|
Normative mineralogy is a geochemical calculation of the whole rock geochemistry of a rock sample that estimates the ''idealised mineralogy'' of a rock according to the principles of geochemistry. Normative mineral calculations can be achieved via either the CIPW Norm or the Barth-Niggli Norm (also known as the Cation Norm). Normative calculations are used to produce an idealised mineralogy of a crystallized melt. First, a rock is chemically analysed to determine the elemental constituents. Results of the chemical analysis traditionally are expressed as oxides (e.g., weight percent Mg is expressed as weight percent MgO). The normative mineralogy of the rock then is calculated, based upon assumptions about the order of mineral formation and known phase relationships of rocks and minerals, and using simplified mineral formulas. The calculated mineralogy can be used to assess concepts such as silica saturation of melts. Because the normative calculation is essentially a computation, it can be achieved relatively painlessly via computer programs. == CIPW Norm == The CIPW Norm was developed in the early 1900s by the petrologists Cross, Iddings, Pirsson and the geochemist Washington. The CIPW normative mineralogy calculation is based on the typical minerals that may be precipitated from an anhydrous melt at low pressure, and simplifies the typical igneous geochemistry seen in nature with the following four constraints: # The magma crystallizes under anhydrous conditions so that no hydrous minerals (hornblende, biotite) are formed. # The ferromagnesian minerals are assumed to be free of Al2O3. # The Fe/Mg ratio for all ferromagnesian minerals is assumed to be the same. # Several minerals are assumed to be incompatible, thus nepheline and/or olivine never appear with quartz in the norm. This is, of course, an artificial set of constraints, and means that the results of the CIPW norm do not reflect the true course of igneous differentiation in nature. The primary benefit of calculating a CIPW norm is determining what the ideal mineralogy of an aphanitic or porphyritic igneous rock is. Secondly, the degree of silica saturation of the melt that formed the rock can be assessed in the absence of diagnostic feldspathoid species. The silica saturation of a rock varies not only with silica content but the proportion of the various alkalis and metal species within the melt. The silica saturation eutectic plane is thus different for various families of rocks and cannot be easily estimated, hence the requirement to calculate whether the rock is silica saturated or not. This is achieved by assigning cations of the major elements within the rock to silica anions in modal proportion, to form solid solution minerals in the idealised mineral assemblage starting with phosphorus for apatite, chlorine and sodium for halite, sulfur and FeO into pyrite, FeO and Cr2O3 is allocated for chromite, FeO and equal molar amount of TiO2 for ilmenite, CaO and CO2 for calcite, to complete the most common non-silicate minerals. From the remaining chemical constituents, Al2O3 and K2O are allocated with silica for orthoclase; sodium, aluminium and potassium for albite, and so on until either there is no silica left (in which case feldspathoids are calculated) or excess, in which case the rock contains normative quartz. 抄文引用元・出典: フリー百科事典『 ウィキペディア（Wikipedia）』 ■ウィキペディアで「Normative mineralogy」の詳細全文を読む スポンサード リンク
|