Role of low solar luminosity in the history of the biosphere

• Published in: Geochemistry international Vol. 55; no. 5; pp. 401 - 417
• Main Author: Galimov, E. M.
• Format: Journal Article
• Language: English
• Published: Moscow Pleiades Publishing 01-05-2017; Springer Nature B.V
• Subjects: Atmosphere; Atmospherics; Biosphere; Biota; Carbon dioxide; Carbonates; Climate; Climate change; Compensation; Earth; Earth and Environmental Science; Earth Sciences; Freezing; Freezing point; Gases; Geochemistry; Glaciation; Glaciers; Glaciology; Greenhouse effect; Greenhouse gases; Luminosity; Magma; Methane; Organic carbon; Solar energy; Solar radiation; Surface temperature; Uptake; Volcanism; greenhouse gases; glaciation; C; δ; CH; solar luminosity; biosphere evolution; climate; CO; carbonates; organic carbon
• ISSN: 0016-7029; 1556-1968
• DOI: 10.1134/S0016702917050068

It was shown that the history of the biosphere is closely related to processes caused by low solar luminosity. Solar radiation is insufficient to maintain the Earth’s surface temperature above the freezing point of water. Positive temperatures are kept owing to the presence of greenhouse gases in the atmosphere: CO
2
, CH
4
, and others. Certain stages in the development of the biosphere and climate are related to these effects. Methane was the main carbon-bearing gas in the primordial atmosphere. It compensated the low solar luminosity. Life originated under the reduced conditions of the early Earth. Methane-producing biota was formed. Methane remained to be the main greenhouse gas in the Archean. The release of molecular oxygen into the atmosphere 2.4 Ga ago resulted in the disruption of the established mechanism of the compensation of the low solar luminosity. Methane ceased to cause a significant greenhouse effect, and the content of carbon dioxide was insufficient to play this role. A global glaciation began and had lasted for approximately 200 million years. However, the increasing CO
2
content in the atmosphere reached eventually a level sufficient for the compensation for the low solar luminosity. The glaciation period came to an end. Simultaneously, a conflict arose between the role of CO
2
as a gas controlling the thermal regime of the planet and as an initial material for biota production. As long as the resource of biotic carbon was inferior to that of atmospheric CO
2
, the uptake of atmospheric CO
2
related to sporadic increases in biologic production was insufficient for a significant change in the thermal regime. This was the reason for a long-term climate stabilization for 1.5 billion years. By 0.8 Ga, the resource of oceanic biota reached the level at which variations in the uptake of atmospheric CO
2
related to variations in the production of organic and carbonate carbon became comparable with the resource of atmospheric CO
2
. Since then, an oscillatory equilibrium has been established between the intensity of biota development and climate-controlling CO
2
content in the atmosphere. Glaciation and warming periods have alternated. These changes were triggered by various geologic events: intensification or attenuation of volcanism; growth, breakup, or migration of continents; large-scale magmatism; etc. A new relation between atmospheric CO
2
and biotic carbon was established in response to the emergence of terrestrial biota and the appearance of massive buffers of organic carbon on land. The interrelation of the biosphere and climate changed.