Carbonated Serpentinite (Listwanite) at Atlin, British Columbia: A Geological Analogue to Carbon Dioxide Sequestration

The Force of Crystallization and Fracture Propagation during In-Situ Carbonation of Peridotite

“…The principal reactions expected during carbonation of peridotites by injection of CO 2 plus water (or brine) are listed in Table 5 (e.g., see [53][54][55][56][57][58]), along with the associated net changes in solid and total volume calculated for a temperature of 423 K and a hydrostatic pressure of 50 MPa. These data show that the main CO 2 -mineralizing reactions (Reactions R.1, R.3, R.4, and R.6, Table 5) are characterized by large changes in solid/fluid volume.…”

Source of the mineralizing fluids in ultramafic related magnesite in the Eskişehir area, northwest Turkey, along the İzmir–Ankara Suture: a stable isotope study

“…Schroll (2002) described the Kraubath type (Pohl, 1989) magnesite deposits as crypto/micro-crystalline, white-colored magnesites that occur in concretions in the soil or in sediments immediately overlying or adjacent to ultramafic rocks, and in strings and veins or stockworks in ultramafic bodies. Magnesite deposits hosted in extensively altered ultramafic rocks are common throughout the world and occur with minor amounts of talc, quartz, and dolomite (Griffis, 1972;Barnes et al, 1973;Duski and Morteani, 1989;Jedrysek and Halas, 1990;AbuJaber andKimberley, 1992a, 1992b;Schandl and 1992; Prasannakumar et al 2002;Ghoneim et al, 2003;Gartzos, 2004;Hansen et al, 2005;Robinson et al, 2005;Akbulut et al, 2006). Meter to kilometer magnesite veins are interpreted in terms of ultramafic rocks that interacted with CO 2 -bearing meteoric/hydrothermal fluids, where prolonged regional tectonics have been active, producing continuous networks of shallow crustal fractures (Pohl, 1989;Boschi et al, 2009).…”

Reject Brines from Desalination as Possible Sources for Environmental Technologies

“…This idea was first proposed by Seifritz in 1990. There is little risk of unexpected release of CO 2 back to the atmosphere, because the resulting carbonates are thermodynamically stable (Ballirano et al, 2010;Ferrini et al, 2009). The process occurs naturally on a small scale during the weathering of rocks (Robertson, 2004), and has been shown to be important locally in ultrabasic and ophiolitic complexes (Hansen et al, 2005). The source of the neutralizing ions could be magnesium and calcium silicates such as olivine, serpentine-group minerals and clinopyroxene.…”