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Ophiolites from the Egyptian Shield: a Case for a Possible Inter-Arc Basin Origin ,' '"'!

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Ophiolites from the Egyptian Shield: a Case for a Possible Inter-Arc Basin Origin ,' ' MITI.ÖSTERR.MINER.GES. 148( 2003) OPHIOLITES FROM THE EGYPTIAN SHIELD: A CASE FOR A POSSIBLE INTER-ARC BASIN ORIGIN 2 A. Y. Abdel Aatl, E. S. Farahatl, G. Hoinkes & M. M. EI Mahalawil l Department of Geology Minia University, El-Minia 61 l l l, Egypt 2Jnstitute of Mineralogy and Petrology University of Graz, Universitätsplatz 2, A-8010 Graz, Austria The pyroxene and whole-rock chemistry of the ophiolitic metavolcanics of Wadi Um Seleimat (WUS) and Muweilih (MU) areas in the central Eastem Desert of Egypt are presented. WUS ophiolite suite seems to be intact where it comprises (from bottom to top): serpentinites, pyro­ xenites, metagabbros, massive diabases and pillowed metavolcanics. MU metavolcanics, about lO km to the southeast of WUS area, consists predominantly of metabasaltic-metadiabasic pillowed and massive lava flows together with the corresponding pyroclastics. These meta­ volcanics, together with their associated metagabbros and serpentinites, can be considered as a part of a dismembered ophiolite sequence. The mineral assemblage in WUS rocks is: albite, chlorite, epidote, titanite, calcite and quartz, which indicates a low greenschist facies (230-320'C) metamorphism. The mineral assemblage of MU metavolcanics includes: albite, actinolite, homblende, epidote, chlorite, titanite, calcite, quartz and ilmenite that reflectsa transitional greenschist-amphibolite facies metamorphism.Few samples of WUS contain plentiful clinopyroxene phenocrysts in plagioclase-free glassy ground­ mass. These features aretypical of rocks of boninitic affinity. Whole-rock and pyroxene chemistry demonstrate that the metavolcanics ofboth areas are mainly andesitic basalts with tholeiitic affinity. The boninitic affinity of some samples fromWUS area is shown on Ti0z-Si02/IOO-Na20 diagram of pyroxenes (Fig. l). On the other hand, clino­ pyroxenes from metavolcanics associated with the boninitic rocks plot mostly in the island-arc tholeiites and mid-ocean ridge basalt fields. TiOz Clinopyroxenes from Muweilih area plot in island-arc tholeiitic-MORB overlap area. Fig. 1 TiOrSi02"100-Na20 diagram of pyroxenes [1]. MORB: mid-oeean ridge basalts; WOPB: within ' '11 oeean plate basalts; IA T: island-are tholeiites; ,' '"'!' . BON+BA-A: boninites+basaltie andesites and ,' /I I / \ ..,.,._, .,,,. andesites from inter oeeanie fore-are regions. ,_' . e - -'� BON +BA-A - C/osed eire/es: Wa di Um Seleimat; Open squares: SiOzllOO so Muweilih. 81 The studied boninitic samples are classified as intennediate-Ti boninites [2]. On the TiOrZr diagram (Fig. 2) WUS rocks fall in volcanic-arc field and the area shared between MORB and volcanic-arc basalts, with high affinity to the latter. On the other band, MU metavolcanics plot mostly in the volcanic-arc MORB overlap area, which may refer to their back-arc basin affinity. In agreement with most of the above discussed discrimination diagrams, WUS metavolcanic MORB nonnalized pattems (Fig. 3) are generally similar to those of the immature island-arc tholeiites, with relative low HFSE and high LILES than those of MORB. In contrast, MU meta­ volcanics have MORB-nonnalized pattems with HFSE value close to unity and relative enrichment in MORB LILE (Fig. 3). These features may imply a transitional MORB-island­ arc (i.e. back-arc basin) affinity of these rocks. Fig. 2 O . J _ _ _ _ 10.__ ......... ..._....._......._........._......_...._100 _._ ....._..._....... u..i ....._. 1000 Ti02 vs. Zr discrimination diagram [3]. Zr ppm Symbols as in Fig. 1. Wadi Um Seleimat ; � l r::������������n { 1 „,. 0. 1 0. 1��_.___,___,___,___,____.___.___.__._.Y Yb Sr K Rb Ba Th Ta Nb Ce P Zr HfSm Ti Y Yb Sr K Rb Ba Th Ta Nb Ce P Zr Hf Sm Ti Fig. 3 MORB-normalized incompatible element spidergrams [3]. As modern boninites are foundonly in supra-subduction zone settings, it is inferred that ancient boninites also fonnedabove a subduction zone. In the case ofWUS metavolcanics, the previous geochemical studies [4] recognized their supra-subduction, i.e. fore-arc environment. However, the available data in the present study do not support such a model forthe followingreaso ns: a) the boninites overlie the arc-tholeiites; b) the absence of the sheeted dykes, which indicates in­ complete extension; c) the thin volcanic section of this ophiolite and d) the little pyroclastics associated. These criteria may represent primary features of ophiolite fonnation in an incipient or rifted island-arc setting where arc volcanics are separated by thinner marginal basin crust [5]. 82 Consequently, WUS tholeiites-boninite sequence appears to reftect the transgression from arc­ style to (incipient) back-arc style volcanism. If the present interpretation is correct, MU meta­ volcanics, which lie about 10 km to southeast of WUS ophiolite sequence and display a back­ arc geochemical characteristic, may represent a more advanced stage ofthis inter-arc basin while those of WUS represent their embryonic stage. The association of WUS and MU metavolcanics with ophiolitic melange, which comprises ophiolitic dismembers of serpentinesand metagabbros within the island-arc metavolcanics and volcanoclastic metasediments [6] are compatible with the above suggestion. References [l) BECCALUV A, L., MACCIOTA, G., PICCARDO, G. B. & ZEDA, 0. ( 1989): Clinopyroxene composition of ophiolitic basalts as petrogenetic indicator. - Chemical Geology, 77, 165-182. [2) BEDARD, J. H. (1999): Petrogenesis of boninites from the Betts Cove ophiolite, Newfoundland, Canada: identification of subduction source components. - Journal of Petrology, 40, 1853-1889. [3) PEARCE, J. A. ( 1982): Trace element characteristicof lavas fromdestructive plate boundaries. - In: R. S. Thorpe (Editor), Andesites. Wiley, New York, pp. 525-548. [4) ABU EL ELA, F. F. (1990): Supra-subduction zone ophiolite of Qift-Qusseir road, Eastern Desert, Egypt. - Bulletin Faculty of Science, Assiut University, 19, 51-70. [5) SHERVAIS, J. W. & KIMBROUGH, D. L. (1985): Geochemical evidence of the tectonic setting of the coast Range ophiolite: a composite island-arc- oceaniccrust terrain in Western California. - Geology, 13, 35-38. [6) AZZAZ,S. A., SABET, A. H., HASSAN, G.A. & EMAM, M. F. (1997): Ophiolites and the associatedmelange of the Abu Mereiwa area along the Qift-Quseir Road, Eastern Desert, Egypt. - Bulletin Faculty of Science, Assiut University, 26, 141-163. 83 Mrrr.ÖsTERR.MINER.GES. MB (2003) DIE ROLLE DER GEOLOGIE BEI NEUEN BERGBAUPROJEKTEN G. Anthes Technisches Büro für Geologie - GEOsolutions Weißenbach 255, A-5351 Strobl, Austria Die Neuanlage von obertägigen und/oder untertägigen Bergbauten steht heute in enger Beziehung zu wirtschaftlichen, rechtlichen, raumordnerischen und gesellschaftlichen Belangen. Daher muss die Gewinnungstätigkeit von mineralischen Rohstoffen nachhaltig und effizient geplant und durchgeführt werden. Für die Auswahl der geeignetsten Lagerstätte, der bestmöglichen Aus­ nutzung der Lagerstättenvorräte (Lagerstättenschutz) und einer optimalen Qualitätssteuerung kommt daher der Geologie eine besondere Rolle bei der Planung von neuen Bergbauprojekten zu. Die genaue Kenntnis der geologisch-lagerstättenkundlichen Verhältnisse im Rohstoffvorkommen mit einem hohen Grad der geologischen Gewissheit setzt ein detailliertes Explorations- und Pro­ spektionsprogramm voraus, dass auf die speziellen geologischen Bedingungen im Prospektions­ gebiet abgestimmt sein muss. Dazu stehen dem Geowissenschaftler eine Vielzahl von modernen, mineralogischen, petrographischen, geochemischen, strukturgeologischen und geophysikalischen Untersuchungsmethoden zur Verfügung, die sinnvoll aufeinander abgestimmt und eingesetzt werden müssen, um effizient das Prospektionsziel - die hinreichend genaue Kenntnis über Lage, Erstreckung, Aufbau, Inhalt, Struktur und Qualitätsverteilung der Lagerstätte - erreichen zu können. Diese geologisch-lagerstättenkundlichen Daten bilden die Grundlage fürdie gesamte Bergbau­ planung, insbesondere für die Konzeptionierung der Geometrie, Gewinnungs-, Förder- und Maschinentechnik sowie der Sicherheit des Abbaus. Insbesonderebei hochwertigen und seltenen mineralischen Rohstoffen stellt eine optimale Qualitätssteuerung sowohl aus betriebswirt­ schaftlichenals auch volkswirtschaftlichen (Lagerstätteneffizienz)Gründen eine wesentliche Vor­ aussetzung für einen effizientenAbbaubetrieb dar. Die Anforderungen an die Qualitätssteuerung hängen aber nicht nur von Produktanforderungen, sondern im wesentlichen auch von der Komplexität der Lagerstätte ab. Allgemein kann gesagt werden, dass eine nicht-optimale Qualitätssteuerung durch fehlende oder ungenügende geologische Kenntnis der Lagerstätte jedenfallseine Verringerung der Produktqualität und somit Erlöseinbußen zur Folge hat. Weiters kann eine Erhöhung des Anteils nicht verwertbaren Materials (und damit erhöhtes Halden­ volumen) bzw. eine Verringerung der Vorräte (Verlust hochwertiger Qualität durch unbeab­ sichtigte Vermengung mit geringwertigem Material) daraus resultieren. 84 Im Rahmen der Wirtschaftlichkeitsberechnungen, der Wertschöpfungseffekte (öffentliches Interesse) und der Einreichplanungen für die behördlichen Genehmigungsverfahren des ge­ planten Bergbauprojektes - insbesondere bei Umweltverträglichkeitsprüfungen - kommt der Geologie ebenfalls eine bedeutende Rolle zu. Dazu zählen Studien zur regionalen und über­ regionalen bis hin zu internationalen Verbreitung und Verfügbarkeit von mineralischen Roh­ stoffen, der Ersetzbarkeit und Güte des Rohstoffes sowie geologisch-hydrologisch-geotechni­ scher und gebirgsmechanischer Bewertungen des
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