ALBERT

Notes: [Auszug] One possibility is that the new phase is NC8A3, described by Brownmiller and Bogue1, or KC8A3, described by Suzukawa2, or more likely, since the two compounds are isomorphous, a solid solution (^ JC8A3; but for the available alumina to be combined as this compound rather than C3A, nearly all the ...

Notes: [Auszug] ALTHOUGH leukaemias and lymphosarcomata of IJL fowls and rodents can often be transferred easily by noculating cells into the same species, cellular transfer of the disease in domesticated animals has proved difficult. Rosenberger1 has reported producing leucosis in cattle by inoculation of blood, ...

Notes: Abstract Olivine melilitites from Namaqualand, South Africa are characterized by a broad range in olivine compositions on the scale of individual hand specimens. It is possible to distinguish four petrographically and chemically distinct olivine populations in both the northern and southern pipe clusters studied: (a) Scarce anhedral or subhedral olivines that display marked disequilibrium features with the surrounding matrix, and which are characterized by having high iron and extremely low nickel contents (referred to as HILN olivines) relative to the other olivines in the same rock, (b) A dominant population of euhedral and often skeletal (hopper) olivines that are richer in Mg and Ni than the HILN olivines in the same rock. There are in addition ‘unusual’ hopper olivines that are petrographically similar to the skeletal olivines, but show aberrant zonation patterns. Hopper and HILN type olivines contain fluid and carbonate inclusions which apparently record the loss of a vapour phase and an immiscible carbonate liquid during magma ascent, (c) A third population consists of large rounded olivines (megacrysts), up to 40 mm in greatest diameter. Individuals are chemically homogeneous, but megacrysts from the same pipe collectively define a trend of decreasing Mg and Ni (Fo92, 0.36% Ni to Fo75, 0.17% Ni). The most fayalitic megacrysts are depleted in Mg and Ni relative to the hopper olivines in the same rock, (d) Scarce magnesium-rich (Fo91) anhedral olivines which show strained extinction are believed to be xenocrysts. It is suggested that the HILN-type olivines crystallized from primitive carbonate-rich magmas under conditions of low oxygen fugacity, intermediate between the Ni-NiO and Fe-FeO buffers. Mineral-melt partition coefficients for the transition elements determined in basaltic systems are considered to be inappropriate to such carbonate-rich melts. Loss of volatiles and an immiscible carbonate liquid during magma ascent resulted in an increase in oxygen activity, a decrease in the Fe-Mg distribution coefficient (K D ) for olivine and liquid and an increase in liquidus temperatures. These effects led to the rapid crystallization of Mg- and Ni-enriched skeletal hopper olivines. The ‘unusual’ hoppers crystallized later than the HILN olivines but prior to the ‘normal’ hoppers, under conditions chracterized by rapid and independent changes in oxygen activity and partition coefficients associated with the loss of volatiles and an immiscible carbonate liquid. The range in chemistry which characterizes the megacryst-olivine suite is believed to record physico-chemical changes to the magmas subsequent to separation from a mantle source area, but prior to crystallization of the HILN olivines. Most important of these changes was an increasing degree of polymerization of the liquid structure and a progressive decrease in oxygen activity as the molar ratio (CO 3 2- /(CO 3 2- + CO2)) in the magma increased with decreasing pressure. Increasing polymerization of the liquid resulted in an increase in olivine-liquid partition coefficients for transition elements. Olivines in kimberlites show compositional characteristics and zonation patterns similar to those recognized in the olivine melilitites which, coupled with ilmenite compositions, suggests that the two magma types initially evolved along similar physico-chemical paths.

Notes: Abstract Petrographic and chemical criteria indicate that the overwhelming majority of olivines in kimberlites are probably cognate phenocrysts. The implied low volume of xenocryst olivines requires that primitive kimberlite magmas are highly ultrabasic liquids. Two chemically distinctive olivine populations are present in all of the kimberlites studied. The dominant olivine population, which includes large rounded olivines and smaller euhedral crystals, is Mg-rich relative to late-stage rim compositions. It is characterized by a range in 100 Mg/(Mg + Fe) and uniform Ni concentration, reflecting Rayleigh-type crystallization during magma evolution. The most Mg-rich of these olivines are considered to be similiar to those in the mantle source rocks. The second compositional population, generally very subordinate, though markedly more abundant in the megacrystrich Monastery kimberlite, is Fe-rich relative to rim compositions. This group of olivines crystallized from evolved liquids in equilibrium with iron-rich megacrysts, both entrained by the kimberlite magma during ascent. Differences between the chemical fields of Fe-rich olivines in Group I and Group II kimberlites point to relatively deeper derivation of the latter suite. Olivine chemistry can be used to characterize kimberlite magma sub-types, and may prove to be a useful tool for evaluating the diamond potential of kimberlites.

Notes: Abstract Ilmenite macrocrysts in olivine melilitites from Namaqualand-Bushmanland, South Africa, have decomposed by subsolidus reduction to form oriented Mg-titanomagnetite along {0001} ilmenite planes. Residual ilmenite contains 10–11 wt% MgO, ∼1 wt% MnO, and ∼0.1 wt% Cr2O3. This macrocryst assemblage is mantled by an annulus of Mg-titanomagnetite, followed by an overgrowth of radiating magnetite + perovskite. Terminal compositions of these magnetites are similar to groundmass spinels, and to the outermost margins of magnetite macrocrysts that have very high Fe3+ core contents. The assemblages are remarkably similar to oxide intergrowths in kimberlites and an upper mantle derivation is proposed for ilmenite macrocrysts in these melilitites. Oxidation states in the source regions are also very similar, whether on-or off-craton, being slightly above FMQ (∼NNO), but reduced to FMQWM with the onset of decompression, volatile loss, and carbonate immiscibility. In the case of the melilitites, late stage, low pressure crystallization above NNO precipated abundant magnetite + perovskite. The oxide fO2 data are consistent with, and refine the fO2 estimates obtained previously for the behavior of Fe/Mg and Ni contents in olivine from the same suite of samples.

Notes: Abstract Mineralogical and chemical relationships indicate that the majority of ilmenites recovered from Group I kimberlites crystallized directly from the kimberlite magma in two contrasting P-T regimes: Ilmenites of the discrete nodule association formed in pegmatitic veins and apophyses surrounding the kimberlite magma at depth. Compositional ranges of the discrete nodule assemblage reflect essentially isobaric crystallization across the thermal aureole about the magma reservoir. Early crystallization of high pressure Cr-rich phases (garnet, clinopyroxene and possibly spinel) could result in later forming megacryst ilmenites being Cr-poor. During ascent of the kimberlite magma (essentially identical to the liquid injected into the pegmatitic veins), crystallization of garnet and clinopyroxene would be inhibited as a result of the expansion of the olivine phase field. The magma would not undergo Crdepletion, with the result that later crystallizing (ground-mass) ilmenites would be Cr-rich relative to associated ilmenite megacrysts. Rare ilmenite inclusions in diamonds show chemical affinities with those of the discrete nodule suite. It is proposed that large Type IIa diamonds may be late-crystallizing members of the discrete nodule assemblage. They are in other words related to the kimberlite event itself, and would represent a third diamond paragenesis, distinctly younger than those related to peridotites and eclogites. The mode of formation of rare MARID suite and metasomatized mantle xenoliths is not clearly understood, although mineralogical and chemical evidence point to a direct or indirect link to the host kimberlite.

Notes: Summary A high level of activity of a β-1,3-glucan hydrolase is present in leaves of Nicotiana glutinosa and the enzyme is also present in the roots, midribs, petioles and stems. By comparison, very low levels of β-1,4-glucan hydrolase are found throughout the plant. The activity of the β-1,3-glucan hydrolase in leaves aged on the plant was found to increase 14-fold during the course of leaf senescence and to reach a maximum in yellow-green leaves. Detached leaves and leaf discs floated on water in the dark showed similar patterns of change. The increase in β-1,3-glucan hydrolase activity during senescence is apparently not due to the loss of an inhibitor from young green leaves or to the formation of an enzyme activator in yellow leaves. The enzyme in yellow leaves was electrophoretically indistinguishable from that in green leaves. The hydrolase is not firmly attached to the cell walls and is not present in the particulate fraction sedimenting at 105400xg for 60 min. Within the leaf cell it is therefore likely to be located either in the cytoplasm or in an easily disrupted structure such as a vacuole. The relationship of the hydrolase to leaf senescence was investigated by examining the effect of plant hormones on the changes in level of hydrolase, protein and chlorophyll in leaf discs during senescence. IAA (10 μM) and GA3 (50 μM) did not alter the normal patterns of change, whilst Kin (50 μM) delayed the loss of protein and chlorophyll and also delayed and decreased the rise in hydrolase activity. In contrast, ABA (190 μM) which increased the rate of loss of protein and chlorophyll, also caused a decrease in the rate and extent of the rise in hydrolase. Possible functions of the hydrolase in the leaf are discussed.