| Mesoarchean | |
| Color: | Mesoarchean |
| Top Bar: | all time |
| Time Start: | 3200 |
| Time End: | 2800 |
| Timeline: | Mesoarchean |
| Proposed Boundaries1: | 3490–2780 Ma |
| Proposed Boundaries1 Ref: | Gradstein et al., 2012 |
| Proposed Subdivision1: | Vaalbaran Period, 3490–3020 Ma |
| Proposed Subdivision1 Coined: | Gradstein et al., 2012 |
| Proposed Subdivision2: | Pongolan Period, 3020–2780 Ma |
| Proposed Subdivision2 Coined: | Gradstein et al., 2012 |
| Name Formality: | Formal |
| Alternate Spellings: | Mesoarchaean |
| Celestial Body: | earth |
| Usage: | Global (ICS) |
| Timescales Used: | ICS Time Scale |
| Chrono Unit: | Era |
| Strat Unit: | Erathem |
| Timespan Formality: | Formal |
| Lower Boundary Def: | Defined Chronometrically |
| Lower Gssa Accept Date: | 1991 |
| Upper Boundary Def: | Defined Chronometrically |
| Upper Gssa Accept Date: | 1991 |
| Caption Map: | A reconstruction of the Earth's continents during the middle Mesoarchean, c. 3 Ga. |
| Caption Art: | Banded iron formation created during the Mesoarchean era |
| Caption Outcrop: | Artist impression of the Archean eon |
The Mesoarchean (also spelled Mesoarchaean) is a geologic era in the Archean Eon, spanning, which contains the first evidence of modern-style plate subduction and expansion of microbial life. The era is defined chronometrically and is not referenced to a specific level in a rock section on Earth.
The Mesoarchean era is thought to be the birthplace of modern-style plate subduction, based on geologic evidence from the Pilbara Craton in western Australia.[1] [2] A convergent margin with a modern-style oceanic arc existed at the boundary between West and East Pilbara approximately 3.12 Ga. By 2.97 Ga, the West Pilbara Terrane converged with and accreted onto the East Pilbara Terrane.[2] A supercontinent, Vaalbara, may have existed in the Mesoarchean.[3]
Analysis of oxygen isotopes in Mesoarchean cherts has been helpful in reconstructing Mesoarchean surface temperatures.[4] These cherts led researchers to draw an estimate of an oceanic temperature around 55-85°C[5] while other studies of weathering rates postulate average temperatures below 50°C.
The Mesoarchean atmosphere contained high levels of atmospheric methane and carbon dioxide, which could be an explanation for the high temperatures during this era.[4] Atmospheric dinitrogen content in the Mesoarchean is thought to have been similar to today, suggesting that nitrogen did not play an integral role in the thermal budget of ancient Earth.[6]
The Pongola glaciation occurred around 2.9 Ga, from which there is evidence of ice extending to a palaeolatitude (latitude based on the magnetic field recorded in the rock) of 48 degrees. This glaciation was likely not triggered by the evolution of photosynthetic cyanobacteria, which likely occurred in the interval between the Huronian glaciations and the Makganyene glaciation.[7]
Microbial life with diverse metabolisms expanded during the Mesoarchean era and produced gases that influenced early Earth's atmospheric composition. Cyanobacteria produced oxygen gas, but oxygen did not begin to accumulate in the atmosphere until later in the Archean.[8] Small oases of relatively oxygenated water did exist in some nearshore shallow marine environments by this era, however.[9]