Difference between revisions of "Geochronology" - New World Encyclopedia

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== Geochronology and biostratigraphy ==
 
== Geochronology and biostratigraphy ==
  
Geochronology differs in application from [[biostratigraphy]], which is the science of assigning sedimentary rocks to a known geological period via describing, cataloging and comparing fossil floral and faunal assemblages. Biostratigraphy does not ''directly'' provide an absolute age determination of a rock, merely places it within an ''interval'' of time at which that fossil assemblage is known to have coexisted. Both disciplines work together hand in hand however, to the point they share the same system of naming [[strata|rock layers]] and the time spans utilized to classify layers within a strata. (See table at right for terminology.)
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Geochronology differs in application from [[biostratigraphy]], which is the science of assigning relative ages of sedimentary rocks by describing, cataloging, and comparing fossil assemblages within them. Biostratigraphy does not ''directly'' provide an absolute age determination of a rock, but it merely places the rock within an ''interval'' of time at which that fossil assemblage is known to have coexisted. However, both disciplines work together hand in hand, to the point that they share the same system of naming [[strata|rock layers]] and the time spans utilized to classify layers within a strata. (The terminology is given in the table on the right.)
  
 
For instance, with reference to the [[Geologic Time Scale|Geologic time scale]], the Upper [[Permian]] ([[Lopingian]]) lasted from 270.6 +/- 0.7 Ma (Ma = millions of years ago) until somewhere between 250.1 +/- 0.4 Ma (oldest known [[Triassic]]) and 260.4 +/- 0.7 Ma (youngest known Lopingian) - a gap in known, dated fossil assemblages of nearly 10 Ma. While the biostratigraphic age of an Upper Permian bed may be shown to be Lopingian, the true date of the bed could be anywhere from 270 to 251 Ma.  
 
For instance, with reference to the [[Geologic Time Scale|Geologic time scale]], the Upper [[Permian]] ([[Lopingian]]) lasted from 270.6 +/- 0.7 Ma (Ma = millions of years ago) until somewhere between 250.1 +/- 0.4 Ma (oldest known [[Triassic]]) and 260.4 +/- 0.7 Ma (youngest known Lopingian) - a gap in known, dated fossil assemblages of nearly 10 Ma. While the biostratigraphic age of an Upper Permian bed may be shown to be Lopingian, the true date of the bed could be anywhere from 270 to 251 Ma.  

Revision as of 23:46, 24 February 2009

e  h
Units in geochronology and stratigraphy
Segments of rock (strata) in chronostratigraphy Periods of time in geochronology Notes
Eonothem
Eon
4 total, half a billion years or more
Erathem
Era
12 total, several hundred million years
System
Period
Series
Epoch
tens of millions of years
Stage
Age
millions of years
Chronozone
Chron
smaller than an age/stage, not used by the ICS timescale

Geochronology is the science of determining the absolute ages of rocks, fossils, and sediments found on Earth. This field of science relies on a variety of dating methods, which can be classified under the larger groupings of radiometric dating, luminescence dating, and incremental dating. There is a certain degree of uncertainty inherent within each method used, but the interdisciplinary approach of using several methods helps produce the best results.

The science of geochronology is the prime tool used in the discipline of chronostratigraphy, which attempts to derive absolute age dates for all fossil assemblages and to determine the geologic history of the Earth and extraterrestrial bodies.

Geochronology and biostratigraphy

Geochronology differs in application from biostratigraphy, which is the science of assigning relative ages of sedimentary rocks by describing, cataloging, and comparing fossil assemblages within them. Biostratigraphy does not directly provide an absolute age determination of a rock, but it merely places the rock within an interval of time at which that fossil assemblage is known to have coexisted. However, both disciplines work together hand in hand, to the point that they share the same system of naming rock layers and the time spans utilized to classify layers within a strata. (The terminology is given in the table on the right.)

For instance, with reference to the Geologic time scale, the Upper Permian (Lopingian) lasted from 270.6 +/- 0.7 Ma (Ma = millions of years ago) until somewhere between 250.1 +/- 0.4 Ma (oldest known Triassic) and 260.4 +/- 0.7 Ma (youngest known Lopingian) - a gap in known, dated fossil assemblages of nearly 10 Ma. While the biostratigraphic age of an Upper Permian bed may be shown to be Lopingian, the true date of the bed could be anywhere from 270 to 251 Ma.

On the other hand, a granite which is dated at 259.5 +/- 0.5 Ma can reasonably safely be called "Permian," or most properly, to have intruded in the Permian.

Dating methods

As noted above, various dating methods are used in geochronology. Each method has a certain degree of uncertainty, but the reliability of the results can be enhanced by using several techniques.[1]

Radiometric dating

By measuring the amount of Radioactive decay of a radioactive isotope with a known half-life, geologists can establish the absolute age of the parent material. A number of radioactive isotopes are used for this purpose, and depending on the rate of decay, are used for dating different geological periods. With the exception of the radiocarbon method, most of these techniques are actually based on measuring an increase in the abundance of a radiogenic isotope, which is the decay-product of the radioactive parent isotope. [2][3][4] Two or more radiometric methods can be used in concert to achieve more robust results.[5] Most radiometric methods are suitable for geological time only, but some such as the radiocarbon method and the 40Ar/39Ar dating method can be extended into the time of early human life [6] and into recorded history.[7]

Some commonly used techniques are as follows:

  • Radiocarbon dating. This technique measures the decay of carbon-14 in organic material (e.g. plant macrofossils), and can be applied to samples younger than about 50,000 years.
  • Uranium-lead dating. This technique measures the ratio of two lead isotopes (lead-206 and lead-207) to the amount of uranium in a mineral or rock. Often applied to the trace mineral zircon in igneous rocks, this method is one of the two most commonly used (along with argon-argon dating) for geologic dating. Uranium-lead dating is applied to samples older than about 1 million years.
  • Uranium-thorium dating. This technique is used to date speleothems, corals, carbonates, and fossil bones. Its range is from a few years to about 700,000 years.
  • Potassium-argon dating and argon-argon dating. These techniques date metamorphic, igneous and volcanic rocks. They are also used to date volcanic ash layers within or overlying paleoanthropologic sites. The younger limit of the argon-argon method is a few thousand years.

Luminescence dating

Luminescence dating techniques observe 'light' emitted from materials such as quartz, diamond, feldspar, and calcite. Many types of luminescence techniques are utilized in geology, including optically stimulated luminescence (OSL), cathodoluminescence (CL), and thermoluminescence (TL). Thermoluminescence and optically stimulated luminescence are used in archaeology to date 'fired' objects such as pottery or cooking stones, and can be used to observe sand migration.

Incremental dating

Incremental dating techniques allow the construction of year-by-year annual chronologies, which can be fixed (i.e. linked to the present day and thus calendar or sidereal time) or floating.

Correlation of marker horizons

Marker horizons are geological units in different geographic locations but which are of the same age. This allow age-equivalence to be established between different sites. [8] For example, tephra is often used in archaeology.

Geological time periods: an overview

The following table gives an overview of geologic time periods. The second timeline expands on the last subsection of the first timeline, and third timeline expands on the last subsection of the second timeline, as indicated by asterisks.

Millions of Years

Differences between chronostratigraphy and geochronology

It is important not to confuse geochronologic and chronostratigraphic units.[9] Geochronological units are periods of time, thus it is correct to say that Tyrannosaurus rex lived during the Late Cretaceous Epoch.[10] Chronostratigraphic units are geological material, so it is also correct to say that fossils of the genus Tyrannosaurus have been found in the Upper Cretaceous Series. [11] In the same way, it is entirely possible to go and visit an Upper Cretaceous Series deposit - such as the Egyptian mangrove deposit where the Tyrannosaurus fossils were found - but it is naturally impossible to visit the Late Cretaceous Epoch as that is a period of time.


See also

  • List of geochronologic names
  • Arthur Holmes
  • Fritz Houtermans
  • Alfred O. C. Nier
  • Thomas Edvard Krogh

Notes

  1. Renne, P.R., K.R. Ludwig, and D.B Karner. 1998. Progress and challenges in geochronology. Science Progress. 83:107-121. Retrieved February 15, 2009.
  2. Dickin, A.P. 1995. Radiogenic Isotope Geology. Cambridge, UK: Cambridge University Press. ISBN 0521598915.
  3. Faure, G. 1986. Principles of isotope geology. Cambridge, UK: Cambridge University Press. ISBN 0471864129.
  4. Faure, G., and D. Mensing. 2005. Isotopes - Principles and applications, 3rd ed. Hoboken, NJ: J. Wiley & Sons. ISBN 0471384372.
  5. Dalrymple, G.B., M. Grove, O.M. Lovera, T.M. Harrison, J.B. Hulen, and M.A. Lanphere. 1999. Age and thermal history of the Geysers plutonic complex (felsite unit), Geysers geothermal field, California: a 40Ar/39Ar and U–Pb study. Earth and Planetary Science Letters. 173:285–298. Retrieved February 15, 2009.
  6. Ludwig, K.R., and P,R. Renne. 2000. Geochronology on the Paleoanthropological Time Scale. Evolutionary Anthropology. 9:101-110.
  7. Renne, P.R., W.D. Sharp, A.L. Deino, G. Orsi, and L. Civetta. 1997. 40Ar/39Ar dating into the historical realm: Calibration against Pliny the Younger. Science. 277:1279-1280. Retrieved February 15, 2009.
  8. Demidov, I.N. 2006. Identification of marker horizon in bottom sediments of the Onega Periglacial Lake. Doklady Earth Sciences. 407:213-216. Retrieved February 15, 2009.
  9. Weishampel, David. 1996. The Evolution and Extinction of the Dinosaurs. Cambridge, UK: Cambridge Press. ISBN 0521444969.
  10. Barrick, R.E., and W.J. Showers. 1994. Thermophysiology of Tyrannosaurus rex: Evidence from Oxygen Isotopes. Science. 265:222-224. Retrieved February 15, 2009.
  11. Smith, J.B., M.C. Lamanna, K.J. Lacovara, P. Dodson Jr., J.C. Poole, and R. Giegengack. 2001. A Giant Sauropod Dinosaur from an Upper Cretaceous Mangrove Deposit in Egypt. Science. 292:1704-1707.

References
ISBN links support NWE through referral fees

  • Dickin, A.P. 1995. Radiogenic Isotope Geology. Cambridge, UK: Cambridge University Press. ISBN 0521598915.
  • Faure, G. 1986. Principles of isotope geology. Cambridge, UK: Cambridge University Press. ISBN 0471864129.
  • Faure, G., and D. Mensing. 2005. Isotopes - Principles and applications, 3rd ed. Hoboken, NJ: J. Wiley & Sons. ISBN 0471384372.
  • Lowe, J.J., and M.J.C. Walker. 1997. Reconstructing Quaternary Environments, 2nd ed. Harlow, UK: Longman. ISBN 0582101662.
  • Smart, P.L., and P.D. Frances. 1991. Quaternary dating methods - a user's guide. Cambridge, UK: Quaternary Research Association Technical Guide No.4. ISBN 0907780083.
  • Weishampel, David. 1996. The Evolution and Extinction of the Dinosaurs. Cambridge, UK: Cambridge Press. ISBN 0521444969.

External links

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