Geologic ages of earth history
The geologic history of the earth is preserved and documented in its rocks. The oldest fragment of earth's crust known so far, a detrital zircon crystal, is 4.4 billion years old. Since then, rocks have registered the events on our planet, an archive that becomes increasingly complete over time.
Geologists use the term age to refer to specific nomenclature that is much more exact than common use (see "nomenclature" below). Geological ages, in common use, refer to periods of marked change in the processes and events in the entire history of the earth. These changes have been delineated by physical evidence found in the earth’s lithosphere. Ages are also noted in reference to the types of organisms found in the fossil record down to the present day. Changes are marked by (but not exclusive of) such processes as volcanic activity, flooding, and seismic activity.
Geologists describe and study the geologic time in two distinct ways. On the one hand, they try to measure the geologic time as a physical quantity: this is the aim of a field of Earth sciences called geochronometry. The geologic time is most commonly measured with methods based on the radioactive decay of long-lived unstable isotopes present in the earth's crust, and is expressed in Ma (i.e., millions of years ago).
On other hand, geologic time can be described by establishing a hierarchical scheme of relative time subdivisions. This was the only representation of geologic time before radioactive decay was discovered, but it is still widely used in the current geologic practice and research. The boundaries of major relative time subdivisions, and especially those of the erathems, are marked by mass extinctions, in turn associated with physical events such as extreme volcanic activity and bolide impacts (bolides are extraterrestrial bodies, asteroids or a meteors for example, that strike or impact the earth.) 
However, the definition of time-rock units must follow a formal procedure, implying that some boundaries are placed at completely arbitrary positions. Indeed, this is the case for most of the minor divisions (ages) of the geologic time.
The identification, description and quantification of geologic time involves, in addition to geochronometry, the fields of stratigraphy (the sub-discipline of geology studying the relationships of strata in time and space), biostratigraphy (the use of fossils for ordering and correlating strata in relative time), and geochronology (the study of geological time itself).
When relative time subdivisions are coupled with absolute (measured) ages, they constitute a Geologic time scale, which is the main topic of this article.
Different geological time scales exist and the issues involved in arriving at a meaningful date can be very complex. Many regionalised time scales carry variations and omissions, but a reasonable consensus was reached on the 2004 geologic time scale by the International Commission on Stratigraphy (ICS). Subdivisions and absolute ages of this article are based mostly on this publication.
The underlying premises or basic ideas about geological ages and time scales in modern earth science are from people who worked during the period spanning the late 17th to the19th centuries. In 1669, Nicolaus Steno  described the principle of original horizontality composed of four basic geologic principles that today are the fundamental concepts of stratigraphy:
- Superposition of strata: Sedimentary materials are deposited from a fluid (particles in solution) onto a solid surface, ergo the strata above did not exist when lower stratum was formed;
- Initial horizontality of strata: Sedimentary materials are laid down laterally in a continuous horizontal manner (stratum),
- Stratal continuity: Superposition (stacking) occurs according to age—younger rocks are deposited on top of older rock;
- Cross cutting relationships: Deviation from horizontal layers (stratum) is altered after the material is deposited—earthquakes, volcanoes, etc.
So, like layers of paint, the different layers are laid down with the oldest on the very bottom and the youngest on top, then the next and so on. The key to this is understanding that at the time, the processes forming the earth were a complete mystery and explanations could be very convoluted and completely wrong. Steno’s work was a major breakthrough and he has been called the father of modern geology.
In 1795, James Hutton proposed the principle of uniformitarianism, later developed by Charles Lyell (Principles of Geology, published 1830). This principle defines natural geologic processes as uniform in frequency and magnitude throughout time. This is a critical concept in other fields as well, the principle that natural phenomena in process in the far distant past are proceeding in the present time. The magnitude of the processes were considered to be unchanged and all change was the result of the ‘sum of small effects’. Conceptually this came to mean that the earth is very old. How old was originally posited to be in the tens of millions of years but later work by Ernest Rutherford changed this dramatically.
The next phase of development in this field was from a canal builder in 19th century England, William Smith, In 1815 Smith produced a geologic map of England demonstrating the principle of biotic succession: The different types of animals that had lived and died in that region over immense periods of time had changed and left their fossils attesting to their existence. Simply put the principle of biotic succession says that fossils are found in rocks in a very definite order. Smith’s work has been incorporated to use fossils to define increments or stages within a relative time scale. Many of the ages are in fact named for the presence of life at those times. 
Determining geological ages and configuring current schema today is a direct outgrowth of research into natural radioactive decay that began with French physicist Henry Becquerel's discovery of the radioactive decay of uranium in 1896. Employing radioactivity to determine geologic time was first suggested in 1905 by New Zealand physicist Ernest Rutherford. Rutherford had determined that radioactive decay in any given material proceeds at a constant rate. Those elements are present in geologic samples and their radioactivity can be measured in extreme lengths of time. In 1907, radiochemist Bertram Borden Boltwood (Massachusetts) published his schema for geologic ages that incorporated radioactive decay measures. Boltwood’s premise for his dating method was that the decay of uranium suggested that geologic age could be determined by ratios of uranium, thorium and lead contained in the rocks. (Lead is the product of the radioactive decay of uranium and thorium.) This produced values of extreme lengths of time, some exceeding two billion years. Boltwood’s ages have since been revised but his calculations indicating from hundreds to thousands of millions of years are still considered correct.
Determining the age of the earth from physical evidence involves a number of fields that are strongly interrelated. Often the terms are intermingled while the goals and methods may be similar or different.
- Stratigraphy: The study of the order in which units of rock are deposited.
- Stratum (pl. strata): A unit of sedimentary rock, bounded on the upper and lower limits by different layers of rock (bedding planes and that are reasonably persistence on a lateral plane. In other words, a definable, physically obvious, layer of rock.
- Formation: A unit of rocks which is consistently recognizable over wide areas. Formations are employed to make geological maps.
- Period: The time-span over which a geological system was deposited. Time-units correspond to a recognised and defined body of rock defined by methods used in stratigraphic palaeontology.
- System: the rocks laid down during a Period (Carboniferous, Jurassic, etc.) For example, the Cretaceous System was created during the Cretaceous Period.
For largely pragmatic reasons, earth history needs to be subdivided into smaller portions. However, any period has different aspects:
- Lithostratigraphic Units: Rocks are deposited in successive layers which have chemically and mineralogically distinct characteristics. The subdivision of the rock successions leads to the distinction of Groups, Formations, and Members.
- Biostratigraphic Units: Distinctive characteristics of fossils of animals and plants which exist for limited periods of time in recognisable biozones permit the delineation rocks of certain ages in which they are deposited.
- Chronostratigraphic Units: Geochonographic measures of absolute time leads to chronostratigraphy and enables the subdivision of systems into Series and Stages.
- Magnetostratigraphic Units: Measurable magnetic properties of rocks may vary between different strata. These variations become the bases for different kinds of stratigraphic units known collectively as "magnetostratigraphic polarity units" or "magnetozones".
These subdivisions are done locally as well as globally. All hierarchically ordered units better serve research if they are fixed by sound boundaries that can be easily correlated worldwide. 
The ICS nomenclature for stratigraphic units is both Chronostratigraphic and Geochronological. They are positioned here in descending order (largest span of time to narrowest):
|Chronostratigraphic units||Geochronologic units|
There are two meanings for "age": one is the fundamental chronostratigraphic unit Age (geology), the other is the result an absolute datation, e.g., a radiometric datation, and is a number (e.g., the Induan age begun ca. 252 Ma, where "252 Ma" is a radiometric age). So "Induan" is an age, but to construe the "Triassic" as an age is an error: "Triassic" is a period.
These demarcations are delineated below in length of time in millions of years.
Global definitions of chronostratigraphic boundaries are the purview of the International Union of Geological Sciences (IUGS). While there are regional stratigraphic schemata that will vary considerably, there are international standards with which these various schema do agree and are referred to. The recommendations for Global Standard Stratotype-section and Points (GSSP) which demarcate the boundaries of the strata and ultimately define the age of the earth are processed through a sequence of stages. Stratigraphic boundaries are proposed to the sub-commission on a particular geologic stage who then submit their recommendations to the International Commission on Stratigraphy (ICS) for official acceptance. The ICS then refer their recommendations to the Executive Committee of IUGS for ratification. In this way, geologists the world over refer to a standard reference for the worldwide correlation of the boundary.
This distinguishes between lithostratigraphic definitions which can vary a great deal from region to region and chronostratigraphic definitions which are meant to set internationally defined standards. Whereas the lithostratigraphic studies denote physical characteristics of the strata (mineral and biotic sequences for example), the chronostratigraphic studies use various methods combining analysis of fossil records and radiometric studies to provide relative and absolute dating.
Beginning approximately 543 Ma (million years ago), the Phanerozoic eonothem is represented by rocks containing abundant fossil evidence. The word has Greek roots, deriving from Phaneros (Greek: φανερος) means “visible”, and zooikos (Greek: ζωικός) means “of or pertaining to animal”. The Phanerozoic spans, indeed, the time when abundant life forms became evident.
The Phanerozoic Eon encompasses three eras (in descending order to oldest):
- Cenozoic Era (65 mya to today)
From the Greek word kainos (καινος), meaning fresh or new and zoikos (ζωικός), of or pertaining to animals, combined here to denote new life. This marked the end of a major extinction of dinosaurs, foraminifers, calcareous nannofossils etc. and the emergence of an abundance of mammalian life.
- Mesozoic Era (248 to 65 mya)
- Paleozoic Era (543 to 248 mya)
The name is derived from Cambria, the Roman word for Wales, the area where the rocks of the Cambrian Period was first studied. Pre- indicates the ages before the rocks dated in Wales.Not actually termed an ‘Eon' by the ICS. Beginning approximately 4,500 mya and ending approximately 543 mya, the Precambrian encompasses about 88% of the earth's entire existence. The Precambrian encompasses three eons (in descending order to oldest), subdivided into eras:
- Proterozoic Eon (2500 to 543 mya)
- Neoproterozoic (900 to 543 mya)
- Mesoproterozoic (1600 to 900 mya)
- Paleoproterozoic (2500 to 1600 mya)
- Archaean Eon (3800 to 2500 mya)
- Neoarchean (2800 mya to 2500 mya)
- Mesoarchean (3200 to 2800 mya)
- Paleoarchean (3600 to 3200 mya)
- Eoarchean (no lower limit defined to 3600 mya)
- Hadean Eon (4500 to 3800 mya – Not Recognised by the International Commission on Stratigraphy)
While the International Commission on Stratigraphy does not define a beginning of the Archean, it is commonly regarded as that time when the earth solidified. The oldest known earth rocks are about 3.8 billion years old and that is a figure often used to mark the beginning of the Archean Era.
The Hadean Eon is divided into varying era schemes but none are recognised by the ISC. The Hadean is the period of time the earth was forming literally from a gaseous cloud as the solar system and the sun were forming. The only rocks on earth that date from that period are meteorites which are about 4.5 billion years old (the oldest lunar rocks are also about 4.5 billion years old). Technically, the Hadean is not a geologic eon since there are no rocks on the planet from the time of formation. The oldest known earth rocks are about 3.8 billion years old and would have formed after the earth turned from a molten to a solid state. The Hadean is not recognised by the International Commission on Stratigraphy.
The geological ages were originally demarcated into Primary, Secondary, Tertiary and Quaternary Eras. Giovanni Arduino (circa 1759) proposed that all of geologic time should be broken up into three great orders: the Primary, Secondary, and Tertiary. In 1829, Jules Desnoyers proposed the term "Quaternary" to describe of rocks younger than the youngest Tertiary deposits. The eras have since been renamed and Tertiary and Quaternary were merged into the Cenozoic as “periods” not eras. However, the boundary between the Tertiary (65 to 1.8 mya) and Quaternary (1.8 mya to today) were ambiguously defined and these terms have in turn been replaced. The International Commission on Stratigraphy now endorses the terms Paleogene and Neogene to subdivide the Cenozoic Era with a provisional demarcation of the Quaternary at the end of the eraCite error: Invalid
<ref> tag; invalid names, e.g. too many
In descending order to oldest:
- Quaternary (end of Neogene to present day - see note below)
- Neogene (23.03 mya to Quaternary Period)
- Paleogene (65.5 to 23.03 mya)
The current stratigraphic schema for the Cenozoic places the Quaternary at the end of the Neogene spanning a period of time beginning 2.6 million years ago or beginning 1.8 mya till the present time. However, the ICS has asterisked the Quaternary as ‘not yet decided’.
- Cretaceous (144 to 65 mya)
- Jurassic (206 to 144 mya)
- Triassic (248 to 206 mya)
- Permian (290 to 248 mya)
- Carboniferous (354 to 290 mya)
- Devonian (417 to 354 mya)
- Silurian (443 to 417 mya)
- Ordovician (48 to 443 mya)
- Cambrian (542 to 488 mya)
- Letter to Nature Wilde SA., Valley JW., Peck WH., Graham CM., 2001. Evidence from detrital zircons for the existence of continental crust and oceans on the Earth 4.4 Gyr ago. Nature, v. 409, pp. 175-178. "No crustal rocks are known to have survived since the time of the intense meteor bombardment that affected Earth between its formation about 4,550Myr ago and 4,030Myr, the age of the oldest known components in the Acasta Gneiss of northwestern Canada."
- Definitions Department of Earth and Environmental Sciences, University of Kentucky. Detrital refers to "loose grains of minerals or rocks that have been eroded from other rocks or earth materials. A detrital sedimentary rock is one that is composed of grains that derive from preexisting rocks. A quartz sandstone, for example, is typically composed of quartz grains that were eroded away from an extant body of rock (igneous, metamorphic or sedimentary)".
- Chesapeake Bay Bolide Woods Hole Field Center, U.S. Geological Survey. “There is no consensus on its [bolide] definition, but we use it to mean an extraterrestrial body in the 1-10-km size range, which impacts the earth at velocities of literally faster than a speeding bullet (20-70 km/sec = Mach 75), explodes upon impact, and creates a large crater. "Bolide" is a generic term, used to imply that we do not know the precise nature of the impacting body . . . whether it is a rocky or metallic asteroid, or an icy comet, for example. or climate changes recognized globally.” Retrieved June 4, 2007
- A Greek-English Lexicon Henry George Liddell, Robert Scott (1940 edition). The word “bolide” is derived from the Greek word βολις, (bolis) which refers to a projectile, a missile or javelin, in hunting or warfare. It is also used to indicate a “flash” of light as in “astrapôn bolides”, literally "lightning flash". It may also refer to “a cast of the dice", which, given the catastrophic and unpredictable events that ensue when a bolide strikes the earth, is an ironic metaphor for bolide influence on earth’s history.
- Geological Time Climate Modeling and Diagnostics Group, Division of Ocean and Climate Physics, Lamont-Doherty Earth Observatory of Columbia University
- A Call for Telling Better Time over the Eons Richard A. Kerr (2003) Science vol 302:14 October
- Gradstein FM., Ogg JG., and Smith AG., 2004, A Geologic Time Scale 2004. Cambridge University Press.
- born Niels Steensen in Copenhagen, Denmark, 1638, died 1686
- De solido intra solidum naturaliter contento dissertationis prodromus, or Preliminary discourse to a dissertation on a solid body naturally contained within a solid. (The book's title is often simply abbreviated to Prodromus.)
- The Geologic Time Scale in Historical Perspective University of California Museum of Paleontology
- Nicholas Steno University of California Museum of Paleontology
- Nicolaus Steno James S. Aber, History of Geology, Emporia State University
- E. Rutherford’s work was reported in numerous publications: Radioactivity 1904, Cambridge University Press 2nd Edition 1905, (pp580); Radioactive Transformations (1906) Charles Scribner's Sons, NY (pp287) From his Silliman Memorial Lectures at Yale University, March 1905. For a comprehensive list of his related publications refer to Rutherford's Publications Rutherford.org.nz
- Boltwood, Bertram (1907) The Ultimate Disintegration Products of the Radio-active Elements. Part II. The disintegration products of uranium. American Journal of Science series 4, volume 23, pages 77-88
- Geologic Age USGS Learning Web. Retrieved 16 April, 2007
- A Brief History of the Division of Earth Sciences National Academy of Sciences. Retrieved 16 April, 2007
- History of Radiometric Dating Changing Views of the History of the Earth
- Geological Society of London
- Lithostratigraphic units International Stratigraphic Guide
- Biostratigraphic units International Stratigraphic Guide
- Chronostratigraphic units International Stratigraphic Guide
- Magnetostratigraphic polarity unitsInternational Stratigraphic Guide
- Cambrian Stratigraphy International Subcommission on Cambrian Stratigraphy, International Commission on Stratigraphy
- see for example the Introduction Global Standard Stratotype-section and Point (GSSP) of the Piacenzian Stage (Middle Pliocene)
-  Woodhouse English Greek Dictionary
- Dorlands Illustrated Medical Dictionary
- Cenozoic GeoWhen Database
- The Cenozoic (or Cainozoic) is subdivided into two sub-eras: Tertiary and Quaternary. In the 2004 Geologic time scale, the base of the Quaternary corresponds to the base of the Gelasian (i.e., within the Pliocene). This convention is at odds with traditional use of the term Quaternary, which is usually intended as the Pleistocene+Holocene, and is currently hotly debated (cf. GRADSTEIN et al., 2004)
- The Pennsylvanian and Mississippian have the rank of subsystems. However, all but the last Carboniferous series comprise only one stage and have been omitted from this scheme
- Glossary Illinois State Geological Survey
- Hadean time University of California Museum of Paleontology. Retrieved April 17, 2007
- Hadean Eon GeoWhen Database
- Whatever happened to the Tertiary and Quaternary? GeoWhen Database, Robert A. Rohde Physics Department, University of California at Berkeley
- International Stratigraphic Chart International Commission on Stratigraphy, 2007