ࡱ> SUR'` 0>bjbj$$ 4JFF#,<B#2HHHHHHH"""""""$,$h&"E#HH##"HH" #>HH" #"  H& 3,!Ia  !#0B# Z'w RZ' ZZ'-!`H  |6HHH"" HHHB#####d zD z" Mineralogical Society Distinguished Lecture Programme 2010-11 The Mineralogical Society is pleased to offer four lectures for the 2010-2011 academic year, to be given by Dr Richard Harrison (Cambridge University) and Dr Jeff Harris (University of Glasgow). Lectures offered by R. Harrison Lecture A: Mineral magnetism at the nanometre scale: or why size really does matter after all Magnetic minerals are ubiquitous in the natural environment, and they are also present in a wide range of biological organisms, from bacteria to human beings. These minerals carry a wealth of information encoded in their magnetic properties that can be used to address an ever increasing range of geoscience problems, from the origins of the early solar system to quantifying variations in Earths paleoclimate. The last ten years have seen a striking improvement in our ability to detect and image the magnetization of minerals in geological and biological samples at the nanometre scale. Arguably the most significant recent advance in mineral magnetism is the application of off-axis electron holography, a transmission electron microscopy (TEM) technique that yields a two-dimensional map of magnetization vectors with nanometer spatial resolution. In this talk I will outline the principle of electron holography and demonstrate how this technique is revolutionising our understanding of magnetism at the nanometre scale. Lecture B: Microstructures and mineral behaviour: from the nanometer to the planetary scale One of the key goals (and one of the greatest achievements) of mineral physics has been the application of sophisticated experimental and theoretical methods to understand the relationship between the crystal structure of a mineral and its macroscopic properties and behaviour. Increasingly, however, it is becoming evident that microstructures can play a crucial role in determining the macroscopic behaviour of minerals, and that our experimental and theoretical understanding of microstructure-property relations lags far behind our understanding of the atomic scale. In this talk I will demonstrate how the presence of nanoscale microstructures can play a dominant role in determining the properties of minerals and how they might impact processes at the planetary scale, from the origin of low-frequency seismic attenuation in perovskite to the origin of magnetic anomalies in the crust of Mars. Lectures offered by J. Harris Lecture A: Smashing diamonds reveals their origins Systematic studies on the mineral impurities contained within diamond and on diamond itself, have provided major insights into the conditions within the mantle under which this mineral formed. Diamond occurs principally in two distinct environments called peridotitic and eclogitic and form over the depth range of 150 to about 700km, a zone which covers the whole of the upper and part of the lower mantle. Diamonds from >200km are relatively rare, the majority for both environments, forming in the subcratonic lithospheric mantle at about 5.0 - 5.5GPa (50-55kbar) and 1160 100C. Within some of the mineral inclusions the analysis of radiogenic isotopes (Nd-Sm, Re-Os, Ar-Ar) indicates that the oldest isochron genesis age for peridotitic diamonds is 3520170Ma, (Panda diamonds, Canada) with other determinations centred about 2000Ma (Premier and Venetia diamonds, South Africa). For eclogitic diamonds genesis ages are more distinctly episodic ranging from 2900Ma (Kimberley diamonds, South Africa), through 158060Ma (Argyle diamonds, Australia) to 99050Ma (Orapa diamonds, Botswana). Trace element analyses, particularly of garnet inclusions, show that diamond formation is associated with the above rocks after they have undergone melt or fluid metasomatism. Over 95% of the diamonds from the peridotitic paragenesis have carbon isotopes (13C) within the range  9 to  1 0 . For eclogitic diamonds there is a much broader 13C distribution ranging from  38.5 to +2.90 . Both parageneses have dominant modes at  5 0 , a value regarded as mantle derived. The isotopic patterns for peridotitic and eclogitic diamonds, especially when combined with the nitrogen content of diamond, can be modelled in terms of precipitation from closed system Rayleigh fractionations involving carbonate-bearing melts or fluids. Mineral equations such as enstatite + magnesite = olivine + cpx + diamond apply for peridotitic whilst dolomite + coesite = cpx + diamond would be eclogitic. In addition, open system fractionation involving CO2 appears to be important for eclogitic diamonds to account for the extended tail of the eclogitic data. In addition to these genesis reactions, the oxidation of a reduced species such as methane (CH4 + O2 = C + 2H2O) has recently been shown to be an important reaction for some peridotitic diamonds. Although the present subcratonic lithospheric mantle is considered too reduced for this reaction to occur, if the genesis age of these diamonds (1900Ma) is considered, then these diamonds formed as a result of an ancient reaction which became less important through time, because of the common subduction of biogenic carbonates which made the mantle more oxidised. Lecture B: Fingerprinting diamonds Diamond classification schemes using such physical properties as shape, colour and surface features, help define diamond populations. Such schemes are not only useful in their own right, providing information about the trials and tribulations of diamond travelling from the upper mantle, but also can assist in diamond prospecting, particularly in linking alluvial diamonds to a primary source. The humble carbon tetrahedron is the building block that enables diamond to create a multitude of primary shapes, some of which then undergo resorption. Diamond growth is usually episodic and patterns may be either straightforward (related to the external diamond shape), or be more complex, the patterns indicating that the final shape will be a consequence of more than one growth form. In other cases there appears to be no clear growth sequence at all. The scale of any classification depends on the number and size of the diamonds available. Examination of large quantities of diamonds from known kimberlite/lamproite mines or alluvial sources, allows the classification of shape and colour to be determined as a function of size. Up to twelve shapes are used and resulting graphs are often distinct. Within southern Africa, for example, cube diamonds are prominent in the mines of Botswana, there are few if any octahedral diamonds in the production from the Letsing-la-terae mine in Lesotho and at the Swartruggens fissure mine in South Africa the so-called macle (the spinel twin of the octahedron) is unusually absent. Diamond colour arises either through incorporation of atomic impurities during growth or through external influences acting on the diamond after growth. Nitrogen is the commonest atomic impurity and specific configurations make diamond either orange/amber or yellow. Small quantities of atomic boron make diamond blue. Body-green diamonds are rare, but a common variety at some mines is a green transparent coat. In both instances the cause is linked to radiation damage inflicted subsequent to formation. Brown in a diamond population is closely associated with plastic deformation, an event which occurs most likely during diamond residence in the Earths upper mantle. Although eleven colours may be noted, classification shows that colourless, yellow, and brown predominate at most mines. Transparent green coated diamonds are found only in the upper oxidised parts of kimberlite pipes. In alluvial deposits green and/or brown spotted diamonds are often a feature, a form of radiation damage which allows an estimate to be made as to how long the diamond has been resident in that environment. Surface features classifications divide into those restricted by a particular shape and those where the surface feature is unrestricted. Surface features are most diverse on resorbed diamonds where growth patterns can be exposed or on those from alluvial deposits where features due to alluvial transport are superimposed on those created in the kimberlite or lamproite. If you would like to bid for one of these lectures, please complete the form overleaf and return it by Monday 20th September 2010 to  HYPERLINK "mailto:Martin.Lee@ges.gla.ac.uk" Martin.Lee@ges.gla.ac.uk Application for Mineralogical Society Distinguished Lecturer 2010-11 Organisation: Department: Name local seminar organizer: E-mail address local seminar organizer: Indicate your preferred lecture: LectureIndicate oneR. Harrison89<=>?mq{ "  cdƹƹƬƬƹ|re|reh#h#CJ^JaJh#h#5CJh#h#5CJ^JaJh#h#5>*CJ^JaJh#h#CJh#h5CJh#h#CJmH sH h#h5CJmH sH h#hiCJmH sH h#hq$CJmH sH h lh#5CJ\mH sH h lhq$5CJ\mH sH !>? 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HarrisSmashing diamonds reveals their originsFingerprinting diamonds Please state a desired date for the lecture, or your usual seminar slot (e.g. Lunchtime on Wednesday 13th January 2011 or Any Thursday evening in November 2010). Please return to Martin.Lee@ges.gla.ac.uk by Monday 20th September 2010 <<<<<<7Zkd$$IfTl0H t644 layt%T $$Ifa$gd5Zkd$$IfTl0H t644 layt%T$If<<<<<<<:Zkd$$IfTl0H t644 layt%TZkd@$$IfTl0H t644 layt%T$If $Ifgd%<<<<<=============gd#Zkd$$IfTl0H t644 layt%T$IfD=K=X=b=d=f=r=s=w==================>>񹬟{m{cht~CJmH sH h#h5CJH*mH sH h#CJmH sH h#h%CJmH sH h#hK6CJmH sH h#h5CJmH sH h#h)?CJmH sH h#h)DCJmH sH h#CJaJmH sH h#h5CJH*aJmH sH h#h5CJaJmH sH h#hiCJaJmH sH =============>$a$gdt~ 21h:pq$. 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