F0091-7613%282002%29030%3C0955%3AMCTBSI%3E2.0.CO%3B2" id="ref_26">"Marine Cretaceous-Tertiary boundary section in southwestern South Dakota: Comment and reply". Geology 30 (10): 954–955. 2002. doi:10.1130/0091-7613(2002)030<0955:MCTBSI>2.0.CO;2. ISSN 0091-7613. Bibcode: 2002Geo....30..954H.  https://dx.doi.org/10.1130%2F0091-7613%282002%29030%3C0955%3AMCTBSI%3E2.0.CO%3B2
  27. 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. 
  28. "Geography of end-Cretaceous marine bivalve extinctions". Science 260 (5110): 971–973. 1993. doi:10.1126/science.11537491. PMID 11537491. Bibcode: 1993Sci...260..971R.  https://dx.doi.org/10.1126%2Fscience.11537491
  29. 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. doi:10.1017/S0022336000026652.  https://dx.doi.org/10.1017%2FS0022336000026652
  30. Kriwet, Jürgen; Benton, Michael J. (2004). "Neoselachian (Chondrichthyes, Elasmobranchii) Diversity across the Cretaceous–Tertiary Boundary". Palaeogeography, Palaeoclimatology, Palaeoecology 214 (3): 181–194. doi:10.1016/j.palaeo.2004.02.049. Bibcode: 2004PPP...214..181K.  https://dx.doi.org/10.1016%2Fj.palaeo.2004.02.049
  31. Patterson, C. (1993). "Osteichthyes: Teleostei". in Benton, M.J.. The Fossil Record. 2. Springer. pp. 621–656. ISBN 978-0-412-39380-8. 
  32. Noubhani, Abdelmajid (2010). "The Selachians' faunas of the Moroccan phosphate deposits and the K-T mass extinctions". Historical Biology 22 (1–3): 71–77. doi:10.1080/08912961003707349.  https://dx.doi.org/10.1080%2F08912961003707349
  33. Zinsmeister, W.J. (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. doi:10.1017/S0022336000024331. 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. 
  34. Robertson, D.S.; McKenna, M.C.; Toon, O.B.; Hope, S.; Lillegraven, J.A. (2004). "Survival in the first hours of the Cenozoic". GSA Bulletin 116 (5–6): 760–768. doi:10.1130/B25402.1. Bibcode: 2004GSAB..116..760R. http://uahost.uantwerpen.be/funmorph/raoul/macroevolutie/robertson2004.pdf. Retrieved 2016-01-06. 
  35. Labandeira, Conrad C.; Johnson, Kirk R.; Wilf, Peter (2002). "Impact of the terminal Cretaceous event on plant–insect associations". 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. Bibcode: 2002PNAS...99.2061L. http://www.geosc.psu.edu/~pwilf/LabandeiraJohnsonWilf%202002PNAS.pdf. Retrieved 2007-07-07. 
  36. Wilf, P.; Labandeira, C.C.; Johnson, K.R.; 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. Bibcode: 2006Sci...313.1112W.  https://dx.doi.org/10.1126%2Fscience.1129569
  37. 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. Bibcode: 2001Sci...294.1700V. http://www.sciencemag.org/cgi/content/abstract/294/5547/1700. Retrieved 2007-07-05. 
  38. 2.0.co;2.  https://dx.doi.org/10.1666%2F0094-8373%282004%29030%3C0347%3Alpeate%3E2.0.co%3B2" id="ref_38">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. doi:10.1666/0094-8373(2004)030<0347:lpeate>2.0.co;2.  https://dx.doi.org/10.1666%2F0094-8373%282004%29030%3C0347%3Alpeate%3E2.0.co%3B2
  39. Johnson, K.R.; Hickey, L.J. (1991). Global Catastrophes in Earth History: An interdisciplinary conference on impacts, volcanism, and mass mortality. Geological Society of America. ISBN 978-0-8137-2247-4. 
  40. Askin, R.A.; Jacobson, S.R. (1996). Cretaceous–Tertiary Mass Extinctions: Biotic and Environmental Changes. W W Norton. ISBN 978-0-393-96657-2. 
  41. 2.3.CO;2. Bibcode: 1996Geo....24..963S. http://geology.geoscienceworld.org/cgi/content/abstract/24/11/963. Retrieved 2007-07-05. " id="ref_41">Schultz, P.H.; 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. Bibcode: 1996Geo....24..963S. http://geology.geoscienceworld.org/cgi/content/abstract/24/11/963. Retrieved 2007-07-05. 
  42. Vajda, V.; McLoughlin, S. (2004). "Fungal proliferation at the Cretaceous–Tertiary boundary". 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. 
  43. "How did dino-era birds survive the asteroid 'apocalypse'?". May 24, 2018. https://news.nationalgeographic.com/2018/05/dinosaurs-asteroid-birds-forests-fires-paleontology-science/. Retrieved October 5, 2018. 
  44. 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. doi:10.1073/pnas.0900906106. ISSN 0027-8424. PMID 19325131. Bibcode: 2009PNAS..106.5737F.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=2667025
  45. Fungal Proliferation at the Cretaceous-Tertiary Boundary https://science.sciencemag.org/content/303/5663/1489/
  46. The Terminal Paleozoic Fungal Event: Evidence of Terrestrial Ecosystem Destabilization and Collapse https://pubmed.ncbi.nlm.nih.gov/11607638/
  47. Archibald, J.D.; Bryant, L.J. (1990). "Differential Cretaceous–Tertiary extinction of nonmarine vertebrates; evidence from northeastern Montana". Global Catastrophes in Earth History: an Interdisciplinary Conference on Impacts, Volcanism, and Mass Mortality. Special Paper. 247. Geological Society of America. pp. 549–562. doi:10.1130/spe247-p549. ISBN 978-0-8137-2247-4.  https://dx.doi.org/10.1130%2Fspe247-p549
  48. Estes, R. (1964). "Fossil vertebrates from the late Cretaceous Lance formation, eastern Wyoming". University of California Publications, Department of Geological Sciences 49: 1–180. 
  49. Gardner, J. D. (2000). "Albanerpetontid amphibians from the upper Cretaceous (Campanian and Maastrichtian) of North America". Geodiversitas 22 (3): 349–388. 
  50. 2.3.co;2. Bibcode: 1992Geo....20..556S.  https://dx.doi.org/10.1130%2F0091-7613%281992%29020%3C0556%3Ameoldv%3E2.3.co%3B2" id="ref_50">Sheehan, P. M.; Fastovsky, D. E. (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. Bibcode: 1992Geo....20..556S.  https://dx.doi.org/10.1130%2F0091-7613%281992%29020%3C0556%3Ameoldv%3E2.3.co%3B2
  51. Novacek, M J (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.  https://dx.doi.org/10.2307%2F2666178
  52. Apesteguía, Sebastián; Novas, Fernando E (2003). "Large Cretaceous sphenodontian from Patagonia provides insight into lepidosaur evolution in Gondwana". Nature 425 (6958): 609–612. doi:10.1038/nature01995. PMID 14534584. Bibcode: 2003Natur.425..609A.  https://dx.doi.org/10.1038%2Fnature01995
  53. Lutz, D. (2005). Tuatara: A living fossil. DIMI Press. ISBN 978-0-931625-43-5. 
  54. Longrich, Nicholas R.; Bhullar, Bhart-Anjan S.; Gauthier, Jacques A. (2012). "Mass extinction of lizards and snakes at the Cretaceous–Paleogene boundary". Proceedings of the National Academy of Sciences of the United States of America 109 (52): 21396–21401. doi:10.1073/pnas.1211526110. PMID 23236177. PMC 3535637. Bibcode: 2012PNAS..10921396L. http://www.pnas.org/content/early/2012/12/07/1211526110.abstract. Retrieved 11 December 2012. 
  55. Chatterjee, S.; Small, B.J. (1989). "New plesiosaurs from the Upper Cretaceous of Antarctica". Geological Society of London. Special Publications 47 (1): 197–215. doi:10.1144/GSL.SP.1989.047.01.15. Bibcode: 1989GSLSP..47..197C. http://sp.lyellcollection.org/cgi/content/abstract/47/1/197. Retrieved 2007-07-04. 
  56. O'Keefe, F.R. (2001). "A cladistic analysis and taxonomic revision of the Plesiosauria (Reptilia: Sauropterygia)". Acta Zoologica Fennica 213: 1–63. 
  57. "The Great Archosaur Lineage". University of California Museum of Paleontology. http://www.ucmp.berkeley.edu/diapsids/archosauria.html. Retrieved 2014-12-18. 
  58. Brochu, C.A. (2004). "Calibration age and quartet divergence date estimation". Evolution 58 (6): 1375–1382. doi:10.1554/03-509. PMID 15266985.  https://dx.doi.org/10.1554%2F03-509
  59. Jouve, S.; Bardet, N.; Jalil, N-E; Suberbiola, X P; 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:TOACPP2.0.CO;2]. ISSN 0272-4634.  https://dx.doi.org/10.1671%2F0272-4634%282008%2928%5B409%3ATOACPP%5D2.0.CO%3B2
  60. Company, J.; Ruiz-Omeñaca, J. I.; Pereda Suberbiola, X. (1999). "A long-necked pterosaur (Pterodactyloidea, Azhdarchidae) from the upper Cretaceous of Valencia, Spain". Geologie en Mijnbouw 78 (3): 319–333. doi:10.1023/A:1003851316054.  https://dx.doi.org/10.1023%2FA%3A1003851316054
  61. Barrett, P. M.; Butler, R. J.; Edwards, N. P.; Milner, A. R. (2008). "Pterosaur distribution in time and space: an atlas". Zitteliana 28: 61–107. http://epub.ub.uni-muenchen.de/12007/1/zitteliana_2008_b28_05.pdf. Retrieved 2015-08-31. 
  62. Slack, K, E; Jones, C M; Ando, T; Harrison, G L; Fordyce, R E; 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.  https://dx.doi.org/10.1093%2Fmolbev%2Fmsj124
  63. Penny, D.; Phillips, M.J. (2004). "The rise of birds and mammals: Are microevolutionary processes sufficient for macroevolution?". Trends in Ecology and Evolution 19 (10): 516–522. doi:10.1016/j.tree.2004.07.015. PMID 16701316.  https://dx.doi.org/10.1016%2Fj.tree.2004.07.015
  64. Butler, Richard J.; Barrett, Paul M.; Nowbath, Stephen; Upchurch, Paul (2009). "Estimating the effects of sampling biases on pterosaur diversity patterns: Implications for hypotheses of bird / pterosaur competitive replacement". Paleobiology 35 (3): 432–446. doi:10.1666/0094-8373-35.3.432.  https://dx.doi.org/10.1666%2F0094-8373-35.3.432
  66. Longrich, N. R.; Martill, D. M.; Andres, B. (2018). "Late Maastrichtian pterosaurs from North Africa and mass extinction of Pterosauria at the Cretaceous-Paleogene boundary". PLOS Biology 16 (3): e2001663. doi:10.1371/journal.pbio.2001663. PMID 29534059.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=5849296
  67. 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. Bibcode: 1996Sci...274.1164H.  https://dx.doi.org/10.1126%2Fscience.274.5290.1164
  68. Clarke, J.A.; Tambussi, C.P.; Noriega, J.I.; Erickson, G.M.; Ketcham, R.A. (2005). "Definitive fossil evidence for the extant avian radiation in the Cretaceous". Nature 433 (7023): 305–308. doi:10.1038/nature03150. PMID 15662422. Bibcode: 2005Natur.433..305C.  https://dx.doi.org/10.1038%2Fnature03150
  69. 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. doi:10.1073/pnas.1110395108. PMID 21914849. Bibcode: 2011PNAS..10815253L.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=3174646
  70. "Primitive birds shared dinosaurs' fate". Science Daily. 20 September 2011. https://www.sciencedaily.com/releases/2011/09/110919151315.htm. Retrieved 20 September 2011. 
  71. Feduccia, Alan (1995). "Explosive evolution in Tertiary birds and mammals". Science 267 (5198): 637–638. doi:10.1126/science.267.5198.637. PMID 17745839. Bibcode: 1995Sci...267..637F.  https://dx.doi.org/10.1126%2Fscience.267.5198.637
  72. Mitchell, K.J.; Llamas, B.; Soubrier, J.; Rawlence, N.J.; Worthy, T.H.; Wood, J.; Lee, M.S.Y.; Cooper, A. (2014). "Ancient DNA reveals elephant birds and kiwi are sister taxa and clarifies ratite bird evolution". Science 344 (6186): 989–900. doi:10.1126/science.1251981. PMID 24855267. Bibcode: 2014Sci...344..898M.  https://dx.doi.org/10.1126%2Fscience.1251981
  73. Yonezawa, Takahiro; Segawa, Takahiro; Mori, Hiroshi; Campos, Paula F.; Hongoh, Yuichi; Endo, Hideki; Akiyoshi, Ayumi; Kohno, Naoki et al. (2017). "Phylogenomics and Morphology of Extinct Paleognaths Reveal the Origin and Evolution of the Ratites". Current Biology 27 (1): 68–77. doi:10.1016/j.cub.2016.10.029. ISSN 0960-9822. PMID 27989673.  https://dx.doi.org/10.1016%2Fj.cub.2016.10.029
  74. David, Archibald; Fastovsky, David (2004). "Dinosaur extinction". in Weishampel, David B.. The Dinosauria (2nd ed.). Berkeley: University of California Press. pp. 672–684. ISBN 978-0-520-24209-8. http://www.bio.sdsu.edu/faculty/archibald/ArchFast.pdf. 
  75. 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". Biological Processes Associated with Impact Events. SpringerLink. pp. 197–219. doi:10.1007/3-540-25736-5_9. ISBN 978-3-540-25735-6. https://archive.org/details/biologicalproces00cock. 
  76. 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. Bibcode: 2010PPP...288...82R.  https://dx.doi.org/10.1016%2Fj.palaeo.2010.01.037
  77. le Loeuff, J. (2012). "Paleobiogeography and biodiversity of Late Maastrichtian dinosaurs: How many dinosaur species became extinct at the Cretaceous-Tertiary boundary?". Bulletin de la Société Géologique de France 183 (6): 547–559. doi:10.2113/gssgfbull.183.6.547.  https://dx.doi.org/10.2113%2Fgssgfbull.183.6.547
  78. 2.0.co;2. Bibcode: 2001Palai..16..482R. Archived from the original on 2006-11-10. https://web.archive.org/web/20061110232442/http://www.biology.ualberta.ca/faculty/philip_currie/uploads/pdfs/2001/2001Centrosaurus.pdf. " id="ref_78">Ryan, M.J.; Russell, A.P.; Eberth, D.A.; Currie, P.J. (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 (5): 482–506. doi:10.1669/0883-1351(2001)016<0482:ttoaco>2.0.co;2. Bibcode: 2001Palai..16..482R. Archived from the original on 2006-11-10. https://web.archive.org/web/20061110232442/http://www.biology.ualberta.ca/faculty/philip_currie/uploads/pdfs/2001/2001Centrosaurus.pdf. 
  79. Sloan, R.E.; Rigby, K.; van Valen, L.M.; 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. Bibcode: 1986Sci...232..629S. http://www.sciencemag.org/cgi/content/abstract/232/4750/629. Retrieved 2007-05-18. 
  80. Fassett, J.E.; Lucas, S.G.; Zielinski, R.A.; Budahn, J.R. (2001). "Compelling new evidence for Paleocene dinosaurs in the Ojo Alamo Sandstone San Juan Basin, New Mexico and Colorado, USA". International Conference on Catastrophic Events and Mass Extinctions: Impacts and Beyond, 9–12 July 2000. 1053. Vienna, Austria. pp. 45–46. Bibcode: 2001caev.conf.3139F. http://www.lpi.usra.edu/meetings/impact2000/pdf/3139.pdf. Retrieved 2007-05-18. 
  81. Sullivan, R.M. (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. 
  82. Evans, Susan E.; Klembara, Jozef (2005). "A choristoderan reptile (Reptilia: Diapsida) from the Lower Miocene of northwest Bohemia (Czech Republic)". Journal of Vertebrate Paleontology 25 (1): 171–184. doi:10.1671/0272-4634(2005)025[0171:ACRRDF2.0.CO;2]. ISSN 0272-4634.  https://dx.doi.org/10.1671%2F0272-4634%282005%29025%5B0171%3AACRRDF%5D2.0.CO%3B2
  83. Matsumoto, Ryoko; Evans, Susan E. (November 2015). "Morphology and function of the palatal dentition in Choristodera". Journal of Anatomy 228 (3): 414–429. doi:10.1111/joa.12414. PMID 26573112. PMC 5341546. http://discovery.ucl.ac.uk/1471979/1/Matsumoto%20and%20Evans%20%20choristoderan%20palatal%20dentition.pdf. Retrieved 2018-08-06. 
  84. Gelfo, J.N.; Pascual, R. (2001). "Peligrotherium tropicalis (Mammalia, Dryolestida) from the early Paleocene of Patagonia, a survival from a Mesozoic Gondwanan radiation". Geodiversitas 23: 369–379. Archived from the original on 2012-02-12. https://web.archive.org/web/20120212193611/http://www.mnhn.fr/publication/geodiv/g01n3a4.pdf. 
  85. Goin, F.J.; Reguero, M.A.; Pascual, R.; von Koenigswald, W.; Woodburne, M.O.; Case, J.A.; Marenssi, S.A.; Vieytes, C. et al. (2006). "First gondwanatherian mammal from Antarctica". Geological Society, London. Special Publications 258 (1): 135–144. doi:10.1144/GSL.SP.2006.258.01.10. Bibcode: 2006GSLSP.258..135G.  https://dx.doi.org/10.1144%2FGSL.SP.2006.258.01.10
  86. McKenna, M.C.; Bell, S.K. (1997). Classification of mammals: Above the species level. Columbia University Press. ISBN 978-0-231-11012-9. 
  87. Wood, D. Joseph (2010). The Extinction of the Multituberculates Outside North America: a Global Approach to Testing the Competition Model (M.S.). The Ohio State University. Archived from the original on 2015-04-08. Retrieved 2015-04-03. https://etd.ohiolink.edu/!etd.send_file?accession=osu1275595604&disposition=inline
  88. Pires, Mathias M.; Rankin, Brian D.; Silvestro, Daniele; Quental, Tiago B. (2018). "Diversification dynamics of mammalian clades during the K–Pg mass extinction". Biology Letters 14 (9): 20180458. doi:10.1098/rsbl.2018.0458. PMID 30258031.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=6170748
  89. "The delayed rise of present-day mammals". Nature 446 (7135): 507–512. 2007. doi:10.1038/nature05634. PMID 17392779. Bibcode: 2007Natur.446..507B. http://www.uni-oldenburg.de/molekularesystematik/download/Publications/mammalST.pdf. Retrieved 2008-06-25. 
  90. "Placental mammal diversification and the Cretaceous–Tertiary boundary". PNAS 100 (3): 1056–1061. 2003. doi:10.1073/pnas.0334222100. PMID 12552136. PMC 298725. Bibcode: 2003PNAS..100.1056S. http://www.pnas.org/cgi/reprint/100/3/1056.pdf. Retrieved 2007-07-21. 
  91. Dodson, Peter (1996). The Horned Dinosaurs: A Natural History. Princeton, NJ: Princeton University Press. pp. 279–281. ISBN 978-0-691-05900-6. https://archive.org/details/horneddinosaursn00dods_0. 
  92. "Online guide to the continental Cretaceous–Tertiary boundary in the Raton basin, Colorado and New Mexico". U.S. Geological Survey. 2004. Archived from the original on 2006-09-25. https://web.archive.org/web/20060925223706/http://esp.cr.usgs.gov/info/kt/stop2b.html. Retrieved 2007-07-08. 
  93. Smathers, G A; Mueller-Dombois D (1974). Invasion and Recovery of Vegetation after a Volcanic Eruption in Hawaii. Scientific Monograph. 5. United States National Park Service. http://www.nps.gov/history/history/online_books/science/5/contents.htm. Retrieved 2007-07-09. 
  94. "Meteorite impact and the mass extinction of species at the Cretaceous/Tertiary boundary". PNAS 95 (19): 11028–11029. 1998. doi:10.1073/pnas.95.19.11028. PMID 9736679. Bibcode: 1998PNAS...9511028P.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=33889
  95. "Sudden and Gradual Molluscan Extinctions in the Latest Cretaceous of Western European Tethys". Science 274 (5291): 1360–1363. 1996. doi:10.1126/science.274.5291.1360. PMID 8910273. Bibcode: 1996Sci...274.1360M.  https://dx.doi.org/10.1126%2Fscience.274.5291.1360
  96. Keller, Gerta (July 2001). "The end-cretaceous mass extinction in the marine realm: Year 2000 assessment". Planetary and Space Science 49 (8): 817–830. doi:10.1016/S0032-0633(01)00032-0. Bibcode: 2001P&SS...49..817K.  https://dx.doi.org/10.1016%2FS0032-0633%2801%2900032-0
  97. Bourgeois, J. (2009). "Chapter 3. Geologic effects and records of tsunamis". The Sea (Ideas and Observations on Progress in the Study of the Seas). 15: Tsunamis. Boston, MA: Harvard University. ISBN 978-0-674-03173-9. http://faculty.washington.edu/jbourgeo/BourgeoisTheSeaCh3.pdf. Retrieved 2012-03-29. 
  98. Lawton, T. F.; Shipley, K. W.; Aschoff, J. L.; Giles, K. A.; Vega, F. J. (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. doi:10.1130/G21057.1. Bibcode: 2005Geo....33...81L.  https://dx.doi.org/10.1130%2FG21057.1
  99. Albertão, G. A.; P. P. Martins Jr. (1996). "A possible tsunami deposit at the Cretaceous-Tertiary boundary in Pernambuco, northeastern Brazil". Sed. Geol. 104 (1–4): 189–201. doi:10.1016/0037-0738(95)00128-X. Bibcode: 1996SedG..104..189A.  https://dx.doi.org/10.1016%2F0037-0738%2895%2900128-X
  100. 2.0.CO;2. Bibcode: 2000Geo....28.1119N.  https://dx.doi.org/10.1130%2F0091-7613%282000%2928%3C1119%3AMFOTNA%3E2.0.CO%3B2" id="ref_100">Norris, R. D.; Firth, J.; Blusztajn, J. S.; Ravizza, G. (2000). "Mass failure of the North Atlantic margin triggered by the Cretaceous-Paleogene bolide impact". Geology 28 (12): 1119–1122. doi:10.1130/0091-7613(2000)28<1119:MFOTNA>2.0.CO;2. Bibcode: 2000Geo....28.1119N.  https://dx.doi.org/10.1130%2F0091-7613%282000%2928%3C1119%3AMFOTNA%3E2.0.CO%3B2
  101. Bryant, Edward (June 2014). Tsunami: The Underrated Hazard. Springer. p. 178. ISBN 9783319061337. https://books.google.com/books?id=tOkpBAAAQBAJ&pg=PA178&lpg=PA17. Retrieved 2017-08-30. 
  102. 2.3.CO;2. PMID 11537752. Bibcode: 1992Geo....20...99S.  https://dx.doi.org/10.1130%2F0091-7613%281992%29020%3C0099%3ATBDWCU%3E2.3.CO%3B2" id="ref_102">Smit, Jan; Montanari, Alessandro; H.M., Nicola; Alvarez, Walter; R. Hildebrand, Alan; V. Margolis, Stanley; Claeys, Philippe; Lowrie, William et al. (1992). "Tektite-bearing, deep-water clastic unit at the Cretaceous-Tertiary boundary in northeastern Mexico". Geology 20 (2): 99–103. doi:10.1130/0091-7613(1992)020<0099:TBDWCU>2.3.CO;2. PMID 11537752. Bibcode: 1992Geo....20...99S.  https://dx.doi.org/10.1130%2F0091-7613%281992%29020%3C0099%3ATBDWCU%3E2.3.CO%3B2
  103. Field guide to Cretaceous-tertiary boundary sections in northeastern Mexico. Lunar and Planetary Institute. 1994. https://www.lpi.usra.edu/lpi/contribution_docs/LPI-000827.pdf. Retrieved 2019-06-25. 
  104. Smit, Jan (1999). "missing". Annual Reviews of Earth and Planetary Science 27: 75–113. 
  105. Kring, David A. (2007). "The Chicxulub impact event and its environmental consequences at the Cretaceous-Tertiary boundary". Palaeogeography, Palaeoclimatology, Palaeoecology 255 (1–2): 4–21. doi:10.1016/j.palaeo.2007.02.037.  https://dx.doi.org/10.1016%2Fj.palaeo.2007.02.037
  106. "Chicxulub impact event". https://www.lpi.usra.edu/science/kring/Chicxulub/regional-effects/. Retrieved 2019-06-25. 
  107. Signor, Philip W., III; Lipps, Jere H. (1982). "Sampling bias, gradual extinction patterns, and catastrophes in the fossil record". in Silver, L.T.; Schultz, Peter H.. Geological implications of impacts of large asteroids and comets on the Earth. Special Publication 190. Boulder, Colorado: Geological Society of America. pp. 291–296. ISBN 978-0-8137-2190-3. OCLC 4434434112. https://books.google.com/books?id=efz87W88HawC&pg=291. Retrieved October 25, 2015. 
  108. Mukhopadhyay, Sujoy (2001). "A Short Duration of the Cretaceous-Tertiary Boundary Event: Evidence from Extraterrestrial Helium-3". Science 291 (5510): 1952–1955. doi:10.1126/science.291.5510.1952. PMID 11239153. Bibcode: 2001Sci...291.1952M. https://authors.library.caltech.edu/36545/7/Mukhopad3.sup.pdf. 
  109. Clyde, William C.; Ramezani, Jahandar; Johnson, Kirk R.; Bowring, Samuel A.; Jones, Matthew M. (15 October 2016). "Direct high-precision U–Pb geochronology of the end-Cretaceous extinction and calibration of Paleocene astronomical timescales". Earth and Planetary Science Letters 452: 272–280. doi:10.1016/j.epsl.2016.07.041. Bibcode: 2016E&PSL.452..272C.  https://dx.doi.org/10.1016%2Fj.epsl.2016.07.041
  110. Alvarez, L W; Alvarez, W; Asaro, F; Michel, H V (1980). "Extraterrestrial cause for the Cretaceous–Tertiary extinction". Science 208 (4448): 1095–1108. doi:10.1126/science.208.4448.1095. PMID 17783054. Bibcode: 1980Sci...208.1095A. https://websites.pmc.ucsc.edu/~pkoch/EART_206/09-0305/Alvarez%20et%2080%20Science%20208-1095.pdf. Retrieved 2018-11-24. 
  111. de Laubenfels, M W (1956). "Dinosaur extinction: One more hypothesis". Journal of Paleontology 30 (1): 207–218. 
  112. Smit J.; Klaver, J. (1981). "Sanidine spherules at the Cretaceous-Tertiary boundary indicate a large impact event". Nature 292 (5818): 47–49. doi:10.1038/292047a0. Bibcode: 1981Natur.292...47S.  https://dx.doi.org/10.1038%2F292047a0
  113. Shocked minerals have their internal structure deformed, and are created by intense pressures as in nuclear blasts and meteorite impacts.
  114. Bohor, B. F.; Foord, E. E.; Modreski, P. J.; Triplehorn, D. M. (1984). "Mineralogic evidence for an impact event at the Cretaceous-Tertiary boundary". Science 224 (4651): 867–9. doi:10.1126/science.224.4651.867. PMID 17743194. Bibcode: 1984Sci...224..867B.  https://dx.doi.org/10.1126%2Fscience.224.4651.867
  115. Bohor, B. F.; Modreski, P. J.; Foord, E. E. (1987). "Shocked quartz in the Cretaceous-Tertiary boundary clays: Evidence for a global distribution". Science 236 (4802): 705–709. doi:10.1126/science.236.4802.705. PMID 17748309. Bibcode: 1987Sci...236..705B. https://zenodo.org/record/1230978. 
  116. Bourgeois, J.; Hansen, T. A.; Wiberg, P. A.; Kauffman, E. G. (1988). "A tsunami deposit at the Cretaceous-Tertiary boundary in Texas". Science 241 (4865): 567–570. doi:10.1126/science.241.4865.567. PMID 17774578. Bibcode: 1988Sci...241..567B.  https://dx.doi.org/10.1126%2Fscience.241.4865.567
  117. 2.3.co;2. Bibcode: 1991Geo....19..867H.  https://dx.doi.org/10.1130%2F0091-7613%281991%29019%3C0867%3Accapct%3E2.3.co%3B2" id="ref_117">Hildebrand, A. R.; Penfield, G. T. et al. (1991). "Chicxulub crater: a possible Cretaceous/Tertiary boundary impact crater on the Yucatán peninsula, Mexico". Geology 19 (9): 867–871. doi:10.1130/0091-7613(1991)019<0867:ccapct>2.3.co;2. Bibcode: 1991Geo....19..867H.  https://dx.doi.org/10.1130%2F0091-7613%281991%29019%3C0867%3Accapct%3E2.3.co%3B2
  118. 2.3.CO;2. PMID 11539331. Bibcode: 1996Geo....24..527P.  https://dx.doi.org/10.1130%2F0091-7613%281996%29024%3C0527%3ASEOTCC%3E2.3.CO%3B2" id="ref_118">Pope, K.O.; Ocampo, A.C.; Kinsland, G.L.; Smith, R. (1996). "Surface expression of the Chicxulub crater". Geology 24 (6): 527–530. doi:10.1130/0091-7613(1996)024<0527:SEOTCC>2.3.CO;2. PMID 11539331. Bibcode: 1996Geo....24..527P.  https://dx.doi.org/10.1130%2F0091-7613%281996%29024%3C0527%3ASEOTCC%3E2.3.CO%3B2
  119. Renne, Paul R.; Deino, Alan L.; Hilgen, Frederik J.; Kuiper, Klaudia F.; Mark, Darren F.; Mitchell, William S.; Morgan, Leah E.; Mundil, Roland et al. (7 February 2013). "Time scales of critical events around the Cretaceous-Paleogene boundary". Science 339 (6120): 684–687. doi:10.1126/science.1230492. PMID 23393261. Bibcode: 2013Sci...339..684R. http://www.cugb.edu.cn/uploadCms/file/20600/20131028144132060.pdf. Retrieved 1 December 2017. 
  120. Perlman, David. "Dinosaur extinction battle flares". http://www.sfgate.com/science/article/Dinosaur-extinction-battle-flares-4261978.php. Retrieved 2013-02-08. 
  121. Bottke, W.F.; 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. doi:10.1038/nature06070. PMID 17805288. Bibcode: 2007Natur.449...48B.  https://dx.doi.org/10.1038%2Fnature06070
  122. "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. February 2009. Bibcode: 2009JRASC.103....7M. Archived from the original on 2010-11-29. https://web.archive.org/web/20101129023918/http://rasc.ca/journal/pdfs/2009-02-lr.pdf. 
  123. Reddy, V.; Emery, J.P.; Gaffey, M.J.; Bottke, W.F.; Cramer, A.; Kelley, M.S. (December 2009). "Composition of 298 Baptistina: Implications for the K/T impactor link". Meteoritics & Planetary Science 44 (12): 1917–1927. doi:10.1111/j.1945-5100.2009.tb02001.x. Bibcode: 2009M&PS...44.1917R.  https://dx.doi.org/10.1111%2Fj.1945-5100.2009.tb02001.x
  124. "NASA's WISE raises doubt about asteroid family believed responsible for dinosaur extinction". 20 September 2011. https://www.sciencedaily.com/releases/2011/09/110919144042.htm. Retrieved 21 September 2011. 
  125. Schulte, P. et al. (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. Bibcode: 2010Sci...327.1214S. http://doc.rero.ch/record/210367/files/PAL_E4389.pdf. Retrieved 6 August 2018. 
  126. 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 118 (1): 329–336. doi:10.1002/jgrg.20018. Bibcode: 2013JGRG..118..329R.  https://dx.doi.org/10.1002%2Fjgrg.20018
  127. Kaiho, Kunio; Oshima, Naga (2017). "Site of asteroid impact changed the history of life on Earth: The low probability of mass extinction". Scientific Reports 7 (1): Article number 14855. doi:10.1038/s41598-017-14199-x. PMID 29123110. Bibcode: 2017NatSR...714855K.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=5680197
  128. Ohno, S. (2014). "Production of sulphate-rich vapour during the Chicxulub impact and implications for ocean acidification". Nature Geoscience 7 (4): 279–282. doi:10.1038/ngeo2095. Bibcode: 2014NatGe...7..279O.  https://dx.doi.org/10.1038%2Fngeo2095
  129. Vellekoop, J. (2013). "Rapid short-term cooling following the Chicxulub impact at the Cretaceous–Paleogene boundary". Proceedings of the National Academy of Sciences 111 (21): 7537–7541. doi:10.1073/pnas.1319253111. PMID 24821785. Bibcode: 2014PNAS..111.7537V.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=4040585
  130. Brugger, Julia; Feulner, Georg; Petri, Stefan (2016). "Baby, it's cold outside: Climate model simulations of the effects of the asteroid impact at the end of the Cretaceous". Geophysical Research Letters 44 (1): 419–427. doi:10.1002/2016GL072241. Bibcode: 2017GeoRL..44..419B.  https://dx.doi.org/10.1002%2F2016GL072241
  131. Pope, K.O.; Baines, K.H.; Ocampo, A.C.; Ivanov, B.A. (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. Bibcode: 1997JGR...10221645P.  https://dx.doi.org/10.1029%2F97JE01743
  132. Morgan J; Lana, C.; Kersley, A.; Coles, B.; Belcher, C.; Montanari, S.; Diaz-Martinez, E.; Barbosa, A. et al. (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. Bibcode: 2006E&PSL.251..264M. http://spiral.imperial.ac.uk/bitstream/10044/1/1208/1/EPSL-D-05-00905%5b1%5d.pdf. Retrieved 2018-08-06. 
  133. Joel, Lucas (16 January 2020). "Meteorite or Volcano? New Clues to the Dinosaurs' Demise - Twin calamities marked the end of the Cretaceous period, and scientists are presenting new evidence of which drove one of Earth's great extinctions.". The New York Times. https://www.nytimes.com/2020/01/16/science/dinosaurs-extinction-meteorite-volcano.html. Retrieved 17 January 2020. 
  134. Hull, Picncelli M. (17 January 2020). "On impact and volcanism across the Cretaceous-Paleogene boundary". Science 367 (6475): 266–272. doi:10.1126/science.aay5055. PMID 31949074. Bibcode: 2020Sci...367..266H. https://escholarship.org/content/qt5sr2q5tr/qt5sr2q5tr.pdf?t=q4ib9s. 
  135. "Asteroid impact, not volcanoes, made the Earth uninhabitable for dinosaurs" (in en). phys.org. https://phys.org/news/2020-06-asteroid-impact-volcanoes-earth-uninhabitable.html. Retrieved 6 July 2020. 
  136. Chiarenza, Alfio Alessandro; Farnsworth, Alexander; Mannion, Philip D.; Lunt, Daniel J.; Valdes, Paul J.; Morgan, Joanna V.; Allison, Peter A. (24 June 2020). "Asteroid impact, not volcanism, caused the end-Cretaceous dinosaur extinction" (in en). Proceedings of the National Academy of Sciences. doi:10.1073/pnas.2006087117. ISSN 0027-8424. https://www.pnas.org/content/early/2020/06/23/2006087117. Retrieved 6 July 2020. 
  137. A megatsunami is a massive movement of sea waters, which can reach inland tens or hundreds of kilometers.
  138. "Updated drilling: Dinosaur-killing impact crater explains buried circular hills". Science Magazine. November 2016. http://www.sciencemag.org/news/2016/11/updated-drilling-dinosaur-killing-impact-crater-explains-buried-circular-hills. Retrieved 2017-10-14. 
  139. "Chicxulub crater dinosaur extinction". The New York Times (New York, NY). 2016-11-18. https://www.nytimes.com/2016/11/18/science/chicxulub-crater-dinosaur-extinction.html. Retrieved 2017-10-14. 
  140. Brannen, Peter (2017). The Ends of the World: Volcanic Apocalypses, Lethal Oceans, and Our Quest to Understand Earth's Past Mass Extinctions. Harper Collins. p. 336. ISBN 9780062364807. 
  141. "Main Deccan volcanism phase ends near the K–T boundary: Evidence from the Krishna-Godavari Basin, SE India". Earth and Planetary Science Letters 268 (3–4): 293–311. 2008. doi:10.1016/j.epsl.2008.01.015. Bibcode: 2008E&PSL.268..293K.  https://dx.doi.org/10.1016%2Fj.epsl.2008.01.015
  142. "Rapid eruption of the Deccan flood basalts at the Cretaceous/Tertiary boundary". Nature 333 (6176): 841–843. 1988. doi:10.1038/333841a0. Bibcode: 1988Natur.333..841D.  https://dx.doi.org/10.1038%2F333841a0
  143. Courtillot, Vincent (1990). "A volcanic eruption". Scientific American 263 (4): 85–92. doi:10.1038/scientificamerican1090-85. PMID 11536474. Bibcode: 1990SciAm.263d..85C.  https://dx.doi.org/10.1038%2Fscientificamerican1090-85
  144. Alvarez, W (1997). T. rex and the Crater of Doom. Princeton University Press. pp. 130–146. ISBN 978-0-691-01630-6. https://archive.org/details/trexcraterofdoo000alva. 
  145. Renne, P. R. (2015). "State shift in Deccan volcanism at the Cretaceous-Paleogene boundary, possibly induced by impact". Science 350 (6256): 76–78. doi:10.1126/science.aac7549. PMID 26430116. Bibcode: 2015Sci...350...76R.  https://dx.doi.org/10.1126%2Fscience.aac7549
  146. Richards, M. A. (2015). "Triggering of the largest Deccan eruptions by the Chicxulub impact". Geological Society of America Bulletin 127 (11–12): 1507–1520. doi:10.1130/B31167.1. Bibcode: 2015GSAB..127.1507R.  https://dx.doi.org/10.1130%2FB31167.1
  147. Mullen L (October 13, 2004). "Debating the Dinosaur Extinction". Astrobiology Magazine. http://www.astrobio.net/exclusive/1243/debating-the-dinosaur-extinction. Retrieved 2012-03-29. 
  148. Mullen L (October 20, 2004). "Multiple impacts". Astrobiology Magazine. http://www.astrobio.net/exclusive/1253/multiple-impacts. Retrieved 2012-03-29. 
  149. Mullen L (November 3, 2004). "Shiva: Another K–T impact?". Astrobiology Magazine. http://www.astrobio.net/exclusive/1281/shiva-another-k-t-impact. Retrieved 2012-03-29. 
  150. 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. https://books.google.com/?id=3IORF1Ei3LIC&pg=PA31. 
  151. 2.3.CO;2. Bibcode: 1998Geo....26..995L.  https://dx.doi.org/10.1130%2F0091-7613%281998%29026%3C0995%3AADSWAT%3E2.3.CO%3B2" id="ref_151">Li, Liangquan; Keller, Gerta (1998). "Abrupt deep-sea warming at the end of the Cretaceous". Geology 26 (11): 995–998. doi:10.1130/0091-7613(1998)026<0995:ADSWAT>2.3.CO;2. Bibcode: 1998Geo....26..995L.  https://dx.doi.org/10.1130%2F0091-7613%281998%29026%3C0995%3AADSWAT%3E2.3.CO%3B2
  152. Petersen, Sierra V.; Dutton, Andrea; Lohmann, Kyger C. (2016). "End-Cretaceous extinction in Antarctica linked to both Deccan volcanism and meteorite impact via climate change". Nature Communications 7: 12079. doi:10.1038/ncomms12079. PMID 27377632. Bibcode: 2016NatCo...712079P.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=4935969
  153. Alroy, John (1999). "The fossil record of North American Mammals: evidence for a Palaeocene evolutionary radiation". Systematic Biology 48 (1): 107–118. doi:10.1080/106351599260472. PMID 12078635.  https://dx.doi.org/10.1080%2F106351599260472
  154. Alroy J (May 1998). "Cope's rule and the dynamics of body mass evolution in North American fossil mammals". Science 280 (5364): 731–4. doi:10.1126/science.280.5364.731. PMID 9563948. Bibcode: 1998Sci...280..731A. http://doc.rero.ch/record/20309/files/PAL_E4068.pdf. 
  155. Ericson, P G; Anderson, C L; Britton, T (December 2006). "Diversification of Neoaves: integration of molecular sequence data and fossils". Biol. Lett. 2 (4): 543–7. doi:10.1098/rsbl.2006.0523. PMID 17148284.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=1834003
  156. Longrich, N. R.; Bhullar, B.-A. S.; Gauthier, J. A. (December 2012). "Mass extinction of lizards and snakes at the Cretaceous-Paleogene boundary". Proc. Natl. Acad. Sci. U.S.A. 109 (52): 21396–401. doi:10.1073/pnas.1211526110. PMID 23236177. Bibcode: 2012PNAS..10921396L.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=3535637
  157. 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 (1688): 1675–1683. doi:10.1098/rspb.2009.2177. PMID 20133356.  http://www.pubmedcentral.nih.gov/articlerender.fcgi?tool=pmcentrez&artid=2871855
  158. Grimaldi, David A. (2007). Evolution of the Insects. Cambridge Univ Pr (E). ISBN 978-0-511-12388-7. 
More
© Text is available under the terms and conditions of the Creative Commons Attribution (CC BY) license (http://creativecommons.org/licenses/by/4.0/)
ScholarVision Creations
Feedback