Earliest known life forms

The earliest known life forms on Earth may be as old as 4.1 billion years according to biologically fractionated graphite inside a single zircon grain in the Jack Hills range of Australia. The earliest evidence of life found in a stratigraphic unit, not just a single mineral grain, is the 3.7 Ga metasedimentary rocks containing graphite from the Isua Supracrustal Belt in Greenland. The earliest direct known life on Earth are stromatolite fossils which have been found in 3.480-billion-year-old geyserite uncovered in the Dresser Formation of the Pilbara Craton of Western Australia. Various microfossils of microorganisms have been found in 3.4 Ga rocks, including 3.465-billion-year-old Apex chert rocks from the same Australian craton region, and in 3.42 Ga hydrothermal vent precipitates from Barberton, South Africa. Much later in the geologic record, likely starting in 1.73 Ga, preserved molecular compounds of biologic origin are indicative of aerobic life. Therefore, the earliest time for the origin of life on Earth is at least 3.5 billion years ago and possibly as early as 4.1 billion years ago — not long after the oceans formed 4.5 billion years ago and after the formation of the Earth 4.54 billion years ago.

Biospheres

Earth is the only place in the universe known to harbor life, where it exists in myriad environments. The origin of life on Earth was at least 3.5 billion years ago, possibly as early as 3.8–4.1 billion years ago. Since its emergence, life has persisted in several geological environments. The Earth's biosphere extends down to at least below the seafloor, up to into the atmosphere, and includes soil, hydrothermal vents, and rock. Further, the biosphere has been found to extend at least below the ice of Antarctica and includes the deepest parts of the ocean. In July 2020, marine biologists reported that aerobic microorganisms in "quasi-suspended animation" were found in organically poor sediment below the seafloor in the South Pacific Gyre . Microbes have been found in the Atacama Desert in Chile, one of the driest places on Earth, and in deep-sea hydrothermal vent environments which can reach temperatures over 400 °C. Microbial communities can also survive in cold permafrost conditions down to -25 °C. Under certain test conditions, life forms have been observed to survive in the vacuum of outer space. More recently, studies conducted on the International Space Station found that bacteria could survive in outer space. In February 2023, findings of a "dark microbiome" of microbial dark matter of unfamiliar microorganisms in the Atacama Desert in Chile, a Mars-like region of planet Earth, were reported.

Geochemical evidence

The age of Earth is about 4.54 billion years; the earliest undisputed evidence of life on Earth dates from at least 3.5 billion years ago according to the stromatolite record. Some computer models suggest life began as early as 4.5 billion years ago. The oldest evidence of life is indirect in the form of isotopic fractionation processes. Microorganisms will preferentially use the lighter isotope of an atom to build biomass, as it takes less energy to break the bonds for metabolic processes. Biologic material will often have a composition that is enriched in lighter isotopes compared to the surrounding rock it's found in. Carbon isotopes, expressed scientifically in parts per thousand difference from a standard as δ¹³C, are frequently used to detect carbon fixation by organisms and assess if purported early life evidence has biological origins. Typically, life will preferentially metabolize the isotopically light ¹²C isotope instead of the heavier ¹³C isotope. Biologic material can record this fractionation of carbon.
File:Quartz-pebble metaconglomerate 1.jpg|thumb|Zircons in metaconglomerates from the Jack Hills in Australia show carbon isotopic evidence for early life.
The oldest disputed geochemical evidence of life is isotopically light graphite inside a single zircon grain from the Jack Hills in Western Australia. The graphite showed a δ¹³C signature consistent with biogenic carbon on Earth. Other early evidence of life is found in rocks both from the Akilia Sequence and the Isua Supracrustal Belt in Greenland. These 3.7 Ga metasedimentary rocks also contain graphite or graphite inclusions with carbon isotope signatures that suggest biological fractionation.
The primary issue with isotopic evidence of life is that abiotic processes can fractionate isotopes and produce similar signatures to biotic processes. Reassessment of the Akilia graphite show that metamorphism, Fischer-Tropsch mechanisms in hydrothermal environments, and volcanic processes may be responsible for enrichment lighter carbon isotopes. The ISB rocks that contain the graphite may have experienced a change in composition from hot fluids, i.e. metasomatism, thus the graphite may have been formed by abiotic chemical reactions. However, the ISB's graphite is generally more accepted as biologic in origin after further spectral analysis.
Metasedimentary rocks from the 3.5 Ga Dresser Formation, which experienced less metamorphism than the sequences in Greenland, contain better preserved geochemical evidence. Carbon isotopes as well as sulfur isotopes found in barite, which are fractionated by microbial metabolisms during sulfate reduction, are consistent with biological processes. However, the Dresser formation was deposited in an active volcanic and hydrothermal environment, and abiotic processes could still be responsible for these fractionations. Many of these findings are supplemented by direct evidence, typically by the presence of microfossils, however.

Fossil evidence

s are direct evidence of life. In the search for the earliest life, fossils are often supplemented by geochemical evidence. The fossil record does not extend as far back as the geochemical record due to metamorphic processes that erase fossils from geologic units.

Stromatolites

s are laminated sedimentary structures created by photosynthetic organisms as they establish a microbial mat on a sediment surface. An important distinction for biogenicity is their convex-up structures and wavy laminations, which are typical of microbial communities who build preferentially toward the sun. A disputed report of stromatolites is from the 3.7 Ga Isua metasediments that show convex-up, conical, and domical morphologies. Further mineralogical analysis disagrees with the initial findings of internal convex-up laminae, a critical criterion for stromatolite identification, suggesting that the structures may be deformation features caused by extensional tectonics in the Isua Supracrustal Belt.
The earliest direct evidence of life are stromatolites found in 3.48 billion-year-old chert in the Dresser formation of the Pilbara Craton in Western Australia. Several features in these fossils are difficult to explain with abiotic processes, for example, the thickening of laminae over flexure crests that is expected from more sunlight. Sulfur isotopes from barite veins in the stromatolites also favor a biologic origin. However, while most scientists accept their biogenicity, abiotic explanations for these fossils cannot be fully discarded due to their hydrothermal depositional environment and debated geochemical evidence.
Most archean stromatolites older than 3.0 Ga are found in Australia or South Africa. Stratiform stromatolites from the Pilbara Craton have been identified in the 3.47 Ga Mount Ada Basalt. Barberton, South Africa hosts stratiform stromatolites in the 3.46 Hooggenoeg, 3.42 Kromberg and 3.33 Ga Mendon Formations of the Onverwacht Group. The 3.43 Ga Strelley Pool Formation in Western Australia hosts stromatolites that demonstrate vertical and horizontal changes that may demonstrate microbial communities responding to transient environmental conditions. Thus, it is likely anoxygenic or oxygenic photosynthesis has been occurring since at least 3.43 Ga Strelley Pool Formation.

Microfossils

Claims of the earliest life using fossilized microorganisms are from hydrothermal vent precipitates from an ancient sea-bed in the Nuvvuagittuq Belt of Quebec, Canada. These may be as old as 4.28 billion years, which would make it the oldest evidence of life on Earth, suggesting "an almost instantaneous emergence of life" after ocean formation 4.41 billion years ago. These findings may be better explained by abiotic processes: for example, silica-rich waters, "chemical gardens," circulating hydrothermal fluids, and volcanic ejecta can produce morphologies similar to those presented in Nuvvuagittuq.
File:Halobacteria.jpg|thumb|168x168px|Archaea were first found in extreme environments, such as hydrothermal vents.
The 3.48 Ga Dresser formation hosts microfossils of prokaryotic filaments in silica veins, the earliest fossil evidence of life on Earth, but their origins may be volcanic. 3.465-billion-year-old Australian Apex chert rocks may once have contained microorganisms, although the validity of these findings has been contested. "Putative filamentous microfossils," possibly of methanogens and/or methanotrophs that lived about 3.42-billion-year-old in "a paleo-subseafloor hydrothermal vein system of the Barberton greenstone belt, have been identified in South Africa." A diverse set of microfossil morphologies have been found in the 3.43 Ga Strelley Pool Formation including spheroid, lenticular, and film-like microstructures. Their biogenicity are strengthened by their observed chemical preservation. The early lithification of these structures allowed important chemical tracers, such as the carbon-to-nitrogen ratio, to be retained at levels higher than is typical in older, metamorphosed rock units.

Molecular biomarkers

Biomarkers are compounds of biologic origin found in the geologic record that can be linked to past life. Although they aren't preserved until the late Archean, they are important indicators of early photosynthetic life. Lipids are particularly useful biomarkers because they can survive for long periods of geologic time and reconstruct past environments.
File:Common lipid types.svg|thumb|Lipids are commonly used in geologic studies to find evidence of oxygenic photosynthesis.
Fossilized lipids were reported from 2.7 Ga laminated shales from the Pilbara Craton and the 2.67 Ga Kaapvaal craton in South Africa. However, the age of these biomarkers and whether their deposition was synchronous with their host rocks were debated, and further work showed that the lipids were contaminants. The oldest "clearly indigenous" biomarkers are from the 1.64 Ga Barney Creek Formation in the McArthur Basin in Northern Australia, but hydrocarbons from the 1.73 Ga Wollogorang Formation in the same basin have also been detected.
Other indigenous biomarkers can be dated to the Mesoproterozoic era. The 1.4 Ga Hongshuizhuang Formation in the North China Craton contains hydrocarbons in shales that were likely sourced from prokaryotes. Biomarkers were found in siltstones from the 1.38 Ga Roper Group of the McArthur Basin. Hydrocarbons possibly derived from bacteria and algae were reported in 1.37 Ga Xiamaling Formation of the NCC. The 1.1 Ga Atar/El Mreïti Group in the Taoudeni Basin, Mauritania show indigenous biomarkers in black shales.