This article is about the geological feature in Zimbabwe. For the manmade Gaojia Weir, sometimes also known as the Great Dyke, see Hongze Lake.
Left - The Great Dyke can be seen as linear feature, running from north-east to south-west in this satellite view of Zimbabwe. Right - The southern end of the dyke is captured in this astronaut photograph.
The Great DykeorDike is a linear geological feature that trends nearly north-south through the centre of Zimbabwe passing just to the west of the capital, Harare. It consists of a band of short, narrow ridges and hills spanning for approximately 550 kilometres (340 mi). The hills become taller as the range goes north, and reach up to 460 metres (1,510 ft) above the Mvurwi Range. The range is host to vast ore deposits, including gold, silver, chromium, platinum, nickel and asbestos.[1]
Wedza Subchamber of the Great Dyke. Mimosa Platinum Mine is located near the heavily wooded section in the centre. The Umvimeela Dyke is visible to the far left of the scene.
Geologically the Great Dyke is not a dyke, but is lopolithic[2] and Y-shaped in cross-section. It is a group of layered ultramafic intrusions that extend across Zimbabwe with a strike of about N20°E. The width of the intrusions vary from 3 to 12 km (7.5 mi). The Great Dyke is unusual in that most ultramafic layered intrusions display near horizontal sill or sheet forms.
The well-layered lower units of ultramafic rocks comprising the Great Dyke are locally overlain by erosional remnants of gabbroic rock. These mark the centres of the four sub-chambers within the Great Dyke magma system, namely (from north to south) Musengezi, Darwendale, Sebakwe and Wedza. Each of these sub-chambers has an elongate, doubly plunging synclinal structure, and was fed by a feeder dyke continuous below almost the entire Great Dyke.[3]Stratigraphically each sub-chamber is divided into a lower Ultramafic Sequence of dunites, harzburgites, olivinebronzitites and pyroxenites together with narrow layers of chromitite that constitute the bases of cyclic units and that are extensively mined along the Great Dyke, and an upper Mafic Sequence mainly consisting of a variety of plagioclase-rich rocks, such as norites, gabbronorites and olivine gabbros.[4]
The dyke lies within the Zimbabwe Craton and has been dated at 2.575 billion years old.[5] The Great Dyke acts as a strain-marker for the craton: The fact that it has been undeformed since intrusion (excluding the Musengezi area) shows that the craton had stabilised by the time the Dyke intruded.[6]
Two mafic dykes, the East and Umvimeela, flank the Great Dyke to the east and west respectively.[7][8]Volcanic surface manifestation of the Great Dyke event has not been recorded and have probably been eroded.[3]
Soils on the Great Dyke are strongly influenced by the underlying bedrock. Shallow, infertile Lithosols over ultramafic rock dominate the northern and southern ends. Best for agriculture are those reddish brown granular clays developed over mafic rock in the central area. Ultramafic rock in the central area supports a complex association of moderately deep to deep dark self-churning clay, and moderately deep reddish brown kaolin-rich clay.[9]
The Great Dyke is a strategic economic resource with significant quantities of chrome and platinum. Chromite occurs to the base of the Ultramafic Sequence and is mined throughout the dyke.[4] Below the Ultramafic-Mafic sequences' contact, and in the uppermost pyroxenite (bronzitite and websterite) units are economic concentrations of nickel, copper, cobalt, gold, and platinum group metals (PGM). The base metals occur as disseminated inter-cumulus Fe-Ni-Cu sulfides within an interval referred to as the base metal subzone, below which is a sublayer enriched in platinum group metals called the PGE subzone. The base metal and PGE subzones together, make up the Main Sulphide Zone (MSZ).[10]
The Great Dyke was first reported in 1867 by the explorer Karl Mauch. However the existence of platinum was not realized until 1918, and mining of oxidized ores did not start until in 1924.[11]
^Guilbert, J.M., and Park, C.F.Jr. 1986 The Geology of Ore Deposits, Freeman, ISBN0-7167-1456-6
^Hughes, Charles James (1970) Lateral Cryptic Variation in the Great Dyke of Rhodesia, Geological Magazine, Volume 107, Issue 4, pages 319-325 [1]. Retrieved 2013-12-01.
^ abWilson, A.H. and Prendergast, M.D., 1989. The Great Dyke of Zimbabwe-I: tectonic setting, stratigraphy, petrology, structure, emplacement and crystallisation. In: Prendergast, M.D., Jones, M.J. (Eds.), Magmatic sulphides-the Zimbabwe volume. Institution Mining Metallurgy, London, 1–20. ISBN978-1-870706-06-3
^ abPrendergast, M.D. and Wilson, A.H. 1989. The Great Dyke of Zimbabwe-II: Mineralisation and mineral deposits. In: Prendergast, M.D., Jones, M.J. (Eds.), Magmatic sulphides-the Zimbabwe volume. Institution Mining Metallurgy, London, 21-42. ISBN978-1-870706-06-3
^Oberthuer, T., Davis, D.W., Blenkinsop, T.G., Hoehndorf, A., 2002. Precise U–Pb mineral ages, Rb–Sr and Sm–Nd systematics for the Great Dyke, Zimbabwe—constraints on crustal evolution and metallogenesis of the Zimbabwe Craton. Precambrian Research, 113, 293–306.[2]
^Dirks, P.H.G.M. and Jesma, H.A. 2002. Crust–mantle decoupling and the growth of the Archaean Zimbabwe craton. Journal of African Earth Sciences, 34, 157–166 [3]
^Stribrny, B., Wellmer, F.-W., Burgath, K.-P., Oberthür, T., Tarkian, M. and Pfeiffer, T. 2000. Unconventional PGE occurrences and PGE mineralization in the Great Dyke: metallogenic and economic aspects. Mineralium Deposita, 35, 260-281. [4]
^Why existing investors are unenthusiastic about Zimbabwe sanctionsZimbabwe Review
^Locmelis, M., Melcher, F.,
Oberthür, T. 2010. Platinum-group element distribution in the oxidized Main Sulfide Zone, Great Dyke, Zimbabwe.Mineralium Deposita, 45, 93-109. [5]
^Oberthür, T., Melcher, F., Buchholz, P., Locmelis, M. 2012. The oxidized ores of the Main Sulfide Zone, Great Dyke, Zimbabwe: Turning resources into minable reserves – mineralogy is the key.In: Platinum 2012, The Southern African Institute of Mining and Metallurgy (SAIMM), Symposium Series, S72, 647-672. [6]
