[Hbond]

I would like to introduce another intuitive theory called ionization sharing. If one looks at the high temperatures and pressures of the fluid and solid chemical/ionized/plasma? states that occur within the earth, ionization should occur much further than expected with the temperatures observed, due to the pressure. Here is my reasoning. Normally when measuring ionization energy in the lab, the electrons are stripped into isolation. Within say the mantle of the earth, because of the close atomic proximity due to pressure, when an electron is ionized from one atom there is always another nearby electron to replace it. The difference in energy makes the ionization less exothermic.

In other words, as the pressure and temp increase, lower and lower orbtial electrons are being shared among the atoms. Only the lowest orbital electrons remain under monopoly control of the atoms. This allows things to get closer and denser bring lowering and lower electrons into states of ionization sharing.  If one assumes the ionization sharing of the first six outer electrons of oxygen one can correlate the changes of properties within the upper and lower mantle and within the transition regions between the upper and lower mantle and between the lower mantle and the fluid aspects of the earth's core.

[Hbond]

I would like to apply the theory of ionization sharing to the layers within the earth, up to the fluid region of the earth core. I will begin on the surface of the earth.

The earth’s surface is dominated by the oceans which are composed of water and dissolved minerals. Because of the effects of weather and underground seepage, water is also more or less present everywhere within the solid aspects of the crust. At the moderately high temperatures and pressures, that are found perhaps several miles within the crust, the water will change phase into a dense fluid when it reaches its critical point. In this critical water state, liquid-liquid water interactions are no longer supported, yet the high pressure maintains liquid volumes and flow characteristics.

Water at the critical point changes its chemical properties such that minerals become more soluble. The solubility effect of critical water increases in the presence of acids, bases and small dissolved ions. Smaller amounts of critical water within high pressure molten fluxes of minerals will also lower their melting point. The main point that is being made is that the critical state of water, combined with hydraulic pressure and mantle heat, allows water to be continuous from the surface to the mantle, first via underground liquid water channels, then via hydrothermal and high pressure hydrated molten flux channels dissolved in the crust by critical water.
 
If one looks at the solid crust material it is primarily composed of mineral oxides. This combined with the continuity of water from the surface to the upper mantle, implies that the  lower crust is relatively rich in oxygen and hydrogen. The oxygen combines within minerals to form crust and it combines with hydrogen to form water. Mediating these two phases within the lower crust is a critical brine phase, composed of critical water and dissolved ions.

As we enter the upper mantle, which should also be relatively rich in oxygen and hydrogen, due to hydraulics, billions of years of dissolving, and hydrogen enrichment due to the formation of continental crust materials, there is a transition phase where the chemical properties of water change again. This shift changes the critical brine phase into a ionized brine phase, which is a very dense high pressure ionized fluid. No solid crust material can exist within this phase. At the outer mantle, it probably has a composition similar to the crust/water dissolved into the oceans. It is also likely that all observed chemical bonds on the surface of the earth will break down in the ionization brine, such that the water will exist as ionized oxygen, hydrogen protons and electrons.

Because the plasma brine is a very hot, extremely dense, high pressure ionized fluid, chemical interactions within the ionization brine closest to the crust involve the outer most  2P electron of atomic oxygen increasingly leaving the permanent care of oxygen and becoming shared with other atoms, through transition style high pressure ionization sharing style chemical bonding. Below is a diagram of the ionization enthalpies of oxygen, Figure 1.




In the above figure, oxygen ionization, beyond maybe ionization number one or two, might appear to be beyond what is predicted by the temperatures measured within the mantle. This plotted data was generated using isolated oxygen atoms at low pressure. The data is useful but qualitative for the ionization brine because the plotted data does not take into consideration the solvent effect of dense high pressure ionized brine fluids, which allow the ionization sharing of outer and inner orbital electrons.

The solvent interactions with the ionization brine alters the nature of ionization energies,  because these electron are not stripped into isolation but are being loosely shared at all times, while no longer being restricted to a particular orbital position on a particular atom. In other words, if we were to label an outer electron of oxygen and place the atom in the ionization brine, that electron would become ionized and mobile between atoms (endothermic). Our test atom would still see constant electron density sharing within its outer orbitals (exothermic for the net lowering of ionization energy). This outer orbital electron sharing increases the density of the ionization brine allowing lower and lower orbital electrons to participate in the sharing as we move our way toward the higher pressures and temperatures of the core. This is something very loosely analogous to higher levels of ionization.


The ionization sharing of the six outer electrons of oxygen readily accounts for the very distinct mantle layers and the mantle and core transition regions. The upper mantle has one electron ionization sharing, leaving oxygen with the very stable 3-electron arrangement within its outer 2p orbitals (one electron in each 2p orbital). This stability is broken in the transition region between the upper and lower mantle. By the end of the lower mantle all the 2p electrons of oxygen are now being ionization shared. This leaves the oxygen with monopoply control of  only its two very stable 2s and two extremely stable 1s electrons. The ionization sharing within the D” layer between the mantle and fluid core region breaks the stability of the 2s electrons of oxygen and these become ionization shared. This leaves the oxygen monopoly control of only its two extremely stable 1s electrons, as the oxygen progresses further into the earth’s fluid core region.