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MINERALOGY AND RADIOACTIVITY OF SOME PEGMATITE BODIES, SOUTHEASTERN SINAI, EGYPT

The area under consideration constitutes the extreme eastern part of the Kid metamorphic belt in Sinai Peninsula. The Neoproterozoic rock units exposed there comprise gneisses, migmatites, old granitoids and monzogranites. Most of the pegmatite bodies encountered in the monzogranite rocks occur as plug-like bodies and veins of variable dimensions. These studied pegmatites are mainly of the simple unzoned type. They are composed of intergrowths of smoky quartz and pink K-feldspar with some accumulations of micas which host most of radioactive mineralizations. Radiomertrically, the concentration of eU ranges between 41 and 117ppm with an average of 73ppm, while eTh varies between 160 and 433ppm with an average of 223ppm. The Ra content reaches up to 94ppm with an average of 62ppm. The radioelements variation diagrams illustrate that the distribution of radioelements is due to both magmatic origin and hydrothermal redistribution. The high level of radioactivity in the studied granitic pegmatites is mainly resulted from the presence of ishikawaite, thorite, uranothorite, thorianite, zircon, betafite and fluorite. Most of the studied radioactive minerals commonly occur in the metamict state. Other accessory minerals like anatase, hematite and magnetite are also recorded. The study reports for the first time the presence of Ishikawaite-Th, where Th prevails U. Ishikawaite-Th grains contain exsolution intergrowths of ishikawaite-U and thorianite.


INTRODUCTION
Post-collision alkaline magmatism (~610-580 Ma) is widely distributed in the northern part of the Neoproterozoic Arabian-Nubian Shield (ANS), i.e. the northern part of the Egyptian Eastern Desert and Sinai. The basement rocks of southern Sinai were recently studied in detail by many authors (eg. El Sayed 1993;El Mowafy 1994&2003;Hamd 1995;El Metwally, 1993;Moghazy et al., 1998;El Aassy et al. 1999, Abu El-Enen, 2008. The present study throw light on the radioactivity and mineral constituents of some mineralized pegmatite bodies, existing in the study area.

GEOLOGIC SETUP
The area under investigation occupies the extremely eastern part of the Kid metamorphic belt in Sinai Peninsula. It is bounded by lat. 28° 15´ -28° 25´ N and long. 34° 05´ -34° 15´ E, and covers an area of about 90km 2 covered by crystalline igneous, metamorphic rock units and quaternary alluvial sediments. These rock units comprise gneisses and migmatites, old granitoids and monzogranites (Fig.  1). These rocks are dissected by several wadies; Wadi Majirat, Wadi Marwa, Wadi Candali and Wadi Yethmid in addition to their tributaries filled with alluvial sediments.
ISSN 2314-5609 Nuclear Sciences Scientific Journal vol. 1, p 57-68 2012 58 HESHAM A. EL NAHAS Gneisses and migmatites represent the rocks mainly surrounding the monzogranites from north, east and west. These rocks are intruded by old granitoids and monzogranites with sharp contacts (Fig. 2a). They form moderate to low relief and characterized by the foliation and gneissose structures with alternation of melanocratic and leucocratic bands. They are composed mainly of biotite-hornblende and quartz-feldspar rich bands respectively. The old granitoids crop out at Wadi Yethmid to the extreme west of the study area. They are hard, massive, medium to coarse-grained and grey to yellowish grey in color forming moderate to low relief. These old granitoids in the area vary in their composition from tonalite to granodiorite and composed essentially of plagioclase, quartz, K-feldspar, biotite and hornblende.
Monzogranites, of high to moderate relief, are the main rock unit and occupy the central part of the study area. The monzogranites are characterized by red to pink color, medium to coarse-grained and sharp contacts with the adjacent rock units. Apophyses and off shoots commonly extend from monzogranites to the country rocks (El Feky et al., 2011). Monzogranites of G. Marwa are extensively fractured and jointed. They are invaded by pegmatite bodies and veins. Pegmatites encountered in the study area mostly occur as small veins, pockets and pod-like bodies of variable dimensions in monzogranites. Salterly (1957) divided the pegmatites into simple and complex. Most of the pegmatite bodies in the study area are of the simple zoned type of Salterly (1957) composed of intergrowths of smoky quartz and pink K-feldspar with some accumulations of micas in which most of radioactive mineralizations are present (Fig. 2b). Texturally, pegmatites are distinguished by large size crystals compared to the normal grain size of the hosting monzogranites.

SAMPLING AND TECHNIQUES
A total of eleven samples were collected from different pegmatite bodies encountered in monzogranites around the different wadies for radiometric and mineralogical studies. These samples were subjected to comminution processes through a laboratory jaw crusher and roll mill to liberate the considered

59
MINERALOGY AND RADIOACTIVITY OF SOME PEGMATITE BODIES radioactive minerals from the other gangue ones. Quantitative determination of the radioactive elements; eU, eTh, Ra(eU) and K was obtained using the multi-channel analyzer of γ-ray spectrometer, (NaI "T1"-detector). The system of γ-ray spectrometry consists of bicorn scintillation detector, NaI "T1" crystal 76x76mm, hermitically sealed with a photomultiplier tube in aluminum housing. A proper weight (300-350 gm) of the crushed sample was placed in a standard size plastic container, sealed well and left for at least 30 days to accumulate free radon and to attain radioactive equilibrium.
Because of these radioactive minerals mainly occur in the medium to very fine sized fractions, the samples were sieved by using 1mm and 0.053mm sieves. The in-between fractions (1-0.053mm) were subjected to the heavy liquid separation using bromoform solution (sp. gr. 2.81g/cm 3 ) and methylene iodide solution (di-iodomethane with sp. gr.= 3.31g/cm 3 ). The obtained heavy fractions were magnetically classified according to the magnetic susceptibility of the heavy minerals. Magnetite was removed using a permanent hand magnet. The free-magnetite heavy minerals fractions were fractionated using the High Intensity Frantz Isodynamic Magnetic Separator (model L-1). These magnetic fractions were examined carefully by the binocular stereomicroscope, X-ray Diffraction (XRD) technique using Philips Xray diffractometer (Model PW-1050/80) and Environmental Scanning Electron Microscope (ESEM) using Philips Model XL 30 supported by an energy dispersive X-ray unit (EDX).

PETROGRAPHIC CHARACTERISTICS
Monzogranites in the study area are generally massive, medium to coarse-grained and characterized by their greyish pink color. They are composed essentially of plagioclase, quartz, potash feldspar, with minor mafic minerals exhibiting hypidiomorphic texture. Zircon, allanite, sphene and opaques are the main accessory minerals, while the secondary minerals include chlorite, sericite and kaolin.
Plagioclase (An 15-23 ) forms anhedral to subhedral grains and shows zoning and lamellar twinning (Fig.3a). Potash feldspar forms subhedral to anhedral prismatic crystals of string and patchy perthitic texture. Sometimes, the minerals of the perthitic texture show partial alteration to sericite. Quartz occurs as anhedral coarse grained crystals. Some quartz minute crystals are occupying the reaction boundaries between perthite crystals. Mafic minerals are mainly biotite and hornblende. Biotite occurs as subhedral to anhedral irregular flakes, strongly pleochroic from yellowish brown to dark brown. Some biotite crystals are partially altered to chlorite and iron oxide (Fig.3b). Hornblende occur as subhedral elongated crystals and characterized by strong pleochroism from brownish green to green color. Zircon is present as randomly distributed fine to very fine-grained euhedral crystals commonly associated with biotite and rarely in plagioclase and quartz. Allanite occurs as fine euhedral to subhedral crystals and characterized by zonation (Fig. 3c). Sphene is present as prismatic, rhombic and sometimes anhedral crystals (Fig. 3d).
The studied pegmatites are massive, coarse to very coarse-grained and buff in color. Petrographically, they consist of megacrysts of potash feldspar, quartz, plagioclase in addition to biotite and muscovite. Potash feldspar occurs as subhedral to euhedral coarse grains and represented as perthitic texture and antiperthite crystals forming graphic texture with quartz and plagioclase. Most of quartz crystals occur as megacrysts graphically intergrown with both textures (Fig. 3e, f), while some of them are present as minute crystals between potash feldspar crystals. Plagioclase (An 10-20 ) ranges in composition from albite to oligoclase. It occurs as subhedral to anhedral crystals and characterized by lamellar twinning and sometimes corroded with potash feldspar and quartz (Fig. 3g). Biotite flakes are characterized by strong pleochroism from yellowish brown to dark brown color (Fig. 3h). Muscovite flakes are commonly associated with quartz and potash feldspar. Fig.3: Photmicrographs of a)crystal of hornblende included within plagioclase, monzogranites, b)zircon, biotite and chlorite, monzogranites, c)zoned crystal of allanite associated with quartz and plagioclase, monzogranites, d)sphene with zircon in chloritized biotite and basal section of hornblende, monzogranite, e)megacryst of minerals in perthitic texture graphically intergrown quartz, pegmatite, f)megacryst of antiperthite graphically intergrown quartz, pegmatite, g)plagioclase associating quartz, pegmatite, and h)biotite associating antiperthite and quartz, pegmatite

RADIOACTIVITY
The results of the radiometric measurements of eU, eTh, Ra(eU) and K for the studied pegmatite samples with the calculated ratios; eTh/eU and eU/Ra are listed in Table  (1). The radiometrical element concentration of eU ranges between 41 and 117ppm with an average of 73ppm, while eTh varies between 160 and 433ppm with an average of 223ppm. The Ra(eU) content reaches up to 94ppm with an average of 62ppm. Most of the studied samples exhibit low concentrations of K, (P 9 11). This may be attributed to the post magmatic processes that affected the studied rocks as koalinization. The results reflect the high concentrations of Th and U in the studied mineralized pegmatites due to the presence of the radioactive minerals as will be seen. Uraniferous granites and pegmatites are radiometrically characterized by high contents of U ( >8 ppm) and/or Th ( >16 ppm) with or without U mineralization (Darnely, 1982). The studied pegmatites have higher values of eU and eTh than those recorded for the World uraniferous pegmatites (av=28 and 21 for U and Th respectively, Ford, 1982). Also, these values are higher than those of the Egyptian uraniferous pegmatites(av.=33 and 28ppm for U and Th respectively, Moharam, 2004&2006).
The average eTh/eU ratio of the pegmatite bodies is 3.23, which is slightly less than the average continental crust value of approx. 3.8 (Van Schmus, 1995). Most of pegmatite samples have eU/Ra ratio more than unity (av.=1.2) reflecting a state of positive radioactive disequilibrium. This may be due to the scape of some Ra during the alkaline hydrothermal solutions. The eU-eTh variation diagram (Fig. 4a) for the studied pegmatites reflects positive correlation indicating that the magmatic processes played an important role in the concentration of radioelements. The figures show also that there is ill-defined relation between eTh/eU and eTh (Fig. 4b) and negative relation between eTh/eU and eU (Fig. 4c), suggesting that the distribution of radioactive elements is due to magmatic processes as well as hydrothermal redistribution (Charbonneau, 1982). The average eU, eTh, Ra and K for the surrounding monzogranites is 13, 18, 7ppm and 3.51% respectively (El Feky et al., 2011). The studied pegmatites compared to these monzogranites have higher concentrations of these radioelements.
Table (1): Radioelements concentrations of eU, eTh, Ra(eU) and K and some ratios for the studied granitic pegmatites.
Av.MG = Average concentrations of the radioelements for the surrounding monzogranites of G. Marwa (El Feky, et al., 2011).ULD = under limit of detection.

MINERALOGY
In fact, most of the radioactive mineralizations of the studied pegmatites in the study area are associating the existing mica agglomerations. The most common radioactive and important minerals of the studied pegmatites are ishikawaite, thorite, uranothorite, thorianite, zircon, betafite and fluorite in addition to anatase, hematite and magnetite.

Ishikawaite: [(Th,U,Y,REE,Ca)(Nb,Ta,Ti)O 4 ]:
Ishikawaite is considered as uranium and thorium-rich samarskite mineral. Ishikawaite mostly occurs as medium to fine anhedral crystals, black to dark brown in color with vitreous luster and concoidal fractures (Fig. 5). The obtained data from ESEM analyses of the studied grains were plotted on the ternary diagram of Hanson et al., (1999), which shows that all points locate in ishikawaite field (Fig.  6) due to the dominant U and Th. In fact, the ESEM analyses of ishikawaite mineral grains reveal that most of the analyzed grains show Th exceeds U (Fig. 7a&c), whereas some grains are characterized by U exceeding Th (Fig. 7b). So, ishikawaite can be classified, in the term of abundance of U and Th, as ishikawaite-Th and ishikawaite-U. Some ishikawaite-Th grains contain unoriented lamellae of ishikawaite-U (Fig. 7c). Regarding to REE content, Hanson et al.,( 1999)   The mineral grains are completely metamict, which was reflected by the amorphous X-ray diffraction pattern, so the annealing to 1100ºC for about six hours for X-ray diffraction analysis was necessary. The obtained xray diffraction pattern of the annealed sample is plotted on Figure (6), illustrates that the mineral is wholly metamict and growing of the diffraction peaks of the mineral by annealing.

Thorianite [(Th,U)O 2 ]:
The mineral is rarely observed in the studied mineralized pegmatite samples. It occurs as fine anhedral crystals of black colors and metallic to submetallic luster. Mostly, thorianite grains are associated as inclusions within ishikawaite-Th, as shown in backscattered ESEM image and analysis (Fig. 7a&c). The mineral, also contains appreciable amount of Nb up to 34%. It is worthy to point out that thorianite in the studied pegmatites may be formed as exsolution intergrowths in ishikawaite-Th mineral grains.

Thorite [ThSiO 4 ]:
Thorite occurs as anhedral to subhedral fine to very fine mineral grains that exhibit black to brownish black colors with metallic to submetallic luster (Fig. 9). The brownish tint of the studied grains may be due to the incrustation with iron oxides (El Nahas, 2006). Th and Si constitute the essential elements forming the mineral, while Zr, U, Ca, Fe and Al are the elements existing in trace amounts (Fig. 10). Some thorite mineral grains contain appreciable amounts of more than 15% UO 2 , so it can be referred as uranothorite (Fig. 10). The X-ray diffraction data are listed in Table ( (Dardier, 1999;Abdel Warith, 2001 andEl Mansi et al., 2004). Zircon occurs as euhedral to subhedral yellowish grey to greenish grey, translucent to opaque mineral grains with resinous luster, which is referred as malacon zircon (Fig. 11). Decay of the radioactive elements in the zircon causes the bombardment of the structure by alpha particles, which gradually disrupt the structure. This disruption is reflected in the optical properties of the zircon and the adjacent parts of the surrounding minerals, where zircons loose their transparency, and birefringence decreases. Poldervaart (1956) suggested that malacon may be also formed as the result of hydrothermal alteration. In this case, the zircons are non-radioactive. The mineral is composed essentially of ZrO 2 and SiO 2 with traces of ThO 2 , Hf 2 O 3 , Fe 2 O 3 , CaO, UO 2 and Al 2 O 3 (Fig.  12). The average Zr/Hf ratio is 21.32 reflecting the acidic origin of the magma from which these zircon were originated. Noteworthy, many of thorite and zircon grains in the studied granitic pegmatites show solid solution range, where Zrrich thorites and Th-rich zircons are present. Förster (2006) demonstrated that the local disequilibrium processes such as supersaturation may have aided in the precipitation of the metastable thorian zircon and zirconian thorite. A sample of zircon was heated to 1000ºC for three hours and analyzed using X-ray diffraction technique. The obtained data are listed in Table (2), which indicate that the presence of thorite diffraction peaks in addition to that of zircon reflecting the intermediate solid solution of zircon and thorite. According to Rozendaal and Philander (2000):

Betafite[(Ca,U)2(Ti,Nb,Ta)2O6(OH)]
Pyrochlore group of minerals are classified into three subgroups on the basis of the B-site composition (Hogarth, 1977): pyrochlore is the Nb-dominant member, microlite is the Ta-dominant member and betafite has 2Ti > (Nb+Ta). Hogarth (1961) demonstrated that a compositional series exists between pyrochlore and betafite, thus firmly establishing betafite as a member of the pyrochlore group. Betafite is rarely observed in the studied granitic pegmatites of the study area and was detected by ESEM technique. It occurs as anhedral fragmental grains of black color and vitreous luster. It is characterized by its concoidal fractures and yellow superficial alteration of some betafite grains (Fig. 13). ESEM analyses of some betafite grains reveal that they consist mainly of Nb, U, Ti with appreciable amount of Fe, Si, Y, Ta, Mn, Th and Al (Fig. 14).

Fluorite [CaF 2 ]:
The hig alkalinity in the magmatic melts and mineralizing solutions play an important role due to the presence of fluorine which caused full separation of the LREE and hence preferential accumulation of the HREE in the fluorite (Bulnayev and Kaperskaya, 1990). Fluorite in the studied pegmatites exhibit wide range of colors from colorless, pale blue to dark violet with vitreous and resinous luster (Fig.15). Allen (1952) concluded that the coloration of fluorite can be attributed to the action REE during the differentiation of the magma, presence of manganese or distortion in the crystal structure. EDX mineral analysis of the mineral reveals that it is composed essentially of Ca and F with the presence of trace amounts (<3.5%) of Si, Al, Mn and Fe. Some fluorite mineral grains contain inclusions from ishikawaite and thorite (Fig. 16). Table (3) gives the X-ray diffraction data of the picked fluorite grains from the studied pegmatites.

Anatase [TiO 2 ]:
Most of anatase grains in the studied pegmatites occur as anhedral to subhedral opaque yellow to yellowish brown grains with resinous luster (Fig. 17). It consists entirely of TiO 2 with appreciable amount of Fe 2 O 3 and traces of CaO and K 2 O (Fig. 18).