Kaszab Zoltán (szerk.): A Magyar Természettudományi Múzeum évkönyve 77. (Budapest 1985)
Szendrei, G. ; N. Tóth, M.: Contribution to the study on the crystallinity degree of kaolinites
Table 3. DTA, TG data and degree of order (DO) of the investigated kaolinites Locality Loss of weight due to water adsorption Endotherm reaction DO Exotherm Locality Loss of weight due to water adsorption peak temperature peak intensity loss of weight DO peak temperature peak intensity Locality % °C % % % °C % 1 Sedlec 1.3 600 79 12.2 62 980 71 2 Cserszegtomaj 1.3 595 42 7.3 32 985 20 3 Királyhegy 0.3 626 36 7.7 60 995 34 4 Georgia 0.3 605 82 9.7 68 1000 89 5 Keokuk 0.0 685 58 11.8 100 1000 64 6 Klösterle 0.7 605 59 8.0 79 995 46 7 Sokolov 0.3 600 48 6.7 72 980 38 8 Vidnova 0.7 580 58 7.7 47 975 41 9 Rochlitz 0.5 620 93 12.8 92 995 100 10 Passau 0.2 580 45 5.8 59 985 29 11 Maria mine 1 0.3 600 37 5.3 65 1000 34 12 Maria mine 2 0.0 610 36 5.3 78 1000 32 13 Petrifalau 0.7 605 60 10.3 64 995 59 14 Sasca-Montana 2.3 615 100 12.7 95 985 89 15 Ladoga lake 0.3 615 63 11.0 71 995 77 16 Kovaso 1 0.7 605 67 9.3 71 980 57 17 Kovaso 2 0.3 610 74 9.5 90 1005 63 Beside average deformation in the (001) direction, the coherently scattering domain size in the same direction was also measured. Both the deformation and the coherently scattering domain size are genetical parameters characterizing circumstances of formation as well. As it is well known, the width at half-maximum as a parameter of ordering includes a superposition of deformation and domain size. As it is shown in Table 2, the values of width at half-maximum (Bf( 001 )) show no great differences (0.26-0.59), while the extent of deformation and domain size vary in a wider range. As typical examples, the specimens from Kovaso 2, Klösterle, Rochlitz and Sasca-Montana are worth mentioning as they all have low deformation values and belong to the well-ordered kaolinites (on the basis of not only the deformations, but the degree of order as well), despite the high values of width at half-maximum which are characteristic for them, while the coherently scattering domain sizes (D^)) are small. From the relationship between DO and coherently scattering domain size (Fig. 3), it can be seen that the values belonging to the abovementioned kaolinites are defineiely separated from the points of the regression line. It seems that the same phenomenon can be observed with these samples (which can be placed among the well-ordered kaolinites according to the thermal parameters as well) as with that published by SMYKATZ-KLOSS (1974a). In his diagram of temperature versus At of the endothermic peak of the kaolinites, a deviation from the line of fireclay samples exists for the well-ordered kaolinites with slightly coarser grain size. It is to be mentioned that coherently scattering domain size and grain size are not identical but can be considered as genetical attributes related to each other. The relationships mentioned above proved that the kaolinite specimens selected for the investigations are suitable for the determination of these relations, and this fact stimulated us to investigate whether there was any correlation between the parameters of ordering
