Paleo / geological time scale

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Overview in proportional representation. On the left the eons are shown with selected subdivisions. Periods from polar to planetary glaciations are marked with triangles. The further the triangle extends to the right, the closer the glaciation came to the equator.

The following is a detailed tabular overview of the history of the earth . The tables are structured according to the geological time scale , provided with numerical age information and list striking geological and evolutionary events as well as typical key fossils for each level . Each of the four eons ( Phanerozoic , Proterozoic , Archean , Hadaic ) is dealt with in a separate section with its own table. For each geological period there is a fold-out overview in the corresponding header.

The great table of the geological ages

The Phanerozoic Eon

The Phanerozoic was named as the “Aeon of Visible Fossils” ( ), because for a long time only fossils were known from this Aeon. Today, however, much older fossils are known that can be examined with a microscope or imaging methods .

  • Duration 543,000,000 years
  • Time span 0 to 543 mya

It is divided into three eras:

General

Five major mass extinctions occurred in the Phanerozoic :

There were four major mountain-building phases:

Table of the Phanerozoic

period epoch step Events Beginning

Cenozoic in general

The New Earth Era begins at 65.5 mya and continues to this day.

quaternary

Quaternary

Fourth
Age

 Holocene

The
Current
Epoch

Geology: In Northern Europe there are repeated transgression on the northern coast through the North Atlantic, Flanders transgression (up to approx. 5,000 BC), the Calais transgression (up to approx. 1000 BC) and the Dunkirk transgression (lasts today still on). Towards the end, local remodeling of the uppermost geological layers by mankind through mining, removal of fossil carbon deposits .
Climate: End of the last glacial period 10,000 years ago. Towards the present, CO 2 input by humans, accelerated warming of the earth's atmosphere .
Flora: Worldwide mixing of the flora, distribution of neophytes . Accelerating the evolution of crops through selection and genetic engineering . Decline in forest cover on all continents.
Fauna: Humans dominate the vertebrate fauna. Extinction of large glacial mammals. Mixing of the animal world, breeding of domestic animals .
from
9,500
BC Chr.
Pleistocene

ice age
also Diluvium

younger
ice age
Homo
sapiens

 Young Pleistocene
Geology:
Climate: Beginning of the last glacial period 115,000 years ago
Flora:
Fauna: the modern man (Homo sapiens) , Mammuthus primigenius (woolly mammoth)
from
0.126
mya
Middle Pleistocene
Geology:
Climate: Riss glacial period 230,000–130,000 years ago, Mindel glacial period 350,000–250,000 years ago, Günz glacial period ago 640,000–540,000 years ago, interrupted by warm periods, see also climate history .
Flora:
Fauna: Mammuthus trogontherii (steppe mammoth)

probably separation of the lines of Homo sapiens and Neanderthals

from
0.781
mya
Old Pleistocene
Geology:
Climate:
Flora:
Fauna: Mammuthus meridionalis (Archidiskodon, southern elephant)
from
1,806
mya
Gelasium
Geology:
Climate:
Flora:
Fauna: Real elephants ( Deinotheria ), settle worldwide (except Australia )
from
2.588
mya

Neogene in general
Neogen

New
period

outdated
designation:
younger
part of
the Tertiary 		Pliocene

grasses
dominate

steppe
savannahs

pre-human

Australo-
Pithecus
in
eastern
Africa 		Piacenzium
Geology:
Climate:
Flora:
Fauna:
from
3,600
mya
Zancleum

parts of
the
Pannon
Geology:
Climate:
Flora:
Fauna: Mastodons distributed worldwide 5 million years ago (except Australia ), first hominini from approx. 4 mya
from
5,332
mya
Miocene

dry
climate

steppes

savannas

mod.
Large mammals 		Messinium

parts of
the
Pannon
Geology: The Mediterranean dries up briefly (so-called salinity crisis), as the sea level sinks by approx. 50 meters due to icing at the South Pole.
Climate:
Flora:
Fauna:
from
7,246
mya
Tortonium
Geology:
Climate:
Flora:
Fauna:
from
11.608
mya
Serravallium
Geology:
Climate:
Flora:
Fauna: Beginning of the development of the real elephant Primelephas ,
from
13.82
mya
Langhium
Geology:
Climate:
Flora:
Fauna:
from
15.97
mya
Burdigalium
Geology:
Climate:
Flora:
Fauna:
from
20.43
mya
Aquitanium
Geology:
Climate:
Flora:
Fauna:
from
23.03
mya

Paleogene

Paleogene

Old
Period

Obsolete
name:
older
part of
the Tertiary 		Oligocene

large
mammals

first
whales 		Chattium
Geology:
Climate:
Flora:
Fauna:
from
28.4
(± 0.1)
mya
Rupelium
Geology:
Climate:
Flora:
Fauna: Large mammals evolve, palaeomastodon
from
33.9
(± 0.1)
mya
Eocene

dawn
epoch

warm, humid
climate

vast
forest areas

many
small
mammals

large
birds of prey 		Priobonium
Geology:
Climate:
Flora:
Fauna: First geese birds
from
37.2
(± 0.1)
mya
Bartonium
Geology: The Himalayas emerge
Climate:
Flora:
Fauna: Mesohippus
from
40.4
(± 0.2)
mya
lutetium
Geology:
Climate:
Flora:
Fauna: Brontotherium , Palaeotherium
from
48.6
(± 0.2)
mya
Ypresium
Geology:
Climate:
Flora:
Fauna: First proboscis , Moeritherium
from
55.8
(± 0.2)
mya
Paleocene

primitive
era

dinosaur
extinct

post-
effects
of an
asteroid
strike 		Thanetium
Geology:
Climate:
Flora:
Fauna: First equine relatives ( Hyracotherium ).
from
58.7
(± 0.2)
mya
Seelandium
Geology:
Climate:
Flora:
Fauna: giant birds like Gastornis .
from
61.1
(± 0.2)
mya
Danium
Geology:
Climate:
Flora:
Fauna: 65 mya Saurischia are disappearing, including theropods such as Tyrannosaurus rex , Gallimimus . Belemnites are disappearing.
from
65.5
(± 0.3)
mya

Mesozoic era in general

The Mesozoic Ages begin 251.0 (± 0.4) and end 65.5 (± 0.3) mya . The mesophytic course deviates from this.

Mesophytic key fossils: dominance of gymnosperms ,cycads ( Cycadophyta ), conifers , ginkgo family ( Glossophyllum ), ferns ( Glossopteris ).

Chalk in general
Chalk Chalk

period

Named
after the
deposits
of
chalk 		Upper
Cretaceous

Younger
Cretaceous
Era 		Maastricht
Geology: The North Atlantic is approx. 4000 kilometers wide. In Central Europe regression, mainland arises.
Climate:
Flora: Rudists are dying out again and are being replaced by the corals as reef builders
Fauna: time of the Tyrannosaurus rex , belemnites die out from 65 mya
from
70.6
(± 0.6)
mya
Campanium
Geology:
Climate:
Flora:
Fauna: The Parasaurolophus appears, 83 mya dies out, 65 mya again. Quetzalcoatlus appears with a wingspan of 12 meters, probably dies out again before the border with the Cenozoic era due to the emerging birds .
from
83.5
(± 0.7)
mya
Santonium
Geology:
Climate:
Flora:
Fauna: 85-83.5 mya: Gallimimus appears
from
85.8
(± 0.7)
mya
Coniacium
Geology: Senon transgression : sea level is 100–300 m above today's level, sandstones formed in coastal areas of Central Europe, further inland Pläner-Mergel (Lower Saxony) and Emscher Mergel (Westphalia).
Climate:
Flora:
Fauna:
from
89.3
(± 1.0)
mya
Turonium
Geology: Middle Cretaceous transgression creates a continuous connection between the Tethys and the North Sea via the Paris Basin and southern England, the northern flank of the Rhenish massif is flooded, formation of 1500 m thick chalk sediments
Climate:
Flora:
Fauna: rudists come and solve temporarily the coral in the reef formation from.
from
93.6
(± 0.8)
mya
Cenomanium
Geology: The water circulation in the Atlantic basin is restricted, bituminous limestone is formed under anoxic conditions
Climate: Warm, proven average surface temperature of 23 ° C
Flora: large foraminifera
Fauna:
from
99.6
(± 0.9)
mya
Lower
Cretaceous

older
Cretaceous
epoch 		Albium
Geology: The water circulation in the Atlantic basin is restricted, under anoxic conditions bituminous limestone forms, continental separation from South America and Africa in full swing, the sea initially transgresses from the south and finally creates a connection to the North Atlantic .
Climate:
Flora: beginning of the cenophytic
Fauna: Heteromorphic ammonites with bizarre shells are dying out again
from
112.0
(± 1.0)
mya
Aptium
Geology: South America begins to separate from Africa, initially a narrow basin without connection to the north emerges, formation of plateau basalts (Parana basins)
Climate:
Flora:
Fauna: feathered dinosaurs : microraptor
from
125.0
(± 1.0)
mya
Barremium
Geology:
Climate:
Flora:
Fauna:
from
130.0
(± 1.5)
mya
Skin rivium
Geology:
Climate:
Flora:
Fauna:
from
133.9
(± 2.0)
mya
Valanginium
Geology:
Climate:
Flora: Rock formers : red algae ( Corallina ) and green algae ( Codiaceae with Halimeda )
Fauna:
from
140.2
(± 3.0)
mya
Berriasium
Geology: Neokom-Transgression : North Sea is transgressing the Wealdensenken , in the Salzgitter area rubble iron ores are produced, debris in front of the Central German Landschwelle ( Hils- und Osningsandstein ). Pangea is finally falling apart.
Climate:
Flora: Continental and brackish - limnic deposits with coal seams (Wealden coal) are formed. Undoubtedly developed bedecktsamer ( angiosperms ).
Fauna:
from
145.5
(± 4.0)
mya

Law in general
Jura

Named
after
the
Jura mountains 		Upper
Jura

Malm

White
Jura 		Tithonium

also
Portlandium
(obsolete)
Geology: regression of Central Europe, the sea is receding
Climate:
Flora: The first flowering plants emerge from a branch of the naked tree
Fauna: 150 mya Archeopteryx (primeval bird) with feathers and skeleton well developed
from
150.8
(± 4.0)
mya
Kimmeridgium
Geology: orogeny around the Pacific begins (Zirkumpazifische orogeny or Cimmerian folding). Start of subduction of the Pacific plates under the western edge of South America, start of the folding of the Andes .
Climate: Climate is changing fundamentally. In the interior of Pangea no longer so dry, snowfalls occur, longer periods of frost in the polar regions. Towards the Cretaceous, more balanced and warm and moist. No icing in Germany.
Flora:
Fauna: Strong reef and carbonate formation , hexacorals , mussels , terebratels , crinoids and pentameric echinoderms .

155.6
(± 4.0)
mya
Oxfordium
Geology:
Climate: Climate continues to become increasingly drier.
Flora:
Fauna:
from
161.2
(± 4.0)
mya
Middle
Jura

Dogger

Brown
Jura 		Callovium
Geology:
Climate:
Flora:
Fauna:
from
164.7
(± 4.0)
mya
Bathonium
Geology:
Climate:
Flora:
Fauna:
from
167.7
(± 3.5)
mya
Bajocium
Geology:
Climate: No clearly differentiated climate zones
Flora:
Fauna:
from
171.6
(± 3.0)
mya
Aalenium
Geology:
Climate: No clearly differentiated climate zones
Flora:
Fauna:
from
175.6
(± 2.0)
mya
Lower
Jura

Lias

Black
Jura 		Toarcium
Geology:
Climate:
Flora:
Fauna:
from
183.0
(± 1.5)
mya
Pliensbachium
Geology:
Climate: In the interior of Pangea extremely dry and extremely hot.
Flora:
Fauna:
from
189.6
(± 1.5)
mya
Sinemurium
Geology:
Climate: In the interior of Pangea extremely dry and extremely hot.
Flora:
Fauna:
from
196.5
(± 1.0)
mya
Hettangium
Geology:
Climate: In the interior of Pangea extremely dry and extremely hot.
Flora:
Fauna: The radiation common after a mass extinction , dinosaurs become the dominant land vertebrates
from
199.6
(± 0.6)
mya

Triad
Trias

Named
as the
three-part
period 		Upper
triad

outdated:
Keuper 		Rhaetium
Geology: In the Germanic Basin renewed transgression
Climate: In the inner areas of Pangea extremely dry and hot, climate is changing due to the break-up of the continent.
Flora: Probably the first ancestors of angiosperms , gymnosperms still dominate.
Fauna: Great mass extinction , the archosaurs lose their dominant position
from
203.6
(± 1.5)
mya
Norium
Geology: In the Germanic Basin the sea level is falling, silting up with the delivery of sediments from the north, the Lettenkohlenkuper and the Gypsumkeuper were formed .
Climate: In the inner areas of Pangea extremely dry and hot, polar caps ice-free.
Flora:
Fauna: Dinosaurs evolve, ichthyosaurs and pterosaurs , therapsids develop into mouse-sized mammals. In the Tethys large reef formation through new coral groups ( Scleractinia ). First turtles , plaster-tooth lizards Placodus and Henodus in the sea. Sea lilies , mussels and brachiopods , including the first terebratulida , and ammonites of the genus Ceratites .
from
216.5
(± 2.0)
mya
Carnium
Geology: Pangea begins to break up, the North Atlantic emerges, and over time a massive rift forms between North America and Northwest Africa. Central and southwestern Europe covered with water, carbonate rocks , reef rocks and evaporites are formed that make up the Swabian Alb , Limestone Alps and the Dolomites today. Analogous to this are the rocks in Asia Minor , Himalaya and Indochina . Mountain formation begins on the Pacific coast of North America, severe volcanism. No ice on the continents.
Climate: In the inner areas of Pangea extremely dry and hot, polar caps ice-free.
Flora:
Fauna: Especially animals of the equatorial Tethys penetrate westwards.
from
228.7
(± 2.0)
mya
Middle
Triassic

outdated:
Muschelkalk 		Ladinium
Geology: The Germanic Basin deposits large amounts of Trochite and Ceratite limestone .
Climate: In the inner areas of Pangea extremely dry and hot, polar caps ice-free.
Flora:
Fauna: 230 mya theropods appear and remain dominant until the end of the Cretaceous Period
from
237.0
(± 2.0)
mya
Anisium
Geology: The Germanic Basin experiences a transgression of the Tethys with the formation of corrugated limestone and thin-layer limestones , rich deposits of mussel and brachiopod limestone
Climate: In the inner areas of Pangea extremely dry and hot, polar caps ice-free.
Flora:
Fauna:
from
245.0
(± 1.5)
mya
Lower
Triassic

outdated:
colored
sandstone 		Olenekium
Geology:
Climate: In the inner areas of Pangea extremely dry and hot, polar caps ice-free.
Flora:
Fauna:
from
249.5
(± 0.7)
mya
Indusium
Geology:
Climate: In the inner areas of Pangea extremely dry and hot, in Central Europe, which was then by the sea, a semi-arid climate. Ice-free polar caps.
Flora:
Fauna: After the mass extinction in the Permian, radiation occurs , the synapsids experience a final bloom in the following period, descendants of the great primordial amphibians ( stegocephalies ) emerge: mastodonsaurus and the chirotherium ("hand animal").
from
251.0
(± 0.4)
mya

Paleozoic in general

The age of the earth begins 542.0 (± 1.0) and ends 251.0 (± 0.4) mya .

Perm in general
Perm

Named
after:
the city of
Perm

outdated
designation
in Germany:
Dyas
divided into:
Zechstein
257.3–251

and

Rotliegend
302–257.3 		Upper
Permian
Lopingium 		Changhsingium
Geology: approx. 250 mya extrusion of continental plateau basalts in Siberia , presumably a cause of the mass extinction at the end of the Permian.
Climate:
Flora:
Fauna: largest mass extinction in the history of the earth, 75–90% of all marine species, u. a. the trilobites and the unicellular fusulins finally die out, the paleoammonoidea are replaced by the ceratites . 20 Therapsid families are dying out.
from
253.8
(± 0.7)
mya
Wuchiapingium
Geology: Central Europe is flooded by five partial transgressions from the Zechstein Sea , which penetrates the continental plate and deposits large amounts of salt (layers up to 1000 meters thick) by the end of the Permian. Mansfeld copper slate , marine lime deposits in southern Europe. Ural folds up.
Climate: The climate is getting warmer, the glaciers begin to shrink, but drift ice continues until the end of the Permian.
Flora:
Fauna:
from
260.4
(± 0.7)
mya
Middle
Permian
Guadalupian 		Capitanium
Geology:
Climate:
Flora: beginning of the mesophytic (dominance of gymnosperms).
Fauna:
from
265.8
(± 0.7)
mya
Wordium
Geology:
Climate:
Flora:
Fauna:
from
268.0
(± 0.7)
mya
Roadium
Geology:
Climate:
Flora:
Fauna:
from
270.6
(± 0.7)
mya
Lower
Permian
Cisuralium 		Kungurium
Geology:
Climate:
Flora:
Fauna:
from
275.6
(± 0.7)
mya
Artinskium
Geology:
Climate:
Flora:
Fauna:
from
284.4
(± 0.7)
mya
Sacmarium
Geology:
Climate:
Flora:
Fauna:
from
294.6
(± 0.8)
mya
Asselium
Geology:
Climate:
Flora: The first coniferous forests are emerging and pushing back the carbon-forming plant groups of the Carboniferous, which are becoming increasingly small.
Fauna:
from
299.0
(± 0.8)
mya

Carbon
Karbon

Named
after
then
fossiliertem
carbon

outdated
sub-
division into
( Silesium )
and
( dinantian ) 		Penny-
sylvanium
Upper
Carbon 		Upper
Penn
sylvanium 		Gzhelium
Geology:
Climate: Permo-Carboniferous glaciation , strong climatic contrasts , partial glaciation of Africa, India, Australia and Antarctica, Central Europe lies in the tropical belt. Falling sea level.
Flora: The forests consist increasingly of seed ferns ( Glossopteris ), horsetail ( Calamites ), bear moss family ( Lepidodendron , Sigillaria ) and conifers ( Gymnosperms ).
Fauna:
from
303.4
(± 0.9)
mya
Kasimovium
Geology: Due to the Variscan orogeny , parts of Europe become mainland.
Climate:
Flora:
Fauna:
from
307.2
(± 1.0)
mya
Medium
Penny-
sylvanium 		Moskovium
Geology:
Climate:
Flora:
Fauna:
from
311.7
(± 1.1)
mya
Lower
Penn
sylvanium 		Bashkirium
Geology:
Climate:
Flora:
Fauna:
from
318.1
(± 1.3)
mya
Mississ-
ippium
sub
karbon 		Upper
Mississ-
ippium 		Serpukhovium
Geology: Variscan orogeny is at its peak. In several phases, an approx. 500 km wide mountain range forms, which runs through all of Western and Central Europe, from Spain to Poland.
Climate: Tropical climate along the equator, but also glaciations in the Upper Carboniferous.
Flora: Paleophytic (age of the fern plants), especially in the Upper Carboniferous tropical swamps and coastal moors, huge tropical rainforests that led to the formation of coal, seed plants and spore plants side by side, mainland completely covered by plants
Fauna: Goniatites , conodonts , large foraminifera , corals , brachiopods
from
328.3
(± 1.6)
mya
Middle
Mississ-
ippium 		Visa
Geology:
Climate:
Flora:
Fauna:
from
345.3
(± 2.1)
mya
Lower
abuse
issippium 		Tournaisium
Geology: mainland swell between Laurussia and Gondwana . (Franco-Alemannic-Bohemian Country, Central German Crystalline Threshold , Norman Threshold ). Shelf Sea over the British Isles.
Climate:
Flora:
Fauna:
from
359.2
(± 2.5)
mya

Devonian in general
Devon

Named
after the
county of
Devonshire 		Upper
Devonian 		Family
Geology: Central Europe under water, the reefs sink, additional debris deposits from the silting Central German threshold . The unfolding of the Rhenish Slate Mountains begins at 370 mya . Baltica and Laurentia will be pushed together and will form a block in future ("Old Red Continent").
Climate:
Flora: Lush forests emerge, first seed plants
Fauna:
from
374.5
(± 2.6)
mya
Frasnium
Geology: Variscan mountainous formation leads to unfolding, Central Europe silts up, end of reef formation in the area of ​​today's Rhenish Slate Mountains , Harz and Eifel .
Climate:
Flora:
Fauna:
from
385.3
(± 2.6)
mya
Middle
Devonian 		Givetium
Geology:
Climate:
Flora:
Fauna:
from
391.8
(± 2.7)
mya
Eifelium
Geology: Central Europe under water, mountain heights of the Caledonian mountains largely leveled, supply of sediments to the coastal regions is decreasing, formation of extensive reefs from corals and stromatopores . In Central Europe, carbonate sediments ( reef limestone and pelagic cephalopod limestone ) are formed.
Climate:
Flora:
Fauna:
from
397.5
(± 2.7)
mya
Lower
Devonian 		Emsium
Geology: Around 400 mya Variscan mountain formation
Climate:
Flora:
Fauna: ammonites well developed around 400 mya
from
407.0
(± 2.8)
mya
Pragium
Geology:
Climate:
Flora:
Fauna:
from
411.2
(± 2.8)
mya
Lochkovium
Geology:
Climate:
Flora:
Fauna:
from
416.0
(± 2.8)
mya

Silurian in general
Silurian

Named
after
a
Celtic Silurian
tribe
in south Wales
 Pridolium no
consistent
subdivision
available yet
Geology:
Climate:
Flora:
Fauna: Ammonites begin to develop.
from
418.7
(± 2.7)
mya
Ludlow Ludfordium
Geology: The Caledonian mountain formation , which began in the Ordovician, leads to the unfolding of the Caledonian mountains .
Climate:
Flora: First primitive land plants ( Psilophyta , Urfarne ) near the coast
Fauna: first arthropods near the coast and shore
from
421.3
(± 2.6)
mya
Gorstium
Geology:
Climate:
Flora:
Fauna:
from
422.9
(± 2.5)
mya
Wenlock Homerium
Geology:
Climate:
Flora:
Fauna:
from
426.2
(± 2.4)
mya
Sheinwood
Geology:
Climate:
Flora:
Fauna:
from
428.2
(± 2.3)
mya
Llandovery Telychium
Geology:
Climate:
Flora:
Fauna: The number of genus graptolites is falling, but not their frequency.
from
436.0
(± 1.9)
mya
Aeronium
Geology:
Climate:
Flora:
Fauna:
from
439.0
(± 1.8)
mya
Rhuddanium
Geology:
Climate:
Flora:
Fauna: The first placodermi (tank fish) appear, die out again 50 million years later
from
443.7
(± 1.5)
mya

Ordovician general
Ordovician

Named
after
a
Celtic
tribe
in Wales
Ordovician 		Upper
Ordovician 		Brain antium
Geology:
Climate: Upper Ordovician glaciation
Flora:
Fauna: Large fauna incessions in which mainly benthonic shallow water groups such as the trilobites and brachiopods participate. Also Orthiden , strophomenida and Pentameriden experience a wide cross- mass extinction .
from
445.6
(± 1.5)
mya
Katium
Geology:
Climate: Very warm worldwide, tropically humid.
Flora:
Fauna:
from
455.8
(± 1.6)
mya
Sandbium
Geology: Due to the collision of Laurentia , Fennosarmatia and Gondwana , the Caledonian mountain formation begins , but the Caledonian mountains do not fold until the Upper Silurian.
Climate: warm water, salt deposits at the equator , Gondwana at the south pole icy. Very warm worldwide, tropical humid.
Flora:
Fauna:
from
460.9
(± 1.6)
mya
Middle
Ordovician 		Darriwilium
Geology:
Climate: warm water, salt deposits at the equator, Gondwana at the South Pole icy (North Africa, today's Sahara). Very warm worldwide, tropical humid.
Flora:
Fauna: The first echinoderms radiate ( cystoids and crinoids ). Sea urchins appear sporadically, agnathes easily differentiate.
from
468.1
(± 1.6)
mya
Dapingium
Geology:
Climate: warm water, salt deposits at the equator, Gondwana at the south pole icy. Very warm worldwide, tropical humid.
Flora:
Fauna: A highlight of the diversity development in the nautilo ideas .
from
471.8
(± 1.6)
mya
Lower
Ordovician 		Floium
Geology:
Climate: warm water, salt deposits at the equator, Gondwana at the south pole icy. Very warm worldwide, tropical humid.
Flora:
Fauna: Graptolites continue to evolve, merge into the actual Graptoloidea (with monomorphic counters). End of the radiation of the articulate brachiopods , the genus numbers stabilize.
from
478.6
(± 1.7)
mya
Tremadocium
Geology:
Climate: North Africa lies on the South Pole and is covered with ice. Average temperatures are rising worldwide.
Flora:
Fauna: Creation of a wealth of new building plans through the transition from sessile to planktonic or pseudoplanktonic life, the graptolites found a completely new habitat in the open oceans, which was accompanied by an explosive development. Artikulate brachiopods experience radiation.
from
488.3
(± 1.7)
mya

Cambrian
Cambrian

Named
for
the
ancient
name
of
Wales
Cambria 		Furongium

Agnostus
Olenus 		10th stage
Geology:
Climate:
Flora:
Fauna: First tabular corals appear, first snails ( Bellerophon ) and cephalopods , primitive nautiloids , graptolites , primitive vertebrates in the sea. Strong distribution of the nautiloids with subsequent mass extinction . Mass extinction also among the trilobites.
from
≈492
mya
9th stage
Geology:
Climate:
Flora:
Fauna:
from
≈496
mya
Paibium
Geology:
Climate:
Flora:
Fauna:
from
≈499
mya
3rd series

Paradoxides 		Guzhangium
Geology:
Climate:
Flora:
Fauna:
from
≈503
mya
Drumium
Geology: continental drift unchanged, Gondwana holds together
Climate: The sea ​​level has reached a temporary high, large-scale sea ​​advances .
Flora:
Fauna: The Burgess Shale allows an insight into the living world in the middle Cambrian. Due to the favorable conservation conditions , the soft tissues of the animals have been preserved in these fossils . The first articulata , castle-bearing brachiopods with a calcitic shell, developed. Primitive echinoderm groups , initially of no significance. Brachiopods make up 33%, trilobites around 56% of the mobile fauna.
from
≈506.5
mya
5th stage
Geology: continental drift unchanged, Gondwana holds together.
Climate: The climate is humid and hot, the poles are free of ice all year round, extensive deserts on all continents, evaporite formation
Flora:
Fauna:
from
≈510
mya
2.

Olenellus series
Holmia
Redlichia 		4th stage
Geology: continental drift unchanged , Gondwana holds together.
Climate: increase in average temperature, locally hot.
Flora:
Fauna: Archaeocyathids die out again towards the end of the Lower Cambrian. Inarticulate corals dominate.
from
≈515
mya
3rd stage
Geology: Pannotia , part of the supercontinent Rodinia , continues to break down into individual parts.
Climate: cold
Flora: land uninhabited
Fauna:
from
≈521
mya
Terreneuvium

 2nd stage
Geology:
Climate:
Flora: land uninhabited
Fauna:
from
≈528
mya
Fortunium
Geology:
Climate:
Flora: land uninhabited
Fauna: Land uninhabited, in the marine area the Cambrian explosion begins at 540 mya . First, a multitude of small, hard-shelled organisms ( small shelly fauna ) appear. These organisms can only be assigned with difficulty or not at all to animal groups known today. In the rest of the (younger) Cambrian, trilobites are the predominant group. The arthropods rise at 530 mya .
from
≈542.0
(± 1.0)
mya

The Proterozoic Eon

The Proterozoic Aeon is also called the “Aeon of the unicellular” . The entire period before 542 mya is also known as the Precambrian .

  • Duration 1,958,000,000 years
  • Period of time 542 to 2,500 mya

It is divided into three eras:

Paleo- / geological overview

Originally regarded as the aeon of the unicellular cells , the first multicellular cells are also known from this eon. The living beings of this time are today - measured against their ancestors - as complex because they have organelles. The boundary between the Cambrian and the older rock strata (outdated: Precambrian ) was for a long time based on a sudden increase in fauna at the beginning of the Cambrian.

The Proterozoic is characterized by geological, climatic and biological developments of global importance.

For the mountain-building phases see also mountain-building phases at a glance .

Table of the Proterozoic

A consistent subdivision of the periods is not yet available.

Era / age period Events Beginning
Neoproterozoic
new
Proterozoikum
neo
Proterozoic

Start:
1000

End:
542
(± 1.0)
mya

Duration:
458 million 		Ediacarium

Named after the
fossil fauna of
the Ediacara
Hills in
South Australia

formerly:
Vendium
Geology:

From 0.63 bya, the fragments of the disintegrating supercontinent Rodinia began to form anew to form the last neoproterozoic supercontinent Pannotia , also Greater Gondwana, Gondwanaland or Vendia. The then still contiguous craton Kongo-Sao-Francisco was at the center of the collisions between continents and other crustal blocks. The Arab-Nubian shield , the Sahara metacraton, the cratons West Africa , Kalahari, Rio de la Plata and Amazonia (Amazon shield) are grouped around him . Laurentia , which was neighboring with Sibiria and Baltica, was also connected to the latter . Greater India ( India with NE Madagascar , Sri Lanka and the Seychelles ), Australia with East Antarctica also collided with the Congo-Sao-Francisco craton and the Sahara metacraton. Pannotia existed for a short time and from about 0.54 to 0.53 bya was already marked in places by drifting apart again and surrounded by the hypothetical Pan-African Ocean. From 0.53 bya, Laurentia, Siberia, and Baltica and other blocks moved away from the rest of the Pannotia land masses. The Iapetus Ocean spread out between these .

Central educational elements of Pannotia were the Pan-African orogeny and the South American Brasiliano orogeny, from which a multitude of individual mountain formations resulted when the oceans began to close around the continents and cratons. The Pan-African orogeny began with the unfolding of the Nazi East African orogen with the Arab-Nubian shield and the Mozambique belt on today's eastern flank of Africa in the period of 0.85 and 0.55 bya. It represented the largest continuous mountain range of the Neoproterozoic and early Cambrian. It also included the collision of Greater India, which closed the Mozambique Ocean. Between 0.57 and 0.53 bya, the OW-striking Kuunga Belt was formed as a result of the collision between East Antarctica and Greater India on the one hand, the southern end of the East African Orogen and the two cratons Kalahari and Congo-Sao-Francisco on the other. The Khomas Sea subducted between these two cratons. The Brasiliano orogeny originated from the closure of the Adamastor Ocean with the collision of West Africa and East South America.

The remaining pannotia components are called gondwana . This major continent is divided into West Gondwana and East Gondwana according to the history of Pannotia. West Gondwana consisted of the “African” and “South American” land masses, while East Gondwana comprised Greater India, Australia and East Antarctica. Gondwana is opposed to the continents Laurentia, Baltica and Sibiria. Gondwana existed as an independent continent until it was united with the supercontinent Pangea at 0.30 bya.

On the northern edge of West Gondwana, according to today's South America and Africa, formed along an active continental margin , the Terrane of Peri-Gondwana. As a result of the subduction, several magmatic island arcs were created , which developed into microcontinents or terranos. With regard to their production locations , petrographic properties and tectonothermal modifications, they can be grouped together into the Avalonia type , Armorika type , Ganderia type and Kraton type. As a result of later plate tectonic processes, rock units can be found in today's foundations of western and central Europe and parts of the east coast of North America . (See also Cadomian and Caledonian Orogeny ).

Several large impact craters , like the one , formed during this period

* Amelia Creek Crater with a central debris cone of approximately 20 × 12 km in Davenport Range National Park / Northern Australia (estimated age between 1.66 and 0.6 bya).

* Formerly up to 90 km large Acraman crater in the Grawler Ranges / Northern Australia (around 0.59 bya).

* approx. 60 km large, heavily eroded Beaverhead crater in Montana / USA (0.6 bya).

* approx. 17 km large Luizi crater in the province of Haut-Katanga / DR Congo (around 0.57 bya).

Climate:

After the end of the global cryogenium glaciation around 0.635 bya, the Gaskiers Ice Age occurred from 0.582 to 0.580 bya . Although it was a short and not a global ice age, it had a great impact on the development of life on earth (see under biology).

From about 0.60 bya the oxygen sinks were largely saturated, and the oxygen in the air rose sharply to about 12% as a result of oxygenated photosynthesis .

Biology:

Between 0.58 and 0.54 bya, the mostly primitive multicellular organisms developed , representing a macro-society and known as the Ediacara fauna . It is named after the Ediacara Hills / South Australia . They can be grouped as fossil communities in the characteristic Avalon community , White Sea community and Nama community , but can come from different localities. The Ediacaran fauna began to develop immediately after the end of the Gaskiers Ice Age .

These living beings do not or hardly resemble recent forms. They can be grouped together, like the

  • Fern-leaf-like , branched Rangeomorpha , which were fused with the ground by means of a bulb-like structure and were rigidly upright.
  • leaf-shaped, not branched Erniettomorpha , which probably lived wholly or partly in the sediment.
  • thin, disc-shaped Dickinsoniomorpha that possibly had a front and rear end and could move around.
  • Fern- frond- like arboreomorpha , which had a bulbous adhesive disc and flexible stem.
  • disc-shaped tri - radialomorpha showing three-dimensional hook-shaped ribs or arms.
  • oval to pear-shaped Kimberellomorpha , which had a single axially symmetrical (bilateral) shell plate on the back.
  • segmented bilaterialomorpha , in which the two front horseshoe-shaped segments are interpreted as a head, which may have housed primitive eyes and a mouth.
  • elongated, conical Thectardis is assigned to the sponges and had a central depression, if necessary for water filtration.
  • tubular skeletal fossils that had curved tubular or funnel-shaped shells.
  • Trace fossils such as Aspidella (syn. Cyclomedusa) and Treptichnus pedum , which left traces of unknown organisms.
from
≈635
mya
Cryogenium

Named as the
frozen period
Geology:

By 0.72 bya the supercontinent of Rodinia had largely fallen apart. Between western Australia with eastern Antarctica , southern China and the northern flank of Laurentia , the Panthalassa Ocean began to open, while the Mirovia Ocean subducted . Rodinia had largely disintegrated again. Extensive lava flows and volcanic eruptions have been found on most of today's continents.

Significant basins and formations were created z. B.

In the McArthur Basin / Northern Australia was formed to 0.65 bya originally km to about 40 large Strangways - impact craters .

Climate:

The oxygen (O 2 ) content in the earth's atmosphere had increased further.

Several Ice Ages occurred with z. T. complete global glaciations ( snowball earth ). They were the worst ice ages on earth. The glacier cover, which is up to 2 km thick , probably spread intermittently and at times extended to the equator . The dates are still imprecise. A distinction is made between the

  • Sturtic Ice Age , approx. 0.72 to 0.67 bya.
  • Varanger Ice Age approx. 0.67 bya (little known).
  • Marino Ice Age approx. 0.65 to 0.635 bya and thus marks the end of the cryogenium.

It is hypothesized that these ice ages are related to the breakup of the supercontinent Rodina. More rain could fall over the now smaller continental plates, which in connection with the physical and chemical weathering of the rocks caused. As a result, carbon dioxide (CO 2 ) was removed from the atmosphere , which led to a global temperature drop. The end of the glaciation is associated with increased volcanism and increased release of carbon dioxide.

Biology:

The photosynthesis came during the ice ages almost complete stop.

The first unicellular amoeba , such as the shell-bearing genus Arcellinida , have been found in fossil records.

The supposedly earliest known representative of the Bilateria (two-sided animals) lived with the genus Vernanimalcula . Finds come from the Doushantuo Formation / China .

from
≈720
mya
Tonium
Geology:

The geological processes were dominated by the fading orogenes , which began in the past Ectasian and led to the final formation of the supercontinent Rodinia around 0.90 bya. Extensive igneous events resulted from the converging continental plates. Rodinia probably comprised all land masses that existed on earth at that time. In its center was probably Laurentia . The supercontinent was surrounded by the global ocean Mirovia .

The disintegration of Rodinia began with the formation of rifts in different places and at different times. Various larger intrusions arose between 0.87 and 0.85 bya , which were detected in southern China and Africa as well as in Scandinavia and Scotland. From 0.83 bya, a superplume developed in northern polar latitudes , which lasted about 25 mya. Another superplume arose from 0.78 bya in equatorial latitudes. From 0.75 bya, this diapir also caused rift breaks in the western areas.

On today's NE edge of Africa, with the beginning of the Rodinia decay, an oceanic basin was created that expanded to the Mozambique Ocean. Herein emerged oceanic plateaus , mid-ocean ridges , Backarc- and forearc basins and passive continental margins and other Terrane . When this ocean began to close again, these crust blocks collided with the NE edge of Africa due to subduction and began to unfold from 0.85 bya on the East African ore. The northernmost and earliest section is the Arab-Nubian shield , which accreted between 0.89 and 0.58 bya. The East African orogeny is the earliest orogeny within the much more extensive Pan-African orogeny, in which cratons and other continental crustal parts were united to form the African continent .

The production of strip ores started again after the decrease of 1.8 bya. A connection with the Algonk Ice Age is suspected.

Climate:

From 0.85 bya a turning point occurred in the oxygen (O 2 ) enrichment in the earth's atmosphere . Initially, the values ​​increased slowly but steadily. The increasing oxygen content was the prerequisite for the development of higher forms of life.

From 0.75 bya, ozone (O 3 ) formed in higher layers of the atmosphere, which shielded UV rays from the earth's surface, which was crucial for the development of life on the continents. The oxygen content was high enough for bacteria to live on and in terrestrial sediment layers .

At 0.95 bya, the Algonk Ice Age , including the Griesjö glaciation, occurred in today's northern European latitudes.

The Kaigas Ice Age took place from 0.78 to 0.735 bya. It is considered to be the oldest of the great glaciations in the Neoproterozoic . Ice age deposits so far only come from Namibia , Brazil and China , so no global glaciation is assumed.

Biology:

The Acritarcha experienced their first great evolutionary adaptive radiation (species diversification). From around 1.0 to 0.7 bya, acritarcha (microfossils) with appendages appeared in various localities, which made planktonic life possible.

Probably from 0.9 bya first mushrooms in a shale rock in Canada . Even older mushroom fossils from China and Australia (approx. 1.5 bya) have not yet been confirmed.

At 0.8 bya and from 0.76 bya the first multicellular animals appeared in the Otavi group / Namibia , such as B. the microfossil sponge-like species Otavia antiqua . However, the interpretation is still debatable.

from
1,000
mya
Mesoproterozoic
Middle
Proterozoic
Meso
Proterozoic

Start:
1600

End:
1000
mya

Duration:
600 million 		Stenium
Geology:

The developing supercontinent Rodinia already consisted of most of the continents, cratons and blocks.

Basins and formations are for example

Climate:

Furthermore, the content of free oxygen (O 2 ) in the earth's atmosphere was still low at around 3%.

Biology:

In the deposits near Chorhat / India approx. 1.1 bya old traces of multicellular animal organisms that could actively move were discovered for the first time. They are interpreted as worm - like bottom - living benthos that could change their biotopes .

from
1,200
mya
Ectasium
Geology:

This period is geologically shaped by the disintegration and new formation of supercontinents with corresponding mountain formations (orogenes) and basin formations .

The supercontinent Columbia had largely broken apart by 1.3 bya, with the formation of final igneous swarms of dykes in North America , Australia and Fennoscandinavia , e.g. B. the Mackenzie Large Igneous Province with the Mackenzie dike swarm in the west of the Canadian shield , the Sudbury dike swarm in NE Ontario / Canada and the Satakunta dyke swarms in the Gulf of Bothnia and Finland .

The supercontinent Rodinia began to form from 1.3 bya from the broken land masses of Columbia through converging plate tectonic and mountain-forming processes. These processes led to large-scale orogenes like that

Components of Rodinia were the cratons or continents of East Antarctica, Laurentia, Baltica, Sibiria, Australia, South America, Africa, India and parts of China. Although the existence of Rodinia is undisputed, there are different concepts about the configuration of the landmasses involved.

The Grand Canyon Supergroup in Arizona / USA is one of the most important basins and formations . The sedimentation of this supergroup began at 1.25 bya in a rift valley that was formed during Terran secession from Laurentia . The supergroup consists of several groups and formations with a thickness of 4 km and is open in the Grand Canyon . The sedimentation takes place in a warm shelf sea and did not finish until around 250 mya. Intrusions of granite punched through local deposits.

Climate:

The atmospheric conditions had hardly changed compared to previous periods. The content of free oxygen (O 2 ) in the earth's atmosphere was still low at around 3%.

Biology:

In the hunting formation of Somerset Island / Northern Canada, 1,2 bya old plants with Bangiophyton-like shapes, which are characteristic of the more complex red algae , were found fossilized . They are described as the species Bangiomorpha pubescens from the genus Bangiomorpha. It is considered to be the possible first known complex multicellular cell with sexual reproduction .

from
1,400
mya
Calymmium
Geology:

Significant events were of the plate-teconical type and the formation of basins and formations .

On the supercontinent Columbia , whose cratons and continental blocks had united by 1.8 bya, further active island arcs - terranos accreted . However, the fragmentation of the land mass along continental rift breaks combined with globally widespread magmatic events began.

At 1.55 bya the Grawler-Kraton / South-Central Australia had formed from several magmatic active belts. It is part of the Australian shield, which also includes the Pilbara Kraton and Yilgarn Kraton. The Grawler Kraton is rich in natural resources such as gold (Au), copper (Cu), nickel (Ni), uranium (U) and diamonds .

Significant pools and formations include

Climate:

The content of free oxygen (O 2 ) in the earth's atmosphere was still low at around 3%.

Biology:

At 1.5 bya first aerobic organisms with oxidative energy metabolism . Breathing and photosynthesis thus achieved a certain balance.

1.5 bya old chemo fossil steranes found in the Barney Creek Formation / N Australia ; Steranes are typical components of eukaryotes and thus a biochemical or geochemical proof as an alternative / in addition to the morphological indicators. Bacteria and cyanobacteria were also fossilized .

from
1,600
mya
Paleoproterozoic
Early
Proterozoic
paleo-
Proterozoic

Start:
2500

End:
1600
mya

Duration:
900 million 		Statherium
Geology:

Geodynamic processes led to the further formation of mountains , basins , geological formations and accretions .

The accretion of cratons and continental blocks to the supercontinent Columbia came to an end at 1.8 bya. It then consisted of the Atlantica land masses, the continents Laurentia , Baltica , Siberia and East Antarctica as well as the Cratonic blocks of India and West Australia . At the edges of Columbia, however, further subduction and accretion processes took place up to 1.3 bya , the terranes of which can be detected worldwide. From 1.73 bya, the Mawson craton , also Mawson continent, formed during the Kimban orogeny , which includes today's Gawler craton (see also Grawler Ranges ) in South Australia and part of the East Antarctic craton.

Significant pools and formations were for example

The production of strip ores decreased significantly or came to a standstill. The reason could have been the ocean water with oxygen better mixing caused by the asteroid - impact in the Sudbury Basin / Ontario / Canada was caused.

Climate:

The earth's atmosphere was further characterized by the so-called third atmosphere . The free oxygen (O 2 ) content was still low at around 3%.

Biology:

In a formation in China there are 1.8 bya old unicellular acritarcha with an acid-resistant wall. These are interpreted as eukaryotic algae or spores from their persistence forms.

The 1.8 bya old Vindhya supergroup / Central India is characterized by a high fossil content of stromatolites , spores , acritars, algae, primitive arm pods (Brachiopoda), vascular plants and trace fossils (Ichnofossils). The algae filaments , which are among the oldest multicellular eukaryotes, are particularly noteworthy .

With the macroscopic , several millimeters large Chuaria and Tawuia, there lived organisms that had elongated or disk-shaped shapes. The 1.7 bya old fossils come from u. a. from the Tuanshanzi formation / China. According to the latest biogeochemical analyzes, it may have been multicellular eukaryotic algae.

from
1,800
mya
Orosirium
Geology:

The exogenous and endogenous processes of the lithosphere continued.

From 2.0 bya the continent Atlantica existed through the union of the West Africa craton with the Congo craton in Africa as well as the Guyana craton, Amazonas craton, Sao Francisco craton and Río de la Plata craton in South America. From 1.8 bya these land masses became part of the supercontinent Columbia .

Mountain building events were for example from 2 bya

  • the Capricorn Orogen between the Pilbara and Yilgarn cratons, creating the Western Australian craton.
  • the Proterozoic Central Indian Tectonic Zone (CITZ), through which the Aravalli Mountains (English Aravalli Range) in northwest India emerged from the collision of the Bundelkhand Kraton with the Marwar Kraton.
  • the Fennoscandinavian orogeny (English Svencofennian orogeny) on the northern European peninsula , which is viewed as a sequence of subduction events and accretion of island arcs . A large part of the continental crust in today's Sweden and Finland as well as smaller parts in north-west Russia formed from it .
  • the Wopmay orogeny , which resulted from the collision between the Hottah Terran, north of the Hottah Lake, an island arc and the archaic slave craton.
  • the Trans-Hudson orogeny was formed by the collision of the Hearne-Rae, Superior and Wyoming cratons and was the main mountain building event that formed the Canadian shield , the North American craton (also called Laurentia ) and thus the North American continent.
  • the Penokean orogeny (English Penokean orogeny) extends to Lake Superior / North America . The core of this orogeny is the Churchill craton, which arose as a result of several collisions of island arcs and terrances with the North American craton. Orogeny led to the formation of the continents Nena and Arctica , which later merged with other continents to form the supercontinent Columbia.

Significant pools and formations are

  • the Vredefort crater in South Africa , which was formed around 2.0 bya by the largest identified impact crater of an asteroid on earth with an initial diameter of approx. 300 km. This impact , which fell in the Witwatersrand Basin, had serious effects on the structure of the basin and the Transvaal supergroup deposited in it . In the center of the crater the semicircular Witwatersrand ridges were raised.
  • the animation group (from 1.9 bya) in the animation pool with the Biwabik Iron Formation and the Gunflint Iron Formation. These formations are particularly characterized by the high content of strip ores .
  • the Sudbury Basin in Ontario / Canada , which was created around 1.85 bya by the second largest known asteroid impact with an original diameter of 250 km. In addition to volcanic sedimentary deposits, it contains rich ore deposits . The impact penetrated the gunflint formation.
Climate:

The earth's atmosphere was further characterized by the so-called third atmosphere . The free oxygen (O 2 ) content was still low at around 3%.

Biology:

In the accompanying rocks (iw Cherts ) of the Gunflint Formation / Canada there are 2.0 to 1.9 bya old microfossil group Acritarcha with high morphological breadth and diversity, ranging from simple spheroidal forms to those with complex sculptured and with appendages provided bowls is enough. The cell size is typically in the range from 10 to 50 µm; they are therefore significantly larger than bacteria . These organisms often serve as key fossils in biostratigraphy and could be interpreted as eukaryotes or the transition from prokaryotes to eukaryotes.

from
2,050
mya
Rhyacium
Geology:

The geological development continued with the formation of further cratons , igneous events, mountain-forming processes and the formation of basins .

At 2.1 bya the Río de la Plata craton in Argentina and Uruguay and the West Africa craton / NW Africa emerged .

The supercontinent Columbia began to form from 2.1 bya, with the following mountain-forming events occurring

At the edge of the Transvaal Basin, the Bushveld complex / South Africa intruded at 2.06 bya . It is one of the world's largest complexes of basic melts on earth and is characterized by its magmatic deposits (Layered Intrusions), which contain extremely rich ore deposits of the platinum metal group (PMG).

Significant sedimentary basins and geological formations formed from 2.2 bya, for example in

From 2.2 bya the first red sediments and anhydrites appeared on the continents. They are regarded as an indication of terrestrial deposits under oxidizing conditions, which could only take place when oxygen was enriched in the atmosphere.

Climate:

From 2.3 bya, the concentrations of iron (II) ( Fe2 + ) and hydrogen sulfide (H 2 S) or its sulfides and thus also their oxidation fell . Oxygen (O 2 ) could accumulate in the oceans , but hardly escape into the earth's atmosphere . This development led to the third atmosphere with the big oxygen catastrophe (Engl. Great Oxygenation Event). In the first stage of this process, which lasted until 0.9 bya, the oxygen concentration in the atmosphere rose to around 3%.

The earth was approaching another ice age , the Paleoproterozoic glaciation, also known as the Huronian ice age . It began at 2.3 bya and lasted about 300 million years with several phases. The earth was probably almost completely frozen over ( snowball earth ). Evidence can be found in southern Canada , Wyoming , Finland , South Africa and India . Oxygen production in the oceans increased again during the end of the Huronic Ice Age.

Biology:

The Transvaal Supergroup / South Africa contains 2.3 to 2.2 bya old stromatolites and filamentous cyanobacteria with heterocysts for the first time . These serve as protection of oxygen-sensitive enzymes against oxygen and thus as evidence of the first free oxygen in the environment.

At 2.1 bya, the filamentous, spiral Grypania from the Marquette Formation / Michigan USA and the disc-shaped, three-dimensional Gabonionta from Gabon / West Africa, the currently oldest known macroscopic multicellular organisms may have existed. The interpretations and dates are not undisputed.

from
2,300
mya
Siderium
Geology:

The supercontinent Kenorland began to break apart from 2.5 bya. From the fragments later the large continent Arctica with the Canadian shield , Wyoming-Kraton and Siberia-Kraton was formed .

Further cratons, geological provinces, formations and igneous plutonites and volcanic rocks formed in the siderium .

The newly formed cratons and shields include the North China Kraton (around 2.5 bya) and the northern Borborema Province / Brazil (from 2.35 bya).

Significant sedimentary basins and geological formations are

Several larger batholiths and dykes intruded between 2.5 and 2.4 bya , such as the Closepet granite in the Dharwar Kraton / India , the Mistassini gang swarm and the Matachewan gang swarm in the Superior Kraton / North America . The Widgiemooltha Dyke Suite intruded into the Yilgin craton, and the Sebangwa Poort dykes invaded the Zimbabwe craton at about the same time. Paleogeographic reconstructions suggest a neighborhood of these cratons. This transition swarms produced Magmatic United Provinces (Engl. Large igneous province (LIP)) and possibly represented the oldest known Superplume represents breakouts.

An asteroid impact formed the Suavjärvi crater in the Russian Republic of Karelia before 2.4 bya . It originally had a diameter of around 16 km and is the oldest known impact crater on earth.

The formation of band ores (BIF) reached its peak.

Climate:

In the oceans, divalent iron ( Fe 2+ ) was converted into trivalent ( Fe 3+ ) iron and hydrogen sulfide (H 2 S) or its sulfides into sulfates , and free oxygen (O 2 ) could hardly accumulate in the earth's atmosphere . However, the second earth atmosphere , which had existed since 3.4 bya, gradually changed into the third earth atmosphere .

Biology:

Unicellular life continued to develop during the Paleoproterozoic . The first complex single cells with organelles (structures with special functions) and later also with a cell nucleus , which are then referred to as eukaryotes , developed from simple bacteria .

from
2,500
mya

The Archean Aeon

Also referred to as the eon of "ancient earth" .

  • Duration 1,500,000,000 years
  • Time span 2,500 to 4,000 mya

The Archean is divided into four eras:

Paleo- / geological overview

During the Archean, the earth continued to cool. Continental lithospheric plates , cratons and continents formed . Due to plate tectonic events, the first high mountains , rift fractures , thrusts and geological formations , in which important deposits can be found, emerged on the now stronger and more stable continental plates . Mighty plutons also intruded into the earth's plates. The Great Meteor Shower ( Great Bombardment ) that began in the Hadean , ended in the Eoarchean . During the entire aeon, thick layers of ribbon ore were deposited in the oceans .

After the loss of the original atmosphere , a new atmosphere was formed , which began with the first atmosphere and passed into the second atmosphere . In the oceans, microorganisms produced oxygen , which oxidized dissolved iron and hydrogen sulfide or its sulfides . As a result, hardly any oxygen could get into the atmosphere. In the Paleoarchean , 40,000 years of continuous rain fell , and the oceans were formed. In neoarchean a clearly ascertainable was cold period instead.

The evolution of life ranges from the chemical evolution in the Eoarchean through the development of prokaryotic cells to the division into the two phylogenetic domains bacteria and archaea at the beginning of the Paleoarchean . In the Paleoarchean, there is also the evolution of photosynthesis , first without releasing oxygen , then through the stromatolites forming cyanobacteria with the production of oxygen.

The predominant rock types in the Archean are mainly continental greenstone belts in granulite areas and submarine strip ores. For the mountain-building phases see also mountain-building phases at a glance .

Table of the Archean

A consistent subdivision is not yet available for the eras.

Era / age Events Beginning
Neoarchean
New
Archaic
Neo-
Archean

Start:
2800

End:
2500
mya

Duration:
300 million
Geology:

The geological conditions changed fundamentally in the Neoarchic . The cooling of the earth had an impact on the rheological (deformation and flow behavior) and other properties of the continental lithospheric plates . They became stronger and more sustainable. Plate tectonic and other geodynamic processes had near-surface effects, such as B. the formation of high mountains , rift fractures and thrusts . Several large intracontinental sedimentary basins and formations with group and supergroup formations, further greenstone belts and magmatic complexes of various types were also created. Important deposits formed in them .

From 2.7 bya the oldest recognized supercontinent Kenorland formed . It comprised the continental formations Canadian Shield , Wyoming Kraton , Siberia Kraton , Baltic Shield or Fennos Scandinavia , East Antartica Kraton and West Australian Shield (Yilgarn Kraton and Pilbara Kraton) and the Kalahari Kraton, which is made up of the Kaapvaal Kraton , the Zimbabwe craton as well as the Limpopo belt and the Namaqua belt.

At 2.5 bya the continent of Vaalbara disintegrated , while the Zimbabwe craton and the Yilgarn craton accreted to the hypothetical continent Ur .

The Algoman orogeny, also known as Kenoran orogeny, occurred between 2.7 and 2.5 bya, during which the Minnesota River Valley Terran collided with the Superior Kraton / Canadian Shield . Magmatic intrusions , green formations and rock metamorphoses were associated with orogeny . It is the earliest datable orogeny in North America .

From 2.7 bya, the submarine Blake River Megacaldera complex formed. It consists of a series of overlapping calderas that extend along the southern zone of the Abitibi greenstone belt of the Superior Kraton / Canada . Due to its size and volume, it is classified as a supervolcano . It contains very rich ore deposits .

At 2.7 bya the Stillwater Complex / USA intruded in the Wyoming Craton in the form of a storage corridor or sills (English layered intrusion or sill). The metamorphosis of the plutonic rocks took place around 2.5 bya. This complex is important because of its large ore deposits of chromium (Cr) , copper (Cu) and nickel (Ni) as well as palladium (Pd) and platinum .

Several larger batholiths and dykes intruded between 2.5 and 2.4 bya , such as the Closepet granite in the Dharwar Kraton / India , the Mistassini gang swarm and the Matachewan gang swarm in the Superior Kraton / North America . This transition swarms produced Magmatic United Provinces (Engl. Large igneous province (LIP)) and possibly represented the oldest known Superplume represents breakouts.

Large sedimentary basins, formations and deposits formed on almost all of the land masses that existed at the time, which today belong to Western Australia , India , North America , South Africa and Brazil . The deposits contain ores with iron from the strip ores, gold , chromium, nickel, copper, platinum and palladium as well as other metallic raw materials .

In Africa , from 2.5 bya on the Kaapvaal craton, the Transvaal Supergroup was formed in northern South Africa and southern Botswana . It sedimented in three basins , which are delimited by the Witwatersrand Basin (2.7 bya) and the Bushveld Complex (2.06 bya). Were deposited clastic sedimentary rocks followed by carbonates and bands ores .

Climate:

The atmosphere was composed of nitrogen (N) with small amounts of water vapor , carbon dioxide (CO 2 ) and other gases. It thus continued to correspond to the second atmosphere .

Cyanobacteria continued to produce oxygen , which, however, hardly got into the earth's atmosphere .

At 2.7 bya 15 diamictite horizons were created , which document an icing in the more than 500 meters thick Talya Conglomerate of the Vanivilas Formation in the Dharwar Craton / India and directly below the base of the Stillwater Complex in Montana .

Biology:

In the Fortescue Group / Australia there are 2.8 bya old stromatolites with filamentous cyanobacteria, but from a non-marine freshwater environment, which indicates settlement on the mainland .

from
2,800
mya
Mesoarchean
Middle
Archean
meso
Archean

Start:
3200

End:
2800
mya

Duration:
400 million
Geology:

On the basis of geological investigations at the Pilbara Craton / Western Australia , Barberton Greenstone Belt / South Africa and Superior Kraton / North America , it was found that from around 3.2 bya continental crust , plate tectonics , subduction and Wilson cycle began to develop similar to today's tectonic principle .

From 3 mya the first hypothetical supercontinent Ur iw had formed from the cratons Western Dharwar and the Singhbhum kratons / India , Kaapvaal kratons / South Africa and Pilbara kratons / Western Australia . The existence of Ur is in dispute.

Band ores (BIF) continued to be produced and deposited.

Due to the lack of oxygen in the atmosphere, no oxidation of the mainland rocks took place.

Climate:

The composition of the atmosphere continued to correspond to the second atmosphere with the main components nitrogen (N) with small amounts of water vapor , carbon dioxide (CO 2 ) and other gases.

Cyanobacteria continued to produce oxygen , which was consumed in the oxidation of divalent ( Fe 2+ ) to trivalent iron ( Fe 3+ ) as well as hydrogen sulfide and sulfidic heavy metal minerals. As a result, only a very small amount of free oxygen got into the earth's atmosphere .

Biology:

In the Cherts of the Fig Tree Formation / SW Africa , 3.1 bya spherical cyanobacteria and chemofossils such as phytane and pristan appear for the first time . These are breakdown products of photosynthesis . The filamentous and spherical cyanobacteria correspond to recent forms. The oxygenic photosynthesis is therefore considered to be assured at this point in time.

from
3,200
mya
Paleoarchean
Early
Archean
paleo-
Archean

Start:
3600

End:
3200
mya

Duration:
400 million
Geology:

Between 3.6 and 3.5 bya formation of further cratons , such as the Kaapvaal craton , the Congo craton and the Zimbabwe craton in Africa , the Pilbara craton in Western Australia , the Dharwar craton in India and the superior kraton and the Wyoming craton in North America and the Guyana craton in South America .

From rock formations and crust fractures in the Barberton-Greestone Belt in the Kaapvaal-Kraton / South Africa it was concluded that the impact of an approximately 58 to 37 kilometers large asteroid probably occurred at 3.26 bya . It was the largest ever found or reconstructed.

The long-lasting, heavy rainfall led to severe weathering of the surface rocks; they dissolved silicates a . a. with bivalent iron ( Fe 2+ ) and calcium (Ca).

The predominant rocks basalt and komatiite show a very high temperature of the initial melts (with 1,600 0 C; about 400 0 C higher than today's melts). Komatite are typical rocks of this and contain deposits of sulphidic n minerals , rich in nickel , copper and gold .

Climate:

The earth continued to cool, and the First Atmosphere evolved into the Second Atmosphere . There was continuous rain for 40,000 years; the oceans formed. The waters were hot and, due to the high content of dissolved carbon dioxide (H 2 CO 3 ) and sulphurous acid (H 2 SO 3 ), very aggressive and had a very low pH value .

The high levels of ultraviolet radiation photochemically decomposed the water, methane (CH 4 ) and ammonia (NH 3 ) molecules , causing carbon dioxide (CO 2 ) and nitrogen (N 2 ) to accumulate in the atmosphere. The increased metabolic processes of fermenting , chemolithotrophic bacteria and archaea led to the accumulation of nitrogen (N) and methane (CH 4 ). The light gases, such as hydrogen (H) or helium (He), evaporated into space .

At 3.4 bya the atmosphere probably consisted only of nitrogen with small amounts of water vapor, carbon dioxide and other gases. The dissolution of large amounts of carbon dioxide in the oceans reduced the greenhouse effect , and temperatures fell over the following periods.

Biology:

At 3.6 bya there was already clearly proven life , as in the rocks of the 3.6 bya old Barberton Greenstone Belt / South Africa . Traces of prokaryotes were found, which are probably the oldest traces of living things worldwide. Also there were stromatolites discovered.

Around 3.5 bya, fossilized filamentous microorganisms were suspected in the apex chert of the Warrawoona group of the Pilbara Kraton / NW Australia . Cyanobacteria and filamentous bacteria produced biogenic carbonate precipitation by means of oxygenated photosynthesis . The morphology corresponds to recent forms. The proof is considered to be relatively secure.

from
3,600
mya
Eoarchean
dawn of
Archean
Eo-
Archean

Start:
4000

End:
3600
mya

Duration:
400 million
Geology:

At about 3.8 bya the great meteor shower fades away ( great bombardment ).

Formation of the first cratons . The oldest are the Yilgrin craton in Western Australia (3.8 bya) and the Sarmatian craton (3.7 bya) as part of the later continent of Baltica .

Presumably as a result of the partial melting and hydration of basaltic oceanic crusts , tonalite-trondhjemite-granodiorite complexes (TTG complexes) formed, which probably represent the first and oldest continental crust .

The 3.8 bya old rock formations of the Isua green stone belt / SW Greenland were deposited in the supracrustal valley , ie on the surface of the earth. They were formed from individual crustal plates that were possibly tectonically stacked in an island-arc regime. In the greenstone belts are banded iron formation (Engl. Banded iron formation (BIF)), which presumably around hydrothermal originated sources.

The band ores deposited from 3.8 bya could have been created with the help of microorganisms that either operate oxygen- producing oxygenic photosynthesis or anoxygenic photosynthesis , in which no oxygen is released. The latter appears to have been predominant.

The oldest rocks include the Napier Complex in Enderbyland / East Antarctica (3.95 bya), the Itsaq Gneiss Complex in Akulleq terrance / SW Greenland (3.9 bya) and the Saglek-Hebron Block / east coast of the Labrador Peninsula (3.86 bya).

Climate:

During the Great Bombardment , which began from 4.1 bya, a new atmosphere , the First Atmosphere , had formed after the loss of the primordial atmosphere . It developed from the gases that escaped from (partially) melted materials and consisted mainly of water vapor (H 2 O), carbon dioxide (CO 2 ) and hydrogen sulfide (H 2 S) as well as small amounts of nitrogen (N 2 ), hydrogen ( H 2 ), carbon monoxide (CO), sulfur dioxide (SO 2 ), methane (CH 4 ) and ammonia (NH 3 ). Free oxygen (O 2 ) and nitrogen (N 2 ) were hardly present.

Hypothetically, phototrophic microorganisms from 3.8 bya , probably ancestors of today's cyanobacteria , could have operated a form of photosynthesis . From this time on, the divalent iron ( Fe 2+ ) was oxidized to trivalent iron ( Fe 3+ ) and precipitated in the form of hydroxides and oxides (see also ribbon ore ).

Biology:

The chemical evolution with more complex processes had intensified. After the formation of short abiotic building block molecules from inorganic compounds in the Hadaikum, cell precursors (pre-cells) developed, such as B. microspheres or organic coacervates, without the ability to self-replicate . This was followed by the formation of macromolecules through abiotic polymerisation with subsequent assembly into larger organelle and cell- like structures. Ultimately, protobionts emerged that already contained self-replication and a genetic code (see also RNA world hypothesis ).

In the Nuvvuagittuq greenstone belt / North America , microfilaments and tube-like structures were discovered that were interpreted as remains of microbes or microorganisms . They should be 3.77 bya old, possibly even older. In the Isua sediments / SW Greenland , 3.7 bya old macrospopic , stratified stromatolites were discovered that formed in shallow waters. However, both interpretations are still controversial.

from
4,000
mya

The Aeon Hadean

The Aeon Hadean or "Aeon of the Earth's Formation" originally referred to the period that predated the oldest known rocks. Etymologically, the name refers to the Greek god Hades , who ruled the underworld of Greek mythology full of heat and disorder. The age was described by the geologist Preston Cloud (1972) as the period from which the oldest known stones come. Synonymous with the "Priscoan period" according to W. Brian Harland .

There is currently no binding subdivision of the Hadaikum.

  • Duration around 600,000,000 years
  • Time span ≈ 4,600 to 4,000 mya

Information about the age of the earth does not come from the rocks of the earth itself, but from special meteorites , the chondrites , of which it is assumed that they formed in the same period as the earth and have not changed since then - in contrast to the earth to have. The age is determined using isotope geochemistry . It was used to determine an age of around 4.568 billion years.

Paleo- / geological overview

One of the oldest known rocks is the Acasta gneiss from the Slave Craton / Northwest Canada with an age of around 4.03 bya. Rocks in the Nuvvuagittuq greenstone belt in northern Québec , Canada are similarly old. Their dating is still controversial and ranges from approx. 4.3 to approx. 3.8 bya.

The primordial atmosphere of the earth probably consisted of gaseous parts of the protoplanetary disk , such as hydrogen (H2) and helium (He) as well as small parts of methane (CH 4 ), ammonia (NH 3 ) and some noble gases . It was followed by the development of the First Atmosphere .

The first earthly hydrosphere was formed with liquid water. This is believed to have accumulated in a primordial ocean .

Presumably the chemo-evolutionary evolution , also called abiogenesis, developed, with which inorganic organic substances were created.

For the mountain-building phases see also mountain-building phases at a glance .

Table of the Hadaikum

Era / age Events Beginning
inconsistent
divided

start:
approx
≈4.600

End:
4000
mya
Duration:
n.def.
Geology:

About 4.57 bya ago the formation of the earth began by accretion of planetesimals into a protoplanet .

From 4.45 bya the moon came into being , caused by an oblique, slow collision (Giant Impact) of an approximately Mars-sized body ( Theia ) with the proto-earth. The ejected mantle materials of the protoplanets involved accreted to the moon.

From around 4.4 to 4.2 bya, the oldest minerals were formed , which come as detritic (transported deposits) zircons from the Jack Hills of the Yilgarn Kraton / Western Australia . From this it is concluded that a continental-like crust and liquid water were already present during this period . The differentiation into a heavy core area and a lighter shell area was also largely complete.

From the low- silicon dioxide (SiO 2 ) -free ultramafic , very low-viscosity magmas of the Earth's mantle, the first lithospheric plates formed around 4.1 bya at a low geothermal gradient , which already interacted with each other.

Between 4.1 and 3.8 bya, u. a. the earth and the moon the Great bombardment (Engl. Late Heavy Bombardment) by many large asteroids and other bodies rest of planet formation .

Probably the oldest rock is the Acasta gneiss from the Slave Craton / Northwest Canada. The protoliths (original rocks) date to around 4.03 bya, the metamorphosis to gneiss took place up to around 3.58 bya.

Climate:

The primordial atmosphere probably consisted of gaseous parts of the protoplanetary disk , such as hydrogen (H 2 ) and helium (He) as well as small parts of methane (CH 4 ) and ammonia (NH 3 ) as well as some noble gases . It probably also contained various types of dusty and larger solid particles.

With the start of the Great Bombardment, the First Atmosphere began to form. Water vapor (H 2 O), carbon dioxide (CO 2 ) and hydrogen sulfide (H 2 S) with small proportions of nitrogen (N 2 ), hydrogen (H 2 ), carbon monoxide (CO) and other gaseous substances are released from the partially melted earth material .

Although the radiation of the sun by 25 to 30% was much lower than today, which were atmospheric temperatures well above the freezing point ; one speaks of the paradox of the weak young sun .

The first earthly hydrosphere was formed with liquid water . This is believed to have accumulated in a primordial ocean .

Biology:

No biological processes have been detected or expected before 4.4 bya . But chemo-evolutionary processes, also known as abiogenesis, presumably took place, after which inorganic organic substances developed. At the end of this development, hypothetical precursors of unicellular life emerged, the protobionts .

from
≈4,600
mya

Origin of the earth

An estimated 4.7 billion years ago, the earth formed from a protoplanetary disk . At that time the earth had little resemblance to our planet today and was exposed to constant cosmic bombardment.

Notes on the large table

  1. The information about the ages shown was taken from the International Chronostratigraphic Chart, status v2017 / 02 as well as the assigned Global Boundary Stratotype Section and Point (GSSP) from the GSSP Table - All Periods of the International Commission on Stratigraphy (ICS) (see also WP- Article International Commission on Stratigraphy and Global Boundary Stratotype Section and Point ) paleontologists often prefer to refer to zones, or more precisely: biozones , than to geological periods.
    The nomenclature of these biozones is quite complex, for more information on the individual biozones see the articles of the respective geological ages.
  2. The terms Tertiary and Quaternary were abolished in 2004 and replaced by Palaeogene and Neogene respectively. Since 2005, however, the ICS has given the Quaternary a new status as the sub-era of the Cenozoic.
  3. The division of the Carboniferous into Mississippian and Pennsylvanian is common only in North America. In Europe, carbon is divided into upper and lower .
  4. Research and more accurate dating capabilities over the past 30 years have shed new light on geological and paleontological events in the Precambrian. The stratigraphic nomenclature is still in the making, since 2004 the Ediacarium has officially preceded the Cambrian as a period. Outdated names for the Neoproterozoic or Ediacarian are: Vendium , Varangium , Protocambrian , Eocambrian or Precambrian , which were also used to denote the period immediately before the Cambrian.

The following abbreviations are used here:

  • bya for English billion years ago or for German "billion (n) years ago" or "x billion (s) years ago"
  • mya for English million years ago or for German "million (s) years ago" or "x million (s) years ago"
  • tya for English thousand years ago, or for German "thousand years ago" or "x thousand years ago"
  • tsd for German "thousand"

Web links

  • stratigraphy.org - The International Commission on Stratigraphy (ICS)
  • geosociety.org - The Geological Society of America's international guidance scale
  • scotese.com - Earth maps of all geological ages since the late Precambrian