Amarygmozoic

5100 - 5050 mya
Phtanum formed approximately 5.1 billion years

ago, and evolved alongside the other planets of

its System and Luzemir in a protoplanetary disk.

As the early system evolved, numerous

protoplanets collided with Phtanum, adding to its

mass. This streak continued until Phtanum had

devoured every rocky planet in the inner system,

with the exception of Dhara.

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Archegozoic

5050 - 4815 mya

The Archegozoic starts with the semi-solidification of Phtanum´s crust. The many collisions with other astronomical bodies made Phtanum rich in water, which was mostly present as vapor as temperatures would still be too hot for it to condense on the surface. The atmosphere, way thicker than now, consisted mostly of carbon dioxide. At this age, the planet was a venuslike mini neptune.

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Pyrrhozoic

4815 - 4530 mya

The Pyrrhozoic is defined​ by the collision of a large rogue planet with young Phtanum after its crust had already solidified. The powerful impact ejected most of the ancestral thick atmosphere, giving Phtanum the lighter air pressure it has today. This impact also gave Phtanum numerous smaller moons.

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Bisuzoic

4530 - 4100 mya

With the thick ancestral atmosphere gone, temperatures and pressures turned more bearable. Enormous volcanism, stirred up by the impact, still eject loads of carbon dioxide into the atmosphere. On a re-solidified surface, first anaerobic life develops in boiling mud pools.

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Eremozoic

4100 - 3400 mya

​As volcanism slowed down gradually, less particles got ejected into the atmosphere. The skies turn from a grim gray into a pale teal. Water vapor in the atmosphere condensates en masse, and enormous rainfall form the first oceans. Phtanum did not go through global freeze-overs like Earth did, but there were phases where the planet fluctuated in temperature. Microbial life expands in niches.

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Lygozoic

3400 - 2250 mya

A great death marked the beginning of the Lygozoic. The now clearer skies allowed for energy generation via photosynthesis - and certain microbes were not going to leave this potential niche unoccupied. The anaerobic life that so far dominared microbial mats died in a chaotic frenzy as oxygen enriched the planet. This way, Phtanum had its own great oxygenation event.

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Auctorozoic

2250 - 1430 mya

​The Auctorozoic is marked by the monumental emerging and diversifying of multicellular life on Phtanum. How this life looked is largely unknown. The lack of rock formations from this age specifically make estimating it difficult. This eon ended with an anomalous, simultaneous bombardment of large bodies, resetting multicellular life and resulting in death on a scale not seen since the Lygozoic.

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​Mezmerozoic

1430 - 890 mya

It took about 300 million years for life to recover and re-emerge in the same splendor it did in the eon before. The impacts enriched Phtanum‘s crust with all manner of heavier elements: Germanium, Titanium, Cooper, Iron and more. The life of the Mezmerozoic subsequently started using said chemicals in their bodies.

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Umbrozoic

890 - 460 mya

Much like the Auctorozoic, rock formations hailing from this era are rare. What little is known of the Umbrozoic implies that the planetary temperature was considerably higher than today. There are no indicationsnof significant extinction events. But not all things last forever.

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Chlorozoic

460 - 0 mya

The chlorozoic starts off with a mass extiction on the same scale as the end-Lygozoic and end-Auctorozoic ones. Microbes start to release chlorine and ammonia into the atmosphere. This causes many chain reactions. Mountains are eroded away by the halogens and the planet cools down. Water levels drop while the oceans become extremely saline. Extremophiles diversify, the planet turns acidic and Phtanum becomes what it is today.