Our initial modeling of climate change and ecology began in the mid 1990s, when it seemed somewhat indeterminate if a consistent warming trend was actually present.

Subsequent data seem to indicate the planetary atmosphere and surface phenomena are apparently warming up slightly, on average, and may be due, in part, at least to atmospheric stoichiometry shift from hydrocarbon emissions, of which carbon dioxide might be the major contributing factor.

Clearly long term modeling of ecological phenomena is to some degree dependent on the assumed numerical distribution and activities of ones dominent species, or set of species, in the form of carbon based molecular combustion processes, often used for transportation, industrial and domestic heating purposes.

In such case one might be advised to margin the possibilities with optimistic, and worst case scenarios from hydrocarbon emissions growth perspectives.

Some technologies, for example next generation fusion reactors and long haul aerospace transport, may be well positioned to reduce hydrocarbon emissions.

It seems this somewhat dramatic turn of events implies significant long term shift, in virtually all of the planetary ecological systems.

Speculatively a planetary scale climate control system might be possible, in the long term future, implying a combination of surface, atmospheric and possibly space based modification systems.

Unfortunately moving thermal energy from the atmosphere to space on a large scale, in the case of a planetary cooling system may be problematic.

Possibly engineering a wavelength shift to a less opaque frequency range, may be feasible.

In terms of modeling planetary climate one might find ongoing investment in widespread sensor grids in the atmosphere, oceans, polar regions and continents, combined with appropriate persistence mechanisms and simulation platform, over the course of centuries, preliminary to climate modification in some form.

Assuming one has a reasonable model of the planetary surface environmental effects, it seems one might be able to simulate systemic change of the relative disposition of biomass amongst a wide array of planetary life forms.

Notably total biomass in a surface shell of a planet or moon is likely roughly constant, assuming one includes, for example petrochemical and coal deposits in the shell boundary.

Releasing carbon from deposits locked under the surface for some time implies a slightly greater number of particles available for incorporation into lifeform systems, overall.

As such one might expect a slightly greater biomass on the planetary surface, in the long term, as a result.