Mineral chemistry and structural relationships of inclusions in diamond samples

Diamant ist das härteste Mineral – und dazu ein Edelstein -, das unter höchstem Druck und hohen Temperaturen in tiefen kontinentalen Regionen der Erde kristallisiert. Die Mineraleinschlüsse in Diamanten werden durch die physikalische Stabilität und chemische Beständigkeit der umgebenden – eigentlich metastabilen -Diamant-Phase geschützt. Aufgrund der koexistierenden Phasenkombination ermöglichen sie, die Mineral-Entwicklung zu studieren, während deren der Einschlüssen und die Diamanten kristallisierten. rnDie Phasenkombinationen von Diamant und Chrom-Pyrop, Chrom-Diopsid, Chromit, Olivin, Graphit und Enstatit nebeneinander (teilweise in Berührungsexistenz) mit Chrom-Pyrop Einschlüssen wurden von neunundzwanzig Diamant-Proben von sechs Standorten in Südafrika (Premier, Koffiefontein, De Beers Pool, Finsch, Venetia und Koingnaas Minen) und Udachnaya (Sibirien/Russland) identifiziert und charakterisiert. Die Mineraleinschlüsse weisen z.T. kubo-oktaedrische Form auf, die unabhängig von ihren eigenen Kristallsystemen ausgebildet werden können. Das bedeutet, dass sie syngenetische Einschlüsse sind, die durch die sehr hohe Formenergie des umgebenden Diamanten morphologisch unter Zwang stehen. Aus zweidiemnsionalen Messungen der ersten Ordnung von charakteristischen Raman-Banden lassen sich relative Restdrucke in Diamanten zwischen Diamant und Einschlussmineral gewinnen; sie haben charakteristische Werte von ca. 0,4 bis 0,9 GPa um Chrom-Pyrop-Einschlüsse, 0,6 bis 2,0 GPa um Chrom-Diopsid-Einschlüsse, 0,3 bis 1,2 GPa um Olivin-Einschlüsse, 0,2 bis 1,0 GPa um Chromit-Einschlüsse, beziehungsweise 0,5 GPa um Graphit Einschlüsse.rnDie kristallstrukturellen Beziehung von Diamanten und ihren monomineralischen Einschlüssen wurden mit Hilfe der Quantifizierung der Winkelkorrelationen zwischen der [111] Richtung von Diamanten und spezifisch ausgewählten Richtungen ihrer mineralischen Einschlüsse untersucht. Die Winkelkorrelationen zwischen Diamant [111] und Chrom-Pyrop [111] oder Chromit [111] zeigen die kleinsten Verzerrungen von 2,2 bis zu 3,4. Die Chrom-Diopsid- und Olivin-Einschlüsse zeigen die Missorientierungswerte mit Diamant [111] bis zu 10,2 und 12,9 von Chrom-Diopsid [010] beziehungsweise Olivin [100].rnDie chemische Zusammensetzung von neun herausgearbeiteten (orientiertes Anschleifen) Einschlüssen (drei Chrom-Pyrop-Einschlüsse von Koffiefontein-, Finsch- und Venetia-Mine (zwei von drei koexistieren nebeneinander mit Enstatit), ein Chromit von Udachnaya (Sibirien/Russland), drei Chrom-Diopside von Koffiefontein, Koingnaas und Udachnaya (Sibirien/Russland) und zwei Olivin Einschlüsse von De Beers Pool und Koingnaas) wurden mit Hilfe EPMA und LA-ICP-MS analysiert. Auf der Grundlage der chemischen Zusammensetzung können die Mineraleinschlüsse in Diamanten in dieser Arbeit der peridotitischen Suite zugeordnet werden.rnDie Geothermobarometrie-Untersuchungen waren aufgrund der berührenden Koexistenz von Chrom-Pyrop- und Enstatit in einzelnen Diamanten möglich. Durchschnittliche Temperaturen und Drücke der Bildung sind mit ca. 1087 (± 15) C, 5,2 (± 0,1) GPa für Diamant DHK6.2 von der Koffiefontein Mine beziehungsweise ca. 1041 (± 5) C, 5,0 (± 0,1) GPa für Diamant DHF10.2 von der Finsch Mine zu interpretieren.rn

REE and Hf distribution among mineral phases in the CV-CK clan : a way to explain present-day Hf isotopic variations in chondrites

Chondrites are among the most primitive objects in the Solar System and constitute the main building blocks of telluric planets. Among the radiochronometers currently used for dating geological events, Sm–Nd and Lu–Hf are both composed of refractory, lithophile element. They are thought to behave similarly as the parent elements (Sm and Lu) are generally less incompatible than the daughter elements (Nd and Hf) during geological processes. As such, their respective average isotopic compositions for the solar system should be well defined by the average of chondrites, called Chondritic Uniform Reservoir (CHUR). However, while the Sm–Nd isotopic system shows an actual spread of less than 4% in the average chondritic record, the Lu–Hf system shows a larger variation range of 28% [Bouvier A., Vervoort J. D. and Patchett P. J. (2008) The Lu–Hf and Sm–Nd isotopic composition of CHUR: Constraints from unequilibrated chondrites and implications for the bulk composition of terrestrial planets. Earth Planet. Sci. Lett.273, 48–57]. To better understand the contrast between Sm–Nd and Lu–Hf systems, the REE and Hf distribution among mineral phases during metamorphism of Karoonda (CK) and Vigarano-type (CV) carbonaceous chondrites has been examined. Mineral modes were determined from elemental mapping on a set of five CK chondrites (from types 3–6) and one CV3 chondrite. Trace-element patterns are obtained for the first time in all the chondrite-forming minerals of a given class (CK chondrites) as well as one CV3 sample. This study reveals that REE are distributed among both phosphates and silicates. Only 30–50% of Sm and Nd are stored in phosphates (at least in chondrites types 3–5); as such, they are not mobilized during early stages of metamorphism. The remaining fraction of Sm and Nd is distributed among the same mineral phases; these elements are therefore not decoupled during metamorphism. Of the whole-rock total of Lu, the fraction held in phosphate decreases significantly as the degree of metamorphism increases (30% for types 3 and 4, less than 5% in type 6). In contrast to Lu, Hf is mainly hosted by silicates with little contribution from phosphates throughout the CK metamorphic sequence. A significant part of Sm and Nd are stored in phosphates in types 3–5, and these elements behave similarly during CK chondrite metamorphism. That explains the robustness of the Sm/Nd ratios in chondrites through metamorphism, and the slight discrepancies observed in the present-day isotopic Nd values in chondrites. On the contrary, Lu and Hf are borne by several different minerals and consequently they are redistributed during metamorphism–induced recrystallization. The Lu/Hf ratios are therefore significantly disturbed during chondrites metamorphism, leading to the high discrepancies observed in present-day Hf isotopic values in chondrites.

Clay mineral and heavy metal composition of sea-bed surface sediments and pre-Holocene sediment samples taken during POLARSTERN cruise ANT-XXIII/9

Surface mineralogical compositions and their association to modern processes are well known from the east Atlantic and south-west Indian sectors of the Southern Ocean, but data from the interface of these areas - the Prydz Bay-Kerguelen region - is still missing. The objective of our study was to provide mineralogical data of reference samples from this region and to relate these mineralogical assemblages to hinterland geology, weathering, transport and depositional processes. Clay mineral assemblages were analysed by means of X-ray diffraction technique. Heavy mineral assemblages were determined by counting of gravity-separated grains under a polarizing microscope. Results show that by use of clay mineral assemblages four mineralogical provinces can be subdivided: i) continental shelf, ii) continental slope, iii) deep sea, iv) Kerguelen Plateau. Heavy mineral assemblages in the fine sand fraction are relatively uniform except for samples taken from the East Antarctic shelf. Our findings show that mineralogical studies on sediment cores from the study area have the potential to provide insights into past shifts in ice-supported transport and activity and provenance of different water masses (e.g. Antarctic slope current and deep western boundary current) in the Prydz Bay-Kerguelen region.

Description and chemical and mineral composition of iron oxide samples from two Finnish lakes

Fifteen iron oxide accumulations from the bottoms of two Finnish lakes ("lake ores") were found to contain as much as 50% Fe. Differential X-ray powder diffraction and selective dissolution by oxalate showed that the samples consisted of poorly crystallized goethite and ferrihydrite. The crust ores of one lake had higher ferrihydrite to goethite ratios than the nodular ores of the other lake. The higher ferrihydrite proportion was attributed to a higher rate of Fe2+ supply from the ground water and/or a higher rate of oxidation as a function of water depth and bottom-sediment permeability. Values of Al-for-Fe substitution of the goethites determined from unit-cell dimensions agreed with those obtained from chemical extraction if the unit-cell volume rather than the c dimension was used. In very small goethite crystals a slight expansion of the a unit-cell dimension is probaby compensated by a corresponding contraction of the c dimension, so that a contraction of the c dimension need not necessarily be caused by Al substitution. The goethites of the two lakes differed significantly in their Al-for-Fe substitutions and hence in their unit-cell sizes, OH-bending characteristics, dehydroxylation temperatures, dissolution kinetics, and Mössbauer parameters. The difference in Al substitution (0 vs. 7 mole %) is attributed to the Al-supplying power of the bottom sediments: the silty-clayey sediments in one lake appear to have supplied A1 during goethite formation, whereas the gravelly-sandy sediments in the other lake did not. The compositions of the goethites thus reflect their environments of formation.

(Table 1) Heavy-mineral analyses for DSDP Leg 67 Holes from electron microprobe

Heavy and light minerals were examined in 29 samples from Sites 494, 498, 499, 500, and 495 on the Deep Sea Drilling Project Leg 67 Middle America Trench transect; these sites represent lower slope, trench, and oceanic crust environments off Guatemala. All samples are Quaternary except those from Hole 494A (Pliocene) and Hole 498A (Miocene). Heavy-mineral assemblages of the Quaternary sediments are characterized by an immature pyroxene-amphibole suite with small quantities of olivine and epidote. The Miocene sediments yielded an assemblage dominated by epidote and pyroxene but lacking olivine; the absence of olivine is attributed to selective removal of the most unstable components by intrastratal solution. Light-mineral assemblages of all samples are predominantly characterized by volcanic glass and plagioclase feldspar. The feldspar compositions are compatible with andesitic source rocks and frequently exhibit oscillatory zoning. The heavy- and light-mineral associations of these sediments suggest a proximal volcanic source, most probably the Neogene highland volcanic province of Guatemala. Sand-sized components from Site 495 are mainly biogenic skeletons and volcanic glass and, in one instance (Section 495-5-3), euhedral crystals of gypsum.

Chemical and isotopic compositions of ocean authigenic carbonates

Oceanic authigenic carbonates are classified according to origin of the carbonate carbon source using a complex methodology that includes methods of sedimentary petrography, mineralogy, isotope geochemistry, and microbiology. Mg-calcite (protodolomite) and aragonite predominate among the authigenic carbonates. All authigenic carbonates are depleted in 13C and enriched in 18O (in PDB system) that indicates biological fractionation of isotopes during carbonate formation. Obtained results show that authigenic carbonate formation is a biogeochemical (microbial) process, which involves carbon from ancient sedimentary rocks, abiogenic methane, and bicarbonate-ion of hydrothermal fluids into the modern carbon cycle.