Few discussions in geology can occur without reference to geologic time. Geologic time is often dicussed in two forms:
- Relative time ("chronostratic") -- subdivisions of the Earth's geology in a specific order based upon relative age relationships (most commonly, vertical/stratigraphic position). These subdivisions are given names, most of which can be recognized globally, usually on the basis of fossils.
- Absolute time ("chronometric") -- numerical ages in "millions of years" or some other measurement. These are most commonly obtained via radiometric dating methods performed on appropriate rock types.
Think of relative time as physical subdivisions of the rock found in the Earth's stratigraphy, and absolute time as the measurements taken upon those to determine the actual time which has expired. Absolute time measurements can be used to calibrate the relative time scale, producing an integrated geologic or "geochronologic" time scale.
It is important to realize that with new information about subdivision or correlation of relative time, or new measurements of absolute time, the dates applied to the time scale can and do change. Revisions to the relative time scale have occurred since the late 1700s. The numerically calibrated geologic time scale has been continuously refined since approximately the 1930s (e.g., Holmes, 1937), although the amount of change with each revision has become smaller over the decades (see fig. 1.5 and 1.6 of Harland et al.) and a few numerical estimates were available previously (but often for the duration of the entire scale rather than its individual subdivisions).
In addition, like any good scientific measurement, every dated boundary has an uncertainty associated with it, expressed as "+- X millions of years". These can not be included in the diagram for practical reasons, but can be found in Harland et al., 1990, along with a detailed description of the history of earlier-proposed time scales and the terminology, methodology and data involved in constructing this geological time scale.
Because of continual refinement, none of the values depicted in this diagram should be considered definitive, even though some have not changed significantly in a long time and are very well constrained (e.g., the Cretaceous/Tertiary boundary has been at 65+-1 Ma for decades, and has been tested innumerable times, with almost all dates somewhere between 64 and 66 million years). The overall duration and relative length of these large geologic intervals is unlikely to change much, but the precise numbers may "wiggle" a bit as a result of new data.
This geological time scale is based upon Harland et al., 1990, but with the Precambrian/Cambrian boundary modified according to the most recently-published radiometric dates on that interval, revising the boundary from 570+-15 million years to 543+-1 million years ago (Grotzinger et al., 1995). Other changes have been proposed since 1990 (e.g., revision of the Cretaceous by Obradovich, 1993), but are not incorporated because they are relatively small.
The time scale is depicted in its traditional form with oldest at the bottom and youngest at the top -- the present day is at the zero mark. Geologic time is finely subdivided through most of the Phanerozoic (see Harland et al., 1990 for details), but most of the finer subdivisions (e.g., epochs) are commonly referred to by non-specialists only in the Tertiary. Because of the vast difference in scale, the younger intervals have been successively expanded to the right to show some of these finer subdivisions.
Earth Science Week Editor's Note: As terms, Tertiary subdivisions Paleogene and Neogene have gained favor relatively recently. Older literature divides the Tertiary into epochs (from oldest to newest): Paleocene, Eocene, Oligocence, Miocene, and Pliocene. Moreover, the Quaternary is sometimes divided into Pleistocene and Holocene.
Source (text and graphic): University of Calgary, Geology and Geophysics Department. References available on the department's web page.