Cretaceous

Mesozoic era (251 - 65 mya)


Triassic

Jurassic

Cretaceous



Cretaceous period
145 - 65 million years ago

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Key events in the Cretaceous period-140 —–-130 —–-120 —–-110 —–-100 —–-90 —–-80 —–-70 —–MaastrichtianCampanianSantonianConiacianTuronianCenomanianAlbianAptianBarremianHauterivianValanginianBerriasianJurassicPaleogene      C

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d Mesozoic era
 Cenozoic era
An approximate timescale of key Cretaceous events.
Axis scale: millions of years ago.


The Cretaceous period is one of the major divisions of the geologic timescale, reaching from the end of the Jurassic period, from about 146 to 136 million years ago (Ma) to the beginning of the Paleocene epoch of the Paleogene period, or Tertiary sub-era (about 65.5 to 64 Ma). As the longest geological period, the Cretaceous constitutes nearly half of the Mesozoic.
The end of the Cretaceous defines the boundary between the Mesozoic and Cenozoic eras, and is marked by the mass extinction known as the Cretaceous-Tertiary extinction event.
Dinosaurs were dominant during this period, while mammals remained small. An interesting development during the Cretaceous was the growing importance and diversity of flowering plants, an advance aided by a harmonious interaction with bees and other insects.
The Cretaceous (from Latin creta meaning "chalk") as a separate period was first defined by a Belgian geologist Jean d'Omalius d'Halloy in 1822, using strata in the Paris basin (GSE 1974) and named for the extensive beds of chalk (calcium carbonate deposited by the shells of marine invertebrates), found in the upper Cretaceous of the continental Europe and Great Britain (including the White Cliffs of Dover).

Contents

1 Dating
2 Divisions
3 Paleogeography
4 Climate
5 Flora
6 Fauna

6.1 Land animals
6.2 Marine animals
6.3 Extinction


7 References
8 Credits


Dating
As with other older geologic periods, the rock beds that define the Cretaceous are well identified but the exact dates of the period's start and end are uncertain by a few million years.
No great extinction or burst of diversity separated the Cretaceous from the Jurassic. However, the end of the period is most sharply defined, being placed at an iridium-rich layer found worldwide that is believed to be associated with the Chicxulub impact crater in Yucatan and the Gulf of Mexico. This layer has been tightly dated at 65.5 Ma. This bolide collision is probably responsible for the major, extensively-studied Cretaceous-Tertiary extinction event.

Divisions


Cretaceous period


Lower/Early Cretaceous

Upper/Late Cretaceous


Berriasian | Valanginian | Hauterivian
Barremian | Aptian | Albian

Cenomanian | Turonian | Coniacian
Santonian | Campanian | Maastrichtian

The Cretaceous is usually separated into Early and Late Cretaceous epochs. The faunal stages (divisions based on changes in the observed fossil assemblages) from youngest to oldest are listed below. Time is referred to as early or late, and the corresponding rocks are referred to as lower or upper:



Upper/Late Cretaceous


Maastrichtian

(70.6 ± 0.6–65.5 ± 0.3 Ma)


Campanian

(83.5 ± 0.7–70.6 ± 0.6 Ma)


Santonian

(85.8 ± 0.7–83.5 ± 0.7 Ma)


Coniacian

(89.3 ± 1.0–85.8 ± 0.7 Ma)


Turonian

(93.5 ± 0.8–89.3 ± 1.0 Ma)


Cenomanian

(99.6 ± 0.9–93.5 ± 0.8 Ma)


 


Lower/Early Cretaceous


Albian

(112.0 ± 1.0–99.6 ± 0.9 Ma)


Aptian

(125.0 ± 1.0–112.0 ± 1.0 Ma)


Barremian

(130.0 ± 1.5–125.0 ± 1.0 Ma)


Hauterivian

(136.4 ± 2.0–130.0 ± 1.5 Ma)


Valanginian

(140.2 ± 3.0–136.4 ± 2.0 Ma)


Berriasian

(145.5 ± 4.0–140.2 ± 3.0 Ma)

Paleogeography
 Pangea separation animation
During the Cretaceous, the late Paleozoic–early Mesozoic supercontinent of Pangea (or Pangaea) completed its breakup into present day continents, although their positions were substantially different at the time.
Though Gondwana was still intact in the beginning of the Cretaceous, Gondwana itself broke up as South America, Antarctica, and Australia rifted away from Africa (though India and Madagascar remained attached to each other). The Indian Ocean was newly formed. Such active rifting lifted great undersea mountain chains along the welts, raising eustatic sea levels worldwide. To the north of Africa, the Tethys Sea continued to narrow. Broad shallow seas advanced across central North America (the Western Interior Seaway) and Europe, and then started to recede, leaving thick marine deposits sandwiched between coal beds.
The Cretaceous is justly famous for its chalk; indeed, more chalk formed in the Cretaceous than in any other Period in the Phanerozoic (Stanley 1999). Laid down by calcareous nannoplankton, they reflect seas that were enriched with calcium relative to today's seas (and hence, more saturated), due to increased mid-ocean ridge activity (Stanley 1999). These widespread carbonates and other sedimentary deposits make the Cretaceous rock record especially fine. Famous formations from North America include the rich marine fossils of Kansas's Smoky Hill Chalk, and the terrestrial fauna of the late Cretaceous Hell Creek Formation. Other important Cretaceous exposures occur in Europe and China. In the area that is now India, massive lava beds called the Deccan Traps were laid down in the very late Cretaceous and early Paleocene.

Climate
The climate is considered to have been very warm during the Cretaceous and without any ice at the poles. Sea level was much higher than today, and large areas of the continental crust were covered with shallow seas. Sediment cores also show that temperatures in the deep ocean were 15-20°C higher than today (Skinner and Porter 1995). The Tethys Seaway connected the tropical oceans east to west, which also helped equalize the global climate. Warm-adapted plant fossils are known from localities as far north as Alaska and Greenland, while dinosaur fossils have been found within 15 degrees of the Cretaceous south pole (Stanley 1999).
The planet was probably not much warmer on average than it had been during the Triassic or Jurassic periods, but instead had a gentler temperature gradient from the equator to the poles; a side effect of this may have been weaker global winds, contributing to less upwelling and more stagnant oceans than today's (Stanley 1999).

Flora
Flowering plants (also known as angiosperms), spread during the Cretaceous, although they did not become predominant until near the end (Campanian age). Their evolution was aided by the appearance of bees; in fact, angiosperms and insects are a good example of mutually beneficial symbiotic interaction. The first representatives of many modern trees, including figs, planes, and magnolias, for example, appear in the Cretaceous. At the same time, some earlier Mesozoic gymnosperms, like conifers, continued to thrive, although other taxa like Bennettitales died out before the end of the period.

Fauna
Land animals
On land, mammals were a small and still relatively minor component of the fauna. The fauna was dominated by archosaurian reptiles, especially dinosaurs, which were at their most diverse. Pterosaurs were common in the early and middle Cretaceous, but as the Cretaceous proceeded they faced growing competition from the growing diversity and increase of birds, and by the end of the period only two highly specialized families remained.
A fascinating glimpse of life in the Early Cretaceous is provided by the Liaoning lagerstätte (Chaomidianzi formation) in China, where the beautifully preserved remains of a number of types of small dinosaurs, birds, and mammals have been found. The coelurosaur dinosaurs found there represent a number of types of the group maniraptora, which is transitional in form between dinosaurs and birds, and are remarkable for the presence of hair-like feathers.
During the Cretaceous, the insects began to diversify, and the oldest known ants, termites, and some lepidopterans appeared. Aphids, grasshoppers, and gall wasps appeared. Another important insect to evolve was the eusocial bee, which was integral to the ecology and evolution of flowering plants. (Eusocial refers to true sociality in an animal species, involving reproductive division of labor and cooperative brood care.)
Numerous exceptionally preserved insects have been found in the Lower Cretaceous Siberian lagerstätte of Baissa.

Marine animals
In the seas, rays, modern sharks, and teleosts became common. Marine reptiles included ichthyosaurs in the early and middle of the Cretaceous, plesiosaurs throughout the entire period, and mosasaurs in the Late Cretaceous.
Baculites, a straight-shelled form of ammonite, flourished in the seas. The Hesperornithiformes were flightless, marine diving birds that swam like grebes. Globotruncanid Foraminifera thrived. The Cretaceous also saw the first radiation of the diatoms in the oceans (freshwater diatoms did not appear until the Miocene).

Extinction
In the extinction event that defines the end of the Cretaceous, a significant number of species (around 50 percent) and known families (around 25 percent) disappeared. Plants appeared to be nearly unscathed, while marine organisms apparently were hit the hardest. These include a large number (around 95 percent) of types of planktic foraminifers (excepting the Globigerinida), an even larger number of Coccolithophores, all the ammonite and belemnite cephalopods, and all reef-forming rudist molluscs and inoceramid clams), as well as all marine reptiles except turtles and crocodiles.
Dinosaurs are the most famous victims of the Cretaceous extinction. Dinosaurs that were unique to the very end of the period (such as Tyrannosaurus rex, Triceratops, and Ankylosaurus) were wiped out. The last of the pterosaurs became extinct and the vast majority of birds did as well, including the Enantiornithes and Hesperornithiformes.
The intensive, mid-Cretaceous insect extinction began during the Albian.

ReferencesISBN links support NWE through referral fees
Great Soviet Encyclopedia (GSE). 1974. Sovetskaya Enciklopediya, 3rd edition. Volume 16, page 50.
Larson, N. L., S. D. Jorgensen, R. A. Farrar, and P. L. Larson. 1997. Ammonites and the other Cephalopods of the Pierre Seaway. Geoscience Press.
Ogg, J. 2004. Overview of Global Boundary Stratotype Sections and Points (GSSP's). Retrieved June 12, 2007.
Ovechkina, M. N., and A. S. Alekseev. 2005. Quantitative changes of calcareous nannoflora in the Saratov region (Russian Platform) during the late Maastrichtian warming event. Journal of Iberian Geology 31(1): 149-165.
Rasnitsyn, A. P. and D. L. J. Quicke. 2002. History of Insects. Kluwer Academic Publishers. ISBN 1-4020-0026-X
Skinner, B. J., and S. C. Porter. 1995. The Dynamic Earth: An Introduction to Physical Geology, 3rd ed. New York: John Wiley & Sons, Inc. ISBN 0-471-59549-7
Stanley, S. M. 1999. Earth System History. New York: W.H. Freeman and Company. ISBN 0-7167-2882-6



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