Clay minerals secondary

Secondary minerals. As weathering of primary minerals proceeds, ions are released into solution, and new minerals are formed. These new minerals, called secondary minerals, include layer silicate clay minerals, carbonates, phosphates, sulfates and sulfides, different hydroxides and oxyhydroxides of Al, Fe, Mn, Ti, and Si, and non-crystalline minerals such as allophane and imogolite. Secondary minerals, such as the clay minerals, may have a specific surface area in the range of 20-800 m /g and up to 1000 m /g in the case of imogolite (Wada, 1985). Surface area is very important because most chemical reactions in soil are surface reactions occurring at the interface of solids and the soil solution. Layer-silicate clays, oxides, and carbonates are the most widespread secondary minerals. 

The use of barium sulphide as a secondary sulphidizer [4] was examined on oxidized lead ores from Sicily (BaS). The results obtained were encouraging. Sulphidization using Na2S can also be improved with the use of ammonium salts (chloride and sulphate). These reagents are used in cases where the ore contains clay minerals and calcium carbonate, which prevents suphidization due to the production of soluble calcium bicarbonate. The ammonium increases the solubility of calcium carbonate and improves sulphidization. 

The clay fraction, which has long been considered as a very important and chemically active component of most solid surfaces (i.e., soil, sediment, and suspended matter) has both textural and mineral definitions [22]. In its textural definition, clay generally is the mineral fraction of the solids which is smaller than about 0.002 mm in diameter. The small size of clay particles imparts a large surface area for a given mass of material. This large surface area of the clay textural fraction in the solids defines its importance in processes involving interfacial phenomena such as sorption/desorption or surface catalysis [ 17,23]. In its mineral definition, clay is composed of secondary minerals such as layered silicates with various oxides. Layer silicates are perhaps the most important component of the clay mineral fraction. Figure 2 shows structural examples of the common clay solid phase minerals. 

During this zone refining, the primary (igneous) rocks are transformed into secondary minerals. These include (1) clay minerals, such as phillipsite, chlorite, montmo-rillonite (smectite), saponite, celadonite, and zeolite (2) iron oxyhydroxides (3) pyrite (4) various carbonates and (5) quartz. These minerals form rapidly, within 0.015 and 0.12 million years after creation of the oceanic crust at the MOR. During these alteration... 

Reverse weathering Chemical reactions that are theorized to occur in the sediments. In these reactions, seawater is thought to react with clay minerals and bicarbonate producing secondary clays and consuming alkalinity and some cations. This process is approximately the reverse of chemical weathering on land that produces clay minerals. 

Primary minerals with low surface area (e.g., sihca minerals) and low reactivity mainly affect the physical transport of water, dissolved chemicals, colloids, immiscible (in water) liqnids, and vapors. Secondary minerals generally have high surface area (e.g., clay minerals) and high reactivity that affect the transport of chemicals, their retention and release onto and from the solid phase, and their surface-induced transformations. The sohd phase also can indirectly induce the degradation of chemical compounds, through its effects on the water-air ratio in the system and, thus, on microbiological activity. 

Melson, W. G. Thompson, G. 1973. Glassy abyssal basalts, Atlantic sea floor near St Paul s rocks petrography and composition of secondary clay minerals. Geological Society of America Bulletin, 84, 703—716. 

In the run MEL 1, the proportion of quartz relative to other secondary minerals increases from the hot to the cold extremity, whereas the proportion of K-feldspar decreases. Towards the cold end of the tube, K-feldspar is gradually overgrown by Na- and K-rich clays. Albite is totally overgrown by clays at the cold extremity. According to XRD patterns (Fig. 9) and chemical compositions (Fig. 10), the clay minerals are... 

The observed paragenesis contains a significant amount of feldspars. Although feldspars are not considered to crystallize in the numerical simulations (Jacquol 2000 Durst Vuataz 2001), our experimental results suggest that formation of clay minerals is controlled by previously crystallized feldspars. Therefore, the presence of feldspars is of importance for the crystallization of secondary minerals and the evolution of porosity in the stimulated reservoir of the HFR site. 

Abrajano, T. A., Bates, J. K., Woodland, A. B., Bradley, J. P. Bourcier, W. L. 1990. Secondary phase formation during nuclear waste-glass dissolution. Clays and Clay Minerals, 38,537-548. 

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