Saponite

Afrodit aluminum-saponite auxite cathkinite ferroan saponite griffithite licianite lucianite. 

Saponite is a naturally occurring phyllosilicate clay of the smectite (montmorillonite) group. It is a magnesium-rich hydrated aluminum silicate and is present as a component of some commercial magnesium aluminum silicate clays. Saponite is a mineral with an approximate empirical formula owing to the variability in cation substitution see Table I. 

Saponite is a natural mineral clay that is a hydrous silicate of aluminum and magnesium. It occurs in soft, amorphous masses in the cavities of certain rocks. 

Saponite is composed of two tetrahedral layers formed by phylosilicate sheets and one octahedral layer. Common impurities include manganese, nickel, phosphorus, potassium, and titanium. 

Adsorbent emulsifying agent viscosity-increasing agent. 

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Polyimide-clay nanocomposites constitute another example of the synthesis of nanocomposite from polymer solution [70-76]. Polyimide-clay nanocomposite films were produced via polymerization of 4,4 -diaminodiphenyl ether and pyromellitic dianhydride in dimethylacetamide (DMAC) solvent, followed by mixing of the poly(amic acid) solution with organoclay dispersed in DMAC. Synthetic mica and MMT produced primarily exfoliated nanocomposites, while saponite and hectorite led to only monolayer intercalation in the clay galleries [71]. Dramatic improvements in barrier properties, thermal stability, and modulus were observed for these nanocomposites. Polyimide-clay nanocomposites containing only a small fraction of clay exhibited a several-fold reduction in the... 

FIG. 13 Reduction of the relative permeability coefficient is dependent on the clay platelet aspect ratio in the system of polyimide-clay hybrid with water vapor as the permeate. Each hybrid contains 2 wt% clay. The aspect ratios for hectorite, saponite, montmorillonite, and synthetic mica are 46, 165, 218, and 1230, respectively. (From Ref. 71.)... 

Chlorite is abundant in Cu-Pb-Zn-rich deposits but is scarce in Au-Ag-rich deposits. Fe chlorite is the most common and Fe-Mg chlorite is subordinate (Shirozu, 1969). Almost all of the chlorite is classified as orthochlorite which can be regarded as part of the clinochlore-daphnite solid solution series. In general, chlorite is intimately associated with sulfide minerals such as sphalerite, galena, pyrite, chalcopyrite, and pyrrhotite. A 7 A septechlorite was reported from the Toyoha Pb-Zn deposits (Sawai, 1980). Interstratified chlorite-smectite and vermiculite-saponite are rather common minerals in Au-Ag deposits (e.g., Yoneda and Watanabe, 1981), but they have not yet been reported from other deposits. 

Shirozu, H., Sakasegawa, T., Katsumoto, N. and Ozaki, M. (1975) Mg-chlorite and interstratified Mg-chlorite/saponite associated with Kuroko deposits. Clay ScL, 4, 305-321. 

Smectites are 2 1 charged layered silicates from natural (montmorillonite, hectorite, beidellite, saponite etc.) or synthetic (synthetic fluorohectorites, such as... 

Except for the PBS/SAP-qC16 (n-hexadecyl tri-n-butyl phosphonium cation modified saponite) system, the degree of degradation is the same for other samples. This indicates that MMT or alkylammonium cations, and at the same time other properties, have no effect on the biodegradability of PBS. The accelerated degradation of PBS matrix in the presence of SAP-qC16 may be due to the presence of alkylpho-sphonium surfactant. This kind of behavior is also observed in the case of PLA/MMT-based nanocomposite systems. 

Fig. 23.6. Calculated saturation indices (log Q/K) of aluminum-bearing minerals plotted versus temperature for a hot spring water from Gjogur, Hveravik, Iceland. Lines for most of the minerals are not labeled, due to space limitations. Sampling temperature is 72 °C and predicted equilibrium temperature (arrow) is about 80 °C. Clinoptilolite (zeolite) minerals are the most supersaturated minerals below this temperature and saponite (smectite clay) minerals are the most supersaturated above it.

The Na+- and Ca2+-saturated montmorilIonite, saponite and beidel-lite were obtained from Dr. J. L. McAtee, Chemistry Department, Baylor University. These minerals had been purified and prepared by methods described by Callaway and McAtee (15). Included in this paper for purposes of comparison are relevant data from previous studies in which hectorite and vermiculite had been doped with paramagnetic probes ( 7, 10). The chemical formulae of the low-Fe smectites and mermiculite are reported in Table I. 

An exception may be Na+-saponite, with a 1.37 nm spacing, which is probably interstratified between the single and double layer of water. 

Several general observations can be made from the spectra and the calculated ESR parameters. First, the Na+- smectites possess narrower resonance line widths than the Ca +-smectites, with the exception of the saponite. Since Ca +-smectites, unlike Na+ -smectites, do not disperse into individual platelets in aqueous suspension, the Na+-smectite films formed by drying suspensions onto a smooth flat surface have the silicate surfaces more perfectly oriented in the plane of the film. As a result, less angular variation of the z-axis of Cu + relative to the plane of the film would narrow the spectra. One can see evidence of hyperfine splitting in the gj component of the Na+-smectite spectra, but not in the Ca +-smectite spectra. Saponite, unlike the other smectites, has very similar spectral linewidths for the Na+ and Ca + form (Figure 16). Since this Na+-saponite sample does not disperse completely in water (Table II), the alignment of Na+-saponite platelets in the clay film may be no better than that of the Ca +-saponite. 

Clays and silicates sheets Montmorillonite, hectonite, saponite, fluorohectonite, vermiculite, Kaolin, etc. 

Saponite, idealized formula, 33 337 SAPO-n-zeolite-supported Pd catalysts, 39 208 Sarin, reaction with cyclohexaamylose, 23 237 Saturation in ESR, 22 280 SbF 37 168-172... 

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... 

The palagonite is thermodynamically unstable and, hence, reacts with seawater to form various clay minerals, including smectites (montmorillonite, nontronite, and saponite), micas (celadonite), and zeolites (phillipsite). This chemical weathering involves uptake of Si, Al, Mg, Ca, Na, and K and the release of water, reversing to some extent, the elemental effect of palagonitization. These mineral alterations tend to proceed progressively from the outer margin of the pillow basalts to their interior. 

This makes the magnitude and direction of the eiementai fluxes difflcuit to generai-ize because of their dependence on such variabies as the water s temperature and circuiation rate and the rock s porosity and chemicai composition. Low-temperature weathering of basait is aiso accompanied by precipitation of iron oxides and iron uptake into various ciays (nontronite, saponite, and ceiadonite). 

Fibrous saponite, with the analyzed chemical formula (Mgs g, AIq i, F o.i)(Si6.76> All o4 Fe 0.2) 02o(OH)4 IOH2O, also had Cao.i and Mgo4 as exchangeable ions (Midgely and Grass, 1956). Saponite is an example of a trioctahedral smectite. The variable chemical compositions of the smectites adds to the difficulties of accurate identification of these minerals. 

In order to prevent the effect of Fe impurities on fluorescence [6], an artificial clay, saponite (referred to as SA), was used as the starting material. Saponite with high transparency in the visible region was obtained from KUNIMINE Industry Co. Its chemical composition determined by atomic absorption spectroscopy was represented as... 

On addition of Na -saponite to the rhodamine-ethanol solution and the pyronine-ethanol solution, the color of the solutions gradually faded within a few hours, even at room temperature. All the composites were intensely colored, namely bright red for Rhodamine 590 and cardinal for Pyronine Y. 

As a function of the dye content intercalated, the relative intensity of fluorescence, the maximum wavelength in the fluorescence spectrum of lax d-spacing are illustrated in Fig. 2(a) for the pyronine Y-saponite composite (referred to as PY-SA), and Fig. 2(b) for the rhodamine 590-saponite composite (referred to as R590-SA). 

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