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To gain insights into the composition and heterogeneity of Earth’s interior, the partial pressure of oxygen (oxygen fugacity, orfO₂) in igneous rocks is characterized. A surprising observation is that relative to reference buffers,fO₂s of mantle melts (mid-ocean ridge basalts, or MORBs) and their presumed mantle sources (abyssal peridotites) differ. Globally, MORBs have near-uniformfO₂s, whereas abyssal peridotites vary by about three orders of magnitude, suggesting these intimately related geologic reservoirs are out of equilibrium. Here, we characterizefO₂s of mantle melting increments represented by plagioclase-hosted melt inclusions, which were entrapped as basaltic melts migrated from their sources toward the seafloor. At temperatures andfO₂s constrained by rare earth element distributions, a range offO₂s consistent with the abyssal peridotites is recovered. ThefO₂s are correlated with geochemical proxies for mantle melting, suggesting partial melting of Earth’s mantle decreases itsfO₂, and that the uniformity of MORBfO₂s is a consequence of the melting process and plate tectonic cycling.

Plagioclase ultraphyric basalts (PUBs) are a class of mid‐ocean ridge (MOR) lavas found in a variety of ocean floor environments, are characterized by abundant (15–40 volume %) plagioclase megacrysts and a diverse trace element and isotopic signature. Paradoxically, we never see lavas erupted on the seafloor that are in equilibrium with these PUB megacrysts. Based on petrographic evidence, melt inclusion composition, and new data on depth of entrapment calculated from CO₂contents in plagioclase‐hosted inclusions, many of the megacrysts formed at upper mantle pressures (∼3–7 kbars). To constrain the composition of the parent magmas of the plagioclase megacrysts, we conducted a series of experiments at 5 and 10 kbars using mid‐ocean ridge basalts glasses as starting materials. The experimental results were consistent with the presence of a pseudoazeotrope in the anorthitic segment of the plagioclase + basalt pseudobinary. This has the effect of dropping the anorthitic end of the feldspar loop, lowering the solidus for upper mantle conditions, and driving evolving magmas toward higher Ca. As magmas rise and pressure drops, the pseudoazeotrope disappears, and the feldspar loop at the high‐An end rises, causing those magmas to undergo decompression crystallization of plagioclase and resorption of olivine. Therefore, the conditions which generated the magmas from which the megacrysts form disappear as the magmas rise and magmas evolve toward lower Ca, Mg (as we normally assume during plagioclase + olivine crystallization). In effect, the phase equilibria conditions that allow for the generation of such liquids also prevent them from being erupted as lavas.

The application of melt inclusions (MI) to infer magmatic processes assumes the MI have remained as constant mass, constant volume systems since the time of trapping. Understanding the effects of both compositional and volumetric re‐equilibration is key for the interpretation of MI data. Although the re‐equilibration behavior MI in quartz and olivine has been studied in some detail, the process is less understood for other MI host phases such as plagioclase, a common phase in igneous rocks. A MI can re‐equilibrate when it experiences pressure and temperature (PT) conditions that differ from formation PT conditions. During laboratory heating, irreversible MI expansion may occur. As a result, the internal pressure within the MI decreases, resulting in chemical and structural changes to the MI and host. We present results of heating experiments on plagioclase‐hosted MI designed to induce volumetric re‐equilibration. The experiments consisted of incrementally heating the MI to temperatures above the homogenization temperatures. At ∼40°C above, the temperature at which the daughter minerals melted, irreversible volume expansion lowered the pressure in the MI, and led to exsolution of CO₂into vapor bubbles. With each additional few degrees of heating, additional episodes of CO₂exsolution, bubble nucleation and expansion of the vapor bubblesoccurred. Re‐equilibration of MI in plagioclase occurred through a combination of ductile and brittle deformation of the host surrounding the MI, whereas previous studies have shown that MI in olivine re‐equilibrate dominantly through ductile deformation associated with movement along dislocations. This behavior is consistent with the differing rheological properties of these phases.

Plagioclase‐hosted melt inclusions are infrequently used to investigate magmatic processes owing to the perception that they are less robust than olivine‐hosted inclusions. Based on a set of time series experiments ranging from 30 min to 4 days, we demonstrate that plagioclase‐hosted melt inclusions can preserve the original (primitive) magmatic signal if steps are taken to correct for post entrapment crystallization. Diffusion within plagioclase‐hosted melt inclusions is sufficiently fast that the melt inclusions can be homogenized within 30 min through heating experiments. As heating time increases, the composition of melt inclusions drifts. We attribute this longer‐term phenomenon to plastic deformation of the host plagioclase (crystal relaxation) inducing a decrease in the internal pressure in the melt inclusion combined with diffusion of elements across the host/melt inclusion interface. The rate of chemical reequilibration within melt inclusions is limited by the much slower rate of diffusion within the solid host. Indeed, the host/melt inclusion partition coefficient for MgO decreases by 25% from the 30‐min to the 4‐day experiments. Our results suggest that the primary character of plagioclase‐hosted melt inclusions can be recovered if one recognizes and corrects for the effects of the complex physical and chemical processes that occur during melt inclusion homogenization.