Geologic time scale
The time scale was developed through the study of physical rock layers and relationships as well as the times when different organisms appeared, evolved and became extinct through the study of fossilized remains and imprints.
The primary and largest catalogued divisions of time are periods called eons.
The first eon was the Hadean, when the Earth and moon were predicted to be formed, lasting over 600 million years until the Archean, which is when the Earth had cooled enough for continents and the earliest known life to emerge.
After about 2.5 billion years, oxygen generated by photosynthesizing single-celled organisms began to appear in the atmosphere marking the beginning of the Proterozoic.
Finally, the Phanerozoic eon encompasses 541 million years of diverse abundance of multicellular life starting with the appearance of hard animal shells in the fossil record and continuing to the present.
The first three eons (i.e. every eon but the Phanerozoic) can be referred to collectively as the Precambrian supereon.
The following four timelines show the geologic time scale.
The first shows the entire time from the formation of the Earth to the present, but this gives little space for the most recent eon.
Therefore, the second timeline shows an expanded view of the most recent eon.
In a similar way, the most recent era is expanded in the third timeline, and the most recent period is expanded in the fourth timeline.
Corresponding to eons, eras, periods, epochs and ages, the terms "eonothem", "erathem", "system", "series", "stage" are used to refer to the layers of rock that belong to these stretches of geologic time in Earth's history.
Geologists qualify these units as "early", "mid", and "late" when referring to time, and "lower", "middle", and "upper" when referring to the corresponding rocks.
The adjectives are capitalized when the subdivision is formally recognized, and lower case when not; thus "early Miocene" but "Early Jurassic."
The geology or deep time of Earth's past has been organized into various units according to events which are thought to have taken place.
For example, the boundary between the Cretaceous period and the Paleogene period is defined by the Cretaceous–Paleogene extinction event, which marked the demise of the non-avian dinosaurs and many other groups of life.
Older time spans, which predate the reliable fossil record (before the Proterozoic eon), are defined by their absolute age.
Geologic units from the same time but different parts of the world often are not similar and contain different fossils, so the same time-span was historically given different names in different locales.
A key aspect of the work of the International Commission on Stratigraphy is to reconcile this conflicting terminology and define universal horizons that can be used around the world.
Dominantly fluid planets, such as the gas giants, do not preserve their history in a comparable manner.
Apart from the Late Heavy Bombardment, events on other planets probably had little direct influence on the Earth, and events on Earth had correspondingly little effect on those planets.
Construction of a time scale that links the planets is, therefore, of only limited relevance to the Earth's time scale, except in a Solar System context.
The existence, timing, and terrestrial effects of the Late Heavy Bombardment are still a matter of debate.
History and nomenclature of the time scale
In Ancient Greece, Aristotle (384–322 BCE) observed that fossils of seashells in rocks resembled those found on beaches – he inferred that the fossils in rocks were formed by organisms, and he reasoned that the positions of land and sea had changed over long periods of time.
Leonardo da Vinci (1452–1519) concurred with Aristotle's interpretation that fossils represented the remains of ancient life.
The 11th-century Persian polymath Avicenna (Ibn Sina, died 1037) and the 13th-century Dominican bishop Albertus Magnus (died 1280) extended Aristotle's explanation into a theory of a petrifying fluid.
Establishment of primary principles
In the late 17th century Nicholas Steno (1638–1686) pronounced the principles underlying geologic (geological) time scales.
Steno argued that rock layers (or strata) were laid down in succession, and that each represents a "slice" of time.
He also formulated the law of superposition, which states that any given stratum is probably older than those above it and younger than those below it.
While Steno's principles were simple, applying them proved challenging.
Steno's ideas also lead to other important concepts geologists use today, such as relative dating.
Over the course of the 18th century geologists realized that:
- Sequences of strata often become eroded, distorted, tilted, or even inverted after deposition
- Strata laid down at the same time in different areas could have entirely different appearances
- The strata of any given area represented only part of Earth's long history
A major shift in thinking came when James Hutton presented his Theory of the Earth; or, an Investigation of the Laws Observable in the Composition, Dissolution, and Restoration of Land Upon the Globe before the Royal Society of Edinburgh in March and April 1785.
John McPhee asserts that "as things appear from the perspective of the 20th century, James Hutton in those readings became the founder of modern geology".
Hutton proposed that the interior of Earth was hot, and that this heat was the engine which drove the creation of new rock: land was eroded by air and water and deposited as layers in the sea; heat then consolidated the sediment into stone, and uplifted it into new lands.
This theory, known as "Plutonism", stood in contrast to the "Neptunist" flood-oriented theory.
Formulation of geologic time scale
The first serious attempts to formulate a geologic time scale that could be applied anywhere on Earth were made in the late 18th century.
The most influential of those early attempts (championed by Werner, among others) divided the rocks of Earth's crust into four types: Primary, Secondary, Tertiary, and Quaternary.
Each type of rock, according to the theory, formed during a specific period in Earth history.
It was thus possible to speak of a "Tertiary Period" as well as of "Tertiary Rocks."
Indeed, "Tertiary" (now Paleogene and Neogene) remained in use as the name of a geological period well into the 20th century and "Quaternary" remains in formal use as the name of the current period.
The identification of strata by the fossils they contained, pioneered by William Smith, Georges Cuvier, Jean d'Omalius d'Halloy, and Alexandre Brongniart in the early 19th century, enabled geologists to divide Earth history more precisely.
It also enabled them to correlate strata across national (or even continental) boundaries.
If two strata (however distant in space or different in composition) contained the same fossils, chances were good that they had been laid down at the same time.
Detailed studies between 1820 and 1850 of the strata and fossils of Europe produced the sequence of geologic periods still used today.
Naming of geologic periods, eras and epochs
Early work on developing the geologic time scale was dominated by British geologists, and the names of the geologic periods reflect that dominance.
The "Cambrian", (the classical name for Wales) and the "Ordovician" and "Silurian", named after ancient Welsh tribes, were periods defined using stratigraphic sequences from Wales.
The "Devonian" was named for the English county of Devon, and the name "Carboniferous" was an adaptation of "the Coal Measures", the old British geologists' term for the same set of strata.
However, some periods were defined by geologists from other countries.
The "Triassic" was named in 1834 by a German geologist Friedrich Von Alberti from the three distinct layers (Latin trias meaning triad) – red beds, capped by chalk, followed by black shales – that are found throughout Germany and Northwest Europe, called the ‘Trias’.
The "Cretaceous" (from Latin creta meaning ‘chalk’) as a separate period was first defined by Belgian geologist Jean d'Omalius d'Halloy in 1822, using strata in the Paris basin and named for the extensive beds of chalk (calcium carbonate deposited by the shells of marine invertebrates) found in Western Europe.
British geologists were also responsible for the grouping of periods into eras and the subdivision of the Tertiary and Quaternary periods into epochs.
In 1841 John Phillips published the first global geologic time scale based on the types of fossils found in each era.
Phillips' scale helped standardize the use of terms like Paleozoic ("old life") which he extended to cover a larger period than it had in previous usage, and Mesozoic ("middle life") which he invented.
Dating of time scales
Main article: Chronological dating
When William Smith and Sir Charles Lyell first recognized that rock strata represented successive time periods, time scales could be estimated only very imprecisely since estimates of rates of change were uncertain.
While creationists had been proposing dates of around six or seven thousand years for the age of Earth based on the Bible, early geologists were suggesting millions of years for geologic periods, and some were even suggesting a virtually infinite age for Earth.
Geologists and paleontologists constructed the geologic table based on the relative positions of different strata and fossils, and estimated the time scales based on studying rates of various kinds of weathering, erosion, sedimentation, and lithification.
Until the discovery of radioactivity in 1896 and the development of its geological applications through radiometric dating during the first half of the 20th century, the ages of various rock strata and the age of Earth were the subject of considerable debate.
The first geologic time scale that included absolute dates was published in 1913 by the British geologist Arthur Holmes.
He greatly furthered the newly created discipline of geochronology and published the world-renowned book The Age of the Earth in which he estimated Earth's age to be at least 1.6 billion years.
In 1977, the Global Commission on Stratigraphy (now the International Commission on Stratigraphy) began to define global references known as GSSP (Global Boundary Stratotype Sections and Points) for geologic periods and faunal stages.
The commission's work is described in the 2012 geologic time scale of Gradstein et al.
A UML model for how the timescale is structured, relating it to the GSSP, is also available.
Popular culture and a growing number of scientists use the term "Anthropocene" informally to label the current epoch in which we are living.
It has evolved to describe an "epoch" starting some time in the past and on the whole defined by anthropogenic carbon emissions and production and consumption of plastic goods that are left in the ground.
Critics of this term say that the term should not be used because it is difficult, if not nearly impossible, to define a specific time when humans started influencing the rock strata – defining the start of an epoch.
Others say that humans have not even started to leave their biggest impact on Earth, and therefore the Anthropocene has not even started yet.
The ICS has not officially approved the term as of September 2015.
The Anthropocene Working Group met in Oslo in April 2016 to consolidate evidence supporting the argument for the Anthropocene as a true geologic epoch.
Evidence was evaluated and the group voted to recommend "Anthropocene" as the new geological age in August 2016.
Should the International Commission on Stratigraphy approve the recommendation, the proposal to adopt the term will have to be ratified by the International Union of Geological Sciences before its formal adoption as part of the geologic time scale.
Table of geologic time
The following table summarizes the major events and characteristics of the periods of time making up the geologic time scale.
This table is arranged with the most recent geologic periods at the top, and the oldest at the bottom.
The height of each table entry does not correspond to the duration of each subdivision of time.
The content of the table is based on the current official geologic time scale of the International Commission on Stratigraphy (ICS), with the epoch names altered to the early/late format from lower/upper as recommended by the ICS when dealing with chronostratigraphy.
The ICS now provides an online, interactive, version of this chart too, , based on a service delivering a machine-readable Resource Description Framework/Web Ontology Language representation of the timescale which is available through the Commission for the Management and Application of Geoscience Information GeoSciML project as a service and at a SPARQL end-point.
Please note that this is not to scale, and even though the Phanerozoic eon looks longer than the rest, it merely spans 500 million years, whilst the previous three eons (or the Precambrian supereon) collectively span over 3.5 billion years.
This discrepancy is caused by the lack of action in the first three eons (or supereon) compared to ours (the Phanerozoic).
|Supereon||Eon||Era||Period||Epoch||Age||Major events||Start, million years ago|
|n/a||Phanerozoic||Cenozoic||Quaternary||Holocene||Meghalayan||4.2 kiloyear event, Little Ice Age, increasing industrial CO2.||0.0042|
|Northgrippian||8.2 kiloyear event, Holocene climatic optimum. Bronze Age.||0.0082|
|Greenlandian||Current interglacial begins. Sea level flooding of Doggerland and Sundaland. Sahara desert forms. Neolithic agriculture.||0.0117|
|Pleistocene||Late ('Tarantian')||Eemian interglacial, Last glacial period, ending with Younger Dryas. Toba eruption. Megafauna extinction.||0.129|
|Chibanian||High amplitude 100 ka glacial cycles. Rise of Homo sapiens.||0.774|
|Calabrian||Further cooling of the climate. Spread of Homo erectus.||1.8|
|Gelasian||Start of Quaternary glaciations. Rise of the Pleistocene megafauna and Homo habilis.||2.58|
|Neogene||Pliocene||Piacenzian||Greenland ice sheet develops. Australopithecus common in East Africa.||3.6|
|Zanclean||Zanclean flooding of the Mediterranean Basin. Cooling climate. Ardipithecus in Africa.||5.333|
|Miocene||Messinian||Messinian Event with hypersaline lakes in empty Mediterranean Basin. Moderate Icehouse climate, punctuated by ice ages and re-establishment of East Antarctic Ice Sheet; Gradual separation of human and chimpanzee ancestors. Sahelanthropus tchadensis in Africa.||7.246|
|Serravallian||Warmer during middle Miocene climate optimum. Extinctions in middle Miocene disruption.||13.82|
|Burdigalian||Orogeny in Northern Hemisphere. Start of Kaikoura Orogeny forming Southern Alps in New Zealand. Widespread forests slowly draw in massive amounts of CO2, gradually lowering the level of atmospheric CO2 from 650 ppmv down to around 100 ppmv during the Miocene. Modern mammal and bird families become recognizable. Horses and mastodons diverse. Grasses become ubiquitous. Ancestor of apes, including humans.||20.44|
|Paleogene||Oligocene||Chattian||Grande Coupure extinction. Start of widespread Antarctic glaciation. Rapid evolution and diversification of fauna, especially mammals. Major evolution and dispersal of modern types of flowering plants||28.1|
|Eocene||Priabonian||Moderate, cooling climate. Archaic mammals (e.g. Creodonts, "Condylarths", Uintatheres, etc.) flourish and continue to develop during the epoch. Appearance of several "modern" mammal families. Primitive whales diversify. Reglaciation of Antarctica and formation of its ice cap; End of Laramide and Sevier Orogenies of the Rocky Mountains in North America. Orogeny of the Alps in Europe begins. Hellenic Orogeny begins in Greece and Aegean Sea.||37.8|
|Ypresian||Two transient events of global warming (PETM and ETM-2) and warming climate until the Eocene Climatic Optimum. The Azolla event decreased CO2 levels from 3500 ppm to 650 ppm, setting the stage for a long period of cooling. Indian Subcontinent collides with Asia and starts Himalayan Orogeny.||56|
|Paleocene||Thanetian||Starts with Chicxulub impact and the K-Pg extinction event. Climate tropical. Modern plants appear; Mammals diversify into a number of lineages following the extinction of the non-avian dinosaurs. First large mammals (up to bear or small hippo size). Alpine orogeny in Europe and Asia begins.||59.2|
|Mesozoic||Cretaceous||Late||Maastrichtian||Flowering plants proliferate, along with new types of insects. More modern teleost fish begin to appear. Ammonoidea, belemnites, rudist bivalves, echinoids and sponges all common. Many new types of dinosaurs (e.g. Tyrannosaurs, Titanosaurs, Hadrosaurs, and Ceratopsids) evolve on land, as do Eusuchia (modern crocodilians); and mosasaurs and modern sharks appear in the sea. Birds toothed and toothless coexist with pterosaurs. Monotremes, marsupials and placental mammals appear. Break up of Gondwana. Beginning of Laramide and Sevier Orogenies of the Rocky Mountains. atmospheric CO2 close to present-day levels.||72.1 ± 0.2|
|Campanian||83.6 ± 0.2|
|Santonian||86.3 ± 0.5|
|Coniacian||89.8 ± 0.3|
|Jurassic||Late||Tithonian||Gymnosperms (especially conifers, Bennettitales and cycads) and ferns common. Many types of dinosaurs, such as sauropods, carnosaurs, and stegosaurs. Mammals common but small. First birds and lizards. Ichthyosaurs and plesiosaurs diverse. Bivalves, Ammonites and belemnites abundant. Sea urchins very common, along with crinoids, starfish, sponges, and terebratulid and rhynchonellid brachiopods. Breakup of Pangaea into Gondwana and Laurasia. Nevadan orogeny in North America. Rangitata and Cimmerian orogenies taper off. Atmospheric CO2 levels 3–4 times the present day levels (1200–1500 ppmv, compared to today's 400 ppmv).||152.1 ± 0.9|
|Kimmeridgian||157.3 ± 1.0|
|Oxfordian||163.5 ± 1.0|
|Middle||Callovian||166.1 ± 1.2|
|Bathonian||168.3 ± 1.3|
|Bajocian||170.3 ± 1.4|
|Aalenian||174.1 ± 1.0|
|Early||Toarcian||182.7 ± 0.7|
|Pliensbachian||190.8 ± 1.0|
|Sinemurian||199.3 ± 0.3|
|Hettangian||201.3 ± 0.2|
|Triassic||Late||Rhaetian||Archosaurs dominant on land as dinosaurs and in the air as pterosaurs. Ichthyosaurs and nothosaurs dominate large marine fauna. Cynodonts become smaller and more mammal-like, while first mammals and crocodilia appear. Dicroidiumflora common on land. Many large aquatic temnospondyl amphibians. Ceratitic ammonoids extremely common. Modern corals and teleost fish appear, as do many modern insect clades. Andean Orogeny in South America. Cimmerian Orogeny in Asia. Rangitata Orogeny begins in New Zealand. Hunter-Bowen Orogeny in Northern Australia, Queensland and New South Wales ends, (c. 260–225 Ma)||~208.5|
|Induan||251.902 ± 0.06|
|Paleozoic||Permian||Lopingian||Changhsingian||Landmasses unite into supercontinent Pangaea, creating the Appalachians. End of Permo-Carboniferous glaciation. Synapsids including (pelycosaurs and therapsids) become plentiful, while parareptiles and temnospondyl amphibians remain common. In the mid-Permian, coal-age flora are replaced by cone-bearing gymnosperms (the first true seed plants) and by the first true mosses. Beetles and flies evolve. Marine life flourishes in warm shallow reefs; productid and spiriferid brachiopods, bivalves, forams, and ammonoids all abundant. Permian-Triassic extinction event occurs 251 Ma: 95% of life on Earth becomes extinct, including all trilobites, graptolites, and blastoids. Ouachita and Innuitian orogenies in North America. Uralian orogeny in Europe/Asia tapers off. Altaid orogeny in Asia. Hunter-Bowen Orogeny on Australian continent begins (c. 260–225 Ma), forming the MacDonnell Ranges.||254.14 ± 0.07|
|Wuchiapingian||259.1 ± 0.4|
|Guadalupian||Capitanian||265.1 ± 0.4|
|Wordian||268.8 ± 0.5|
|Roadian||272.95 ± 0.5|
|Cisuralian||Kungurian||283.5 ± 0.6|
|Artinskian||290.1 ± 0.26|
|Sakmarian||295 ± 0.18|
|Asselian||298.9 ± 0.15|
|Carbon- iferous||Pennsylvanian||Gzhelian||Winged insects radiate suddenly; some (esp. Protodonata and Palaeodictyoptera) are quite large. Amphibians common and diverse. First reptiles and coal forests (scale trees, ferns, club trees, giant horsetails, Cordaites, etc.). Highest-ever atmospheric oxygen levels. Goniatites, brachiopods, bryozoa, bivalves, and corals plentiful in the seas and oceans. Testate forams proliferate. Uralian orogeny in Europe and Asia. Variscan orogeny occurs towards middle and late Mississippian Periods.||303.7 ± 0.1|
|Kasimovian||307 ± 0.1|
|Moscovian||315.2 ± 0.2|
|Bashkirian||323.2 ± 0.4|
|Mississippian||Serpukhovian||Large primitive trees, first land vertebrates, and amphibious sea-scorpions live amid coal-forming coastal swamps. Lobe-finned rhizodonts are dominant big fresh-water predators. In the oceans, early sharks are common and quite diverse; echinoderms (especially crinoids and blastoids) abundant. Corals, bryozoa, goniatites and brachiopods (Productida, Spiriferida, etc.) very common, but trilobites and nautiloids decline. Glaciation in East Gondwana. Tuhua Orogeny in New Zealand tapers off.||330.9 ± 0.2|
|Viséan||346.7 ± 0.4|
|Tournaisian||358.9 ± 0.4|
|Devonian||Late||Famennian||First clubmosses, horsetails and ferns appear, as do the first seed-bearing plants (progymnosperms), first trees (the progymnosperm Archaeopteris), and first (wingless) insects. Strophomenid and atrypid brachiopods, rugose and tabulate corals, and crinoids are all abundant in the oceans. Goniatite ammonoids are plentiful, while squid-like coleoids arise. Trilobites and armoured agnaths decline, while jawed fishes (placoderms, lobe-finned and ray-finned fish, and early sharks) rule the seas. First tetrapods still aquatic. "Old Red Continent" of Euramerica. Beginning of Acadian Orogeny for Anti-Atlas Mountains of North Africa, and Appalachian Mountains of North America, also the Antler, Variscan, and Tuhua Orogeny in New Zealand.||372.2 ± 1.6|
|Frasnian||382.7 ± 1.6|
|Middle||Givetian||387.7 ± 0.8|
|Eifelian||393.3 ± 1.2|
|Early||Emsian||407.6 ± 2.6|
|Pragian||410.8 ± 2.8|
|Lochkovian||419.2 ± 3.2|
|Silurian||Pridoli||First vascular plants (the rhyniophytes and their relatives), first millipedes and arthropleurids on land. First jawed fishes, as well as many armoured jawless fish, populate the seas. Sea-scorpions reach large size. Tabulate and rugose corals, brachiopods (Pentamerida, Rhynchonellida, etc.), and crinoids all abundant. Trilobites and mollusks diverse; graptolites not as varied. Beginning of Caledonian Orogeny for hills in England, Ireland, Wales, Scotland, and the Scandinavian Mountains. Also continued into Devonian period as the Acadian Orogeny, above. Taconic Orogeny tapers off. Lachlan Orogeny on Australian continent tapers off.||423 ± 2.3|
|Ludlow||Ludfordian||425.6 ± 0.9|
|Gorstian||427.4 ± 0.5|
|Wenlock||Homerian||430.5 ± 0.7|
|Sheinwoodian||433.4 ± 0.8|
|Llandovery||Telychian||438.5 ± 1.1|
|Aeronian||440.8 ± 1.2|
|Rhuddanian||443.8 ± 1.5|
|Ordovician||Late||Hirnantian||Invertebrates diversify into many new types (e.g., long straight-shelled cephalopods). Early corals, articulate brachiopods (Orthida, Strophomenida, etc.), bivalves, nautiloids, trilobites, ostracods, bryozoa, many types of echinoderms (crinoids, cystoids, starfish, etc.), branched graptolites, and other taxa all common. Conodonts (early planktonic vertebrates) appear. First green plants and fungi on land. Ice age at end of period.||445.2 ± 1.4|
|Katian||453 ± 0.7|
|Sandbian||458.4 ± 0.9|
|Middle||Darriwilian||467.3 ± 1.1|
|Dapingian||470 ± 1.4|
|477.7 ± 1.4|
|Tremadocian||485.4 ± 1.9|
|Cambrian||Furongian||Stage 10||Major diversification of life in the Cambrian Explosion. Numerous fossils; most modern animal phyla appear. First chordates appear, along with a number of extinct, problematic phyla. Reef-building Archaeocyatha abundant; then vanish. Trilobites, priapulid worms, sponges, inarticulate brachiopods (unhinged lampshells), and numerous other animals. Anomalocarids are giant predators, while many Ediacaran fauna die out. Prokaryotes, protists (e.g., forams), fungi and algae continue to present day. Gondwana emerges. Petermann Orogeny on the Australian continent tapers off (550–535 Ma). Ross Orogeny in Antarctica. Delamerian Orogeny (c. 514–490 Ma) and Lachlan Orogeny (c. 540–440 Ma) on Australian continent. Atmospheric CO2 content roughly 15 times present-day (Holocene) levels (6000 ppmv compared to today's 400 ppmv)||~489.5|
|Series 2||Stage 4||~514|
|Fortunian||~541 ± 1.0|
|Precambrian||Proterozoic||Neoproterozoic||Ediacaran||Good fossils of the first multi-celled animals. Ediacaran biota flourish worldwide in seas. Simple trace fossils of possible worm-like Trichophycus, etc. First sponges and trilobitomorphs. Enigmatic forms include many soft-jellied creatures shaped like bags, disks, or quilts (like Dickinsonia). Taconic Orogeny in North America. Aravalli Range orogeny in Indian Subcontinent. Beginning of Petermann Orogeny on Australian continent. Beardmore Orogeny in Antarctica, 633–620 Ma.||~635|
|Cryogenian||Possible "Snowball Earth" period. Fossils still rare. Rodinia landmass begins to break up. Late Ruker / Nimrod Orogeny in Antarctica tapers off.||~720|
|Tonian||Rodinia supercontinent persists. Sveconorwegian orogeny ends. Trace fossils of simple multi-celled eukaryotes. First radiation of dinoflagellate-like acritarchs. Grenville Orogeny tapers off in North America. Pan-African orogeny in Africa. Lake Ruker / Nimrod Orogeny in Antarctica, 1,000 ± 150 Ma. Edmundian Orogeny (c. 920 – 850 Ma), Gascoyne Complex, Western Australia. Deposition of Adelaide Superbasin and Centralian Superbasin begins on Australian continent.||1000|
|Mesoproterozoic||Stenian||Narrow highly metamorphic belts due to orogeny as Rodinia forms. Sveconorwegian orogeny starts. Late Ruker / Nimrod Orogeny in Antarctica possibly begins. Musgrave Orogeny (c. 1,080 Ma), Musgrave Block, Central Australia.||1200|
|Ectasian||Platform covers continue to expand. Green algae colonies in the seas. Grenville Orogeny in North America.||1400|
|Calymmian||Platform covers expand. Barramundi Orogeny, McArthur Basin, Northern Australia, and Isan Orogeny, c.1,600 Ma, Mount Isa Block, Queensland||1600|
|Paleoproterozoic||Statherian||First complex single-celled life: protists with nuclei, Francevillian biota. Columbia is the primordial supercontinent. Kimban Orogeny in Australian continent ends. Yapungku Orogeny on Yilgarn craton, in Western Australia. Mangaroon Orogeny, 1,680–1,620 Ma, on the Gascoyne Complex in Western Australia. Kararan Orogeny (1,650 Ma), Gawler Craton, South Australia.||1800|
|Orosirian||The atmosphere becomes oxygenic. Vredefort and Sudbury Basin asteroid impacts. Much orogeny. Penokean and Trans-Hudsonian Orogenies in North America. Early Ruker Orogeny in Antarctica, 2,000–1,700 Ma. Glenburgh Orogeny, Glenburgh Terrane, Australian continent c. 2,005–1,920 Ma. Kimban Orogeny, Gawler craton in Australian continent begins.||2050|
|Rhyacian||Bushveld Igneous Complex forms. Huronian glaciation.||2300|
|Siderian||Oxygen catastrophe: banded iron formations forms. Sleaford Orogeny on Australian continent, Gawler Craton 2,440–2,420 Ma.||2500|
|Archean||Neoarchean||Stabilization of most modern cratons; possible mantle overturn event. Insell Orogeny, 2,650 ± 150 Ma. Abitibi greenstone belt in present-day Ontario and Quebec begins to form, stabilizes by 2,600 Ma.||2800|
|Mesoarchean||First stromatolites (probably colonial cyanobacteria). Oldest macrofossils. Humboldt Orogeny in Antarctica. Blake River Megacaldera Complex begins to form in present-day Ontario and Quebec, ends by roughly 2,696 Ma.||3200|
|Paleoarchean||First known oxygen-producing bacteria. Oldest definitive microfossils. Oldest cratons on Earth (such as the Canadian Shield and the Pilbara Craton) may have formed during this period. Rayner Orogeny in Antarctica.||3600|
|Eoarchean||Simple single-celled life (probably bacteria and archaea). Oldest probable microfossils. The first life forms and self-replicating RNA molecules evolve around 4,000 Ma, after the Late Heavy Bombardment ends on Earth. Napier Orogeny in Antarctica, 4,000 ± 200 Ma.||~4000|
|Hadean||Early Imbrian (Neohadean) (unofficial)||Indirect photosynthetic evidence (e.g., kerogen) of primordial life. This era overlaps the beginning of the Late Heavy Bombardment of the Inner Solar System, produced possibly by the planetary migration of Neptune into the Kuiper belt as a result of orbital resonances between Jupiter and Saturn. Oldest known rock (4,031 to 3,580 Ma).||4130|
|Nectarian (Mesohadean) (unofficial)||Possible first appearance of plate tectonics. This unit gets its name from the lunar geologic timescale when the Nectaris Basin and other greater lunar basins form by big impact events. Earliest evidence for life based on unusually high amounts of light isotopes of carbon, a common sign of life.||4280|
|Basin Groups (Paleohadean) (unofficial)||End of the Early Bombardment Phase. Oldest known mineral (Zircon, 4,404 ± 8 Ma). Asteroids and comets bring water to Earth.||4533|
|Cryptic (Eohadean) (unofficial)||Formation of Moon (4,533 to 4,527 Ma), probably from giant impact, since the end of this era. Formation of Earth (4,570 to 4,567.17 Ma), Early Bombardment Phase begins. Formation of Sun (4,680 to 4,630 Ma) .||4600|
Proposed Precambrian timeline
The ICS's Geologic Time Scale 2012 book which includes the new approved time scale also displays a proposal to substantially revise the Precambrian time scale to reflect important events such as the formation of the Earth or the Great Oxidation Event, among others, while at the same time maintaining most of the previous chronostratigraphic nomenclature for the pertinent time span.
(See also Period (geology)#Structure.)
- Hadean Eon – 4600–4031 Ma
- Chaotian Era – 4600–4404 Ma – the name alluding both to the mythological Chaos and the chaotic phase of planet formation
- Jack Hillsian or Zirconian Era – 4404–4031 Ma – both names allude to the Jack Hills Greenstone Belt which provided the oldest mineral grains on Earth, zircons
- Archean Eon – 4031–2420 Ma
- Paleoarchean Era – 4031–3490 Ma
- Acastan Period – 4031–3810 Ma – named after the Acasta Gneiss
- Isuan Period – 3810–3490 Ma – named after the Isua Greenstone Belt
- Mesoarchean Era – 3490–2780 Ma
- Vaalbaran Period – 3490–3020 Ma – based on the names of the Kapvaal (Southern Africa) and Pilbara (Western Australia) cratons
- Pongolan Period – 3020–2780 Ma – named after the Pongola Supergroup
- Neoarchean Era – 2780–2420 Ma
- Proterozoic Eon – 2420–541 Ma
- Paleoproterozoic Era – 2420–1780 Ma
- Oxygenian Period – 2420–2250 Ma – named for displaying the first evidence for a global oxidizing atmosphere
- Jatulian or Eukaryian Period – 2250–2060 Ma – names are respectively for the Lomagundi–Jatuli δC isotopic excursion event spanning its duration, and for the (proposed) first fossil appearance of eukaryotes
- Columbian Period – 2060–1780 Ma – named after the supercontinent Columbia
- Mesoproterozoic Era – 1780–850 Ma
- Neoproterozoic Era – 850–541 Ma
Shown to scale:
Compare with the current official timeline, not shown to scale:
Credits to the contents of this page go to the authors of the corresponding Wikipedia page: en.wikipedia.org/wiki/Geologic time scale.