Paleocene

Not to be confused with Paleogene.
System/
Period		 Series/
Epoch		 Stage/
Age		 Age (Ma)
Neogene Miocene Aquitanian younger
Paleogene Oligocene Chattian 23.03–28.1
Rupelian 28.1–33.9
Eocene Priabonian 33.9–38.0
Bartonian 38.0–41.3
Lutetian 41.3–47.8
Ypresian 47.8–56.0
Paleocene Thanetian 56.0–59.2
Selandian 59.2–61.6
Danian 61.6–66.0
Cretaceous Upper/
Late		 Maastrichtian older
Subdivision of the Paleogene Period
according to the ICS, as of January 2013.[1]

The Paleocene (/ˈpæliɵsiːn/ or /ˈpeɪliɵsiːn/; symbol Pε [2]) or Palaeocene, the "old recent", is a geologic epoch that lasted from about 66 to 56 million years ago. It is the first epoch of the Paleogene Period in the modern Cenozoic Era. As with many geologic periods, the strata that define the epoch's beginning and end are well identified, but the exact ages remain uncertain.

The Paleocene Epoch brackets two major events in Earth's history. It started with the mass extinction event at the end of the Cretaceous, known as the Cretaceous–Paleogene (K–Pg) boundary. This was a time marked by the demise of non-avian dinosaurs, giant marine reptiles and much other fauna and flora. The die-off of the dinosaurs left unfilled ecological niches worldwide. It ended with the Paleocene–Eocene Thermal Maximum. This was a geologically brief (~0.2 million year) interval characterized by extreme changes in climate and carbon cycling.

The name "Paleocene" comes from Greek and refers to the "old(er)" (παλαιός, palaios) "new" (καινός, kainos) fauna that arose during the epoch.[3]

Boundaries and subdivisions

The K–Pg boundary that marks the separation between Cretaceous and Paleocene is visible in the geological record of much of the Earth by a discontinuity in the fossil fauna, with high iridium levels. There is also fossil evidence of abrupt changes in flora and fauna. There is some evidence that a substantial but very short-lived climatic change may have happened in the very early decades of the Paleocene. There are several theories about the cause of the K–Pg extinction event, with most evidence supporting the impact of a 10 km diameter asteroid forming the buried Chicxulub crater on the coast of Yucatan, Mexico.

The end of the Paleocene (~55.8 Ma) was also marked by a time of major change, one of the most significant periods of global change during the Cenozoic.[4] The Paleocene–Eocene Thermal Maximum upset oceanic and atmospheric circulation and led to the extinction of numerous deep-sea benthic foraminifera and a major turnover in mammals on land.

The Paleocene is divided into three stages, the Danian, the Selandian and the Thanetian, as shown in the table above. Additionally, the Paleocene is divided into six Mammal Paleogene zones.

Climate

The early Paleocene was cooler and dryer than the preceding Cretaceous, though temperatures rose sharply during the Paleocene–Eocene Thermal Maximum. The climate became warm and humid worldwide towards the Eocene boundary, with subtropical vegetation growing in Greenland and Patagonia, crocodiles swimming off the coast of Greenland, and early primates evolving in tropical palm forests of northern Wyoming.[5] The Earth's poles were cool and temperate; North America, Europe, Australia and southern South America were warm and temperate; equatorial areas had tropical climates; and north and south of the equatorial areas, climates were hot and arid.[6]

Paleogeography

In many ways, the Paleocene continued processes that had begun during the late Cretaceous Period. During the Paleocene, the continents continued to drift toward their present positions. Supercontinent Laurasia had not yet separated into three continents - Europe and Greenland were still connected, North America and Asia were still intermittently joined by a land bridge, while Greenland and North America were beginning to separate.[7] The Laramide orogeny of the late Cretaceous continued to uplift the Rocky Mountains in the American west, which ended in the succeeding epoch.

South and North America remained separated by equatorial seas (they joined during the Neogene); the components of the former southern supercontinent Gondwanaland continued to split apart, with Africa, South America, Antarctica and Australia pulling away from each other. Africa was heading north towards Europe, slowly closing the Tethys Ocean, and India began its migration to Asia that would lead to a tectonic collision and the formation of the Himalayas.

The inland seas in North America (Western Interior Seaway) and Europe had receded by the beginning of the Paleocene, making way for new land-based flora and fauna.

Oceans

Warm seas circulated throughout the world, including the poles. The earliest Paleocene featured a low diversity and abundance of marine life, but this trend reversed later in the epoch.[7] Tropical conditions gave rise to abundant marine life, including coral reefs. With the demise of marine reptiles at the end of the Cretaceous, sharks became the top predators. At the end of the Cretaceous, the ammonites and many species of foraminifera became extinct.

Marine fauna also came to resemble modern fauna, with only the marine mammals and the Carcharhinid sharks missing.

Flora

Terrestrial Paleocene strata immediately overlying the K–Pg boundary is in places marked by a "fern spike": a bed especially rich in fern fossils.[8] Ferns are often the first species to colonize areas damaged by forest fires; thus the fern spike may indicate post-Chicxulub crater devastation.[9]

In general, the Paleocene is marked by the development of modern plant species. Cacti and palm trees appeared. Paleocene and later plant fossils are generally attributed to modern genera or to closely related taxa.

The warm temperatures worldwide gave rise to thick tropical, sub-tropical and deciduous forest cover around the globe (the first recognizably modern rain forests) with ice-free polar regions covered with coniferous and deciduous trees.[7] With no large grazing dinosaurs to thin them, Paleocene forests were probably denser than those of the Cretaceous.[10]

Flowering plants (angiosperms), first seen in the Cretaceous, continued to develop and proliferate, and along with them coevolved the insects that fed on these plants and pollinated them.

Fauna

Mammals

Life restoration of Titanoides

Mammals had first appeared in the Triassic, evolving from advanced cynodonts, and developed alongside the dinosaurs, exploiting ecological niches untouched by the larger and more famous Mesozoic animals: in the insect-rich forest underbrush and high up in the trees. These smaller mammals (as well as birds, reptiles, amphibians, and insects) survived the mass extinction at the end of the Cretaceous which wiped out the non-avian dinosaurs, and mammals diversified and spread throughout the world.

While early mammals were small nocturnal animals that mostly ate soft plant material and small animals such as insects, the demise of the non-avian dinosaurs and the beginning of the Paleocene saw mammals growing bigger and occupying a wider variety of ecological niches. Ten million years after the death of the non-avian dinosaurs, the world was filled with rodent-like mammals, medium-sized mammals scavenging in forests, and large herbivorous and carnivorous mammals hunting other mammals, birds, and reptiles.

Fossil evidence from the Paleocene is scarce, and there is relatively little known about mammals of the time. Because of their small size (constant until late in the epoch) early mammal bones are not well preserved in the fossil record, and most of what we know comes from fossil teeth (a much tougher substance), and only a few skeletons.[7]

The brain to body mass ratios of these archaic mammals were quite low.[11]

Mammals of the Paleocene include:

Reptiles

Section of an Asiatosuchus jaw

Because of the climatic conditions of the Paleocene, reptiles were more widely distributed over the globe than at present. Among the sub-tropical reptiles found in North America during this epoch are champsosaurs (aquatic reptiles that resemble modern gharials), crocodilia, soft-shelled turtles, palaeophi snakes, varanid lizards, and Protochelydra zangerli (similar to modern snapping turtles).

Examples of champsosaurs of the Paleocene include Champsosaurus gigas, the largest champsosaur ever discovered. This creature was unusual among Paleocene reptiles in that C. gigas became larger than its known Mesozoic ancestors: C. gigas is more than twice the length of the largest Cretaceous specimens (3 meters versus 1.5 meters). Reptiles as a whole decreased in size after the K–Pg event. Champsosaurs declined towards the end of the Paleocene and became extinct during the Miocene.

Examples of Paleocene crocodylians are Borealosuchus (formerly Leidyosuchus) formidabilis, the apex predator and the largest animal of the Wannagan Creek fauna, and the alligatorid Wannaganosuchus.

Non-avian dinosaurs may have survived to some extent into the early Danian stage of the Paleocene Epoch circa 64.5 Mya. The controversial evidence for such is a hadrosaur leg bone found from Paleocene strata in New Mexico;[13] but such stray late forms may be derived fossils.[14]

Birds

Gastornis

Birds began to re-diversify during the epoch, occupying new niches. Most modern bird types had appeared by mid-Cenozoic, including perching birds, cranes, hawks, pelicans, herons, owls, ducks, pigeons, loons, and woodpeckers.

Large flightless birds have been found in late Paleocene deposits, including the herbivorous Gastornis in Europe and carnivorous terror birds in South America, the latter of which survived until the Pleistocene.

In the late Paleocene, early owl types appeared, such as Ogygoptynx in the United States and Berruornis in France.

References

  1. ↑ Cohen, K.M.; Finney, S.; Gibbard, P.L. (2013), International Chronostratigraphic Chart (PDF), International Commission on Stratigraphy.
  2. ↑ "Geologic Age Symbol Font (StratagemAge)" (PDF). USGS. 99-430. Retrieved 2011-06-22.
  3. ↑ "Paleocene". Online Etymology Dictionary.
  4. ↑ Gavin A. Schmidt and Drew T. Shindell (2003). "Atmospheric composition, radiative forcing, and climate change as a consequence of a massive methane release from gas hydrates" (PDF). Paleoceanography 18 (1). doi:10.1029/2002PA000757.
  5. ↑ "Science Notes 2003:". Scicom.ucsc.edu. Retrieved 2012-08-28.
  6. ↑ "Paleocene Climate". PaleoMap Project. Retrieved 2012-08-28.
  7. ↑ 7.0 7.1 7.2 7.3 Hooker, J.J., "Tertiary to Present: Paleocene", pp. 459-465, Vol. 5. of Selley, Richard C., L. Robin McCocks, and Ian R. Plimer, Encyclopedia of Geology, Oxford: Elsevier Limited, 2005. ISBN 0-12-636380-3
  8. ↑ Vajda, Vivi. "Global Disruption of Vegetation at the Cretaceous-Tertiary Boundary – A Comparison Between the Northern and Southern Hemisphere Palynological Signals". Gsa.confex.com. Retrieved 2006-07-15.
  9. ↑ Bigelow, Phillip. "The K–T boundary In The Hell Creek Formation". Scn.org. Retrieved 2006-07-15.
  10. ↑ Stephen Jay Gould, ed., The Book of Life (New York: W.W. Norton & Company, 1993), p. 182.
  11. ↑ Kazlev, M. Alan (2002) "The Paleocene". Palaeos Cenozoic. Retrieved April 3, 2013.
  12. ↑ Musser, A. M. (2003). "Review of the monotreme fossil record and comparison of palaeontological and molecular data". Comparative Biochemistry and Physiology Part A 136: 927–942. doi:10.1016/S1095-6433Ž03.00275-7. Retrieved April 3, 2013.
  13. ↑ Fassett, JE, Lucas, SG, Zielinski, RA, and Budahn, JR (2001). "Compelling new evidence for Paleocene dinosaurs in the Ojo Alamo Sandstone, San Juan Basin, New Mexico and Colorado, USA" (PDF). Catastrophic events and mass extinctions, Lunar and Planetary Contribution 1053: 45–46. Retrieved 2007-05-18.
  14. ↑ Sullivan, RM (2003). "No Paleocene dinosaurs in the San Juan Basin, New Mexico". Geological Society of America Abstracts with Programs 35 (5): 15. Retrieved 2007-07-02.

External links

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Paleogene Period
Paleocene Epoch Eocene Epoch Oligocene Epoch
Danian | Selandian
Thanetian		 Ypresian | Lutetian
Bartonian |Priabonian		 Rupelian | Chattian