Boundary Layer Control On Mineral Reactivity In Soils And Rocks
It starts when the rain reaches the ground and percolates into the soil, infiltrating the first layers of the Earth’s crust where groundwater circulates. This water reacts with the rocks, dissolving some minerals and growing other ones.
In the presence of dissolved carbon dioxide, newly-formed minerals include various carbonate minerals such as calcite, magnesite, or siderite, which form by binding a dissolved carbonate group CO32- with calcium, magnesium, or iron, respectively. These minerals are widespread in the first kilometers of the Earth’s crust and may react with various other elements, including hazardous species such as arsenic, phosphate, selenium, or antimony. They can store these elements either as attached to the carbonate surface or directly incorporated in the crystalline structure.
Mineral-fluid reactions are usually modeled as occurring in the bulk fluid and following equilibrium geochemical theories. Such theories allow approximating the long-term evolution of complex fluid-rock systems that include various minerals, dissolved species, and water. However, at the atomic scale, the situation is more complex because several local out-of-equilibrium processes may control the formation of new minerals.
We have imaged the interactions between various carbonate minerals with either pure water or water that contained dissolved negatively-charged species (anions) such as arsenic, phosphate, selenium, and antimony. The technique of atomic force microscopy was employed because it allows imaging, as a function of time, the dissolution and precipitation processes over a mineral surface with nanometer height resolution and submicrometer spatial resolution.
In our experiments, we started with a given carbonate mineral and let some pure water flow over its surface, dissolving it. Dissolution occurs by the continuous removal of atomic layers from the carbonate. The dissolved species build a boundary layer of a thickness of a micrometer to a millimeter, where the fluid is locally more enriched than the bulk water into species coming from the dissolution of the carbonate. Such boundary layers act as microchemical reactors where new solid phases can form; the entire process is called an interface coupled dissolution-precipitation mechanism (Figure 1). When some toxic species are present in the fluid, they can be incorporated into these new solid phases, trapping them more permanently than if they kept dissolved in the fluid and transported with it.
We have studied several carbonate systems. When magnesite or dolomite, magnesium-bearing minerals, are the dissolving phase, nanoparticles of hydrated magnesium-rich minerals form at the surface. When calcite, a calcium-bearing carbonate, is the dissolving mineral, and in the presence of arsenic, phosphate, selenium, or antimony dissolved into the fluid, new minerals grow on the calcite surface in the form of nanoparticles (Figures 2, 3). When siderite, an iron-bearing carbonate, is the dissolving mineral, new precipitates are iron oxide minerals that can also trap some toxic species present in the fluid. This process of coupled dissolution-precipitation is therefore widespread, concerns most major carbonate minerals present in Earth surface environments, and can immobilize pollutants into solid phases.
We have identified the parameters controlling the formation of nanoparticles. For a fluid at a given acidity (pH), the solubility of the carbonate mineral and its dissolution rate control the thickness of the boundary layer and the time scales of the formation of nanoparticles, as long as the precipitation of the nanoparticles is faster than the dissolution of the carbonate. The boundary layer thickness may vary from several micrometers to several millimeters. The time scales necessary for the formation of the first nanoparticles is in the range of seconds to hours. Our theoretical developments provide therefore predictions for the boundary layer thickness and for the time scale of nanoparticle formation that could be tested in other fluid-mineral systems.
The evolution of a mineral-fluid boundary layer is a dynamic process where dissolved species concentrations will vary depending on dissolution and precipitation rates. The interface-coupled process that occurs in a micro-reactor, the boundary layer, controls many transformations of carbonate minerals in shallow Earth environments. An important property of this process is that it happens locally, even if the fluid is undersaturated with respect to the new precipitates at the macroscopic scale. This phenomenon has important environmental implications for the trapping of pollutants on calcite surfaces because the mobility of these pollutants in circulating groundwater is reduced. Such an effect has implications not only for global geochemical cycles of those elements but also for the remediation of contaminated geochemical systems such as acid mine drainage and effluents of municipal waste landfills.
These findings are described in the article entitled Timescales of interface-coupled dissolution-precipitation reactions on carbonates, recently published in the journal Geoscience Frontiers.
- Renard, F., Røyne, A., Putnis, C. V. (2019) Timescales of interface-coupled dissolution-precipitation reactions on carbonates, Geoscience Frontiers, 10, 17-27, https://linkinghub.elsevier.com/retrieve/pii/S1674987118300768.