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The purpose of this article is to explore how social forces related to the corporatization of universities play out at the granular level of institutional mission and vision statements in the racialized context of Canadian Kinesiology. The stated aims of Canadian Kinesiology academic units (N = 36) were collected from their public-facing websites, and we conducted a critical discourses analysis of our evidence. We argue that mission and vision statements construct Kinesiology as an altruistic and impactful scholarly project and conceal the contested nature of health, scientific knowledge, and community engagement in the field. Careful analysis of the data, with particular attention paid to that which is unspoken, silenced or erased, highlights how these guiding declarations can renew the field's underlying racial and colonial logics. To conclude, we note instances when programs use institutional statements to unsettle dominant scripts and open possibilities to work toward a more progressive and just Kinesiology.

Dr. Cabri has a number of criticisms of Djon and Barnes (2012). Some of the criticisms are valid and are the result of what we consider to be minor errors and omissions that can occur when an M.Sc. is converted to a paper. However, none of these change our conclusions, and we stand by our interpretations. [ABSTRACT FROM AUTHOR]

The Lac des Iles Complex hosts Pd deposits with unusually high Pd/Pt and Pd/Ir ratios. These high ratios have been attributed to the introduction of Pd by late magmatic-hydrothermal fluids. The presence of hydrous silicates and low-temperature sulfide mineral assemblages has been advanced as evidence for fluid overprint. This idea has been investigated by documenting the change in silicate, sulfide, and platinum-group mineralogy and texture in samples from the deposit ranging from fresh gabbronorite to extensively altered chlorite-actinolite schist. In addition, whole-rock analysis combined with laser ablation analysis of the sulfides was used to determine which phase controlled each of the PGE. In fresh gabbronorite the sulfide assemblage is igneous (pyrrhotite-pentlandite-chalcopyrite) and Pd is present mainly in pentlandite and kotulskite (PdTe) inclusions associated with the sulfide minerals. All other PGE (except Pt) are present in solid solution in pyrrhotite and pentlandite. Platinum is present as sperrylite (PtAs) and montcheite (PtTe) inclusions associated with the sulfide minerals. These observations suggest that the PGE in the fresh gabbronorite were all collected by magmatic sulfide liquid. In the chlorite-actinolite schist the sulfide assemblage is a low-temperature assemblage consisting of chalcopyrite, pyrite ± millerite. A minor amount of palladium is present in millerite, but most is present as bismuth-rich kotulskite and Pd arsenides both of which are associated with hydrous silicate. All other PGE (except Pt) are hosted by pyrite. A minor amount of Pt is present in pyrite, but most is found as sperrylite and montcheite associated with hydrous silicate minerals. The pyrite could have formed by Fe-loss from pyrrhotite (resulting in the pyrite inheriting Os, Ir, Ru, and Rh) and Fe-loss from pentlandite to form millerite (resulting in the millerite inheriting some Pd). The PGE concentrations of the whole rock show there is no direct correlation between the sulfide assemblage, the degree of alteration of the silicate minerals and ore grade. Thus, although fluids have clearly altered the sulfide-, silicate-, and platinum-group mineralogy and their textures, it is not clear that these fluids have changed the PGE content of the rocks. [ABSTRACT FROM AUTHOR]

Abstract: Laser ablation ICP-MS analysis has been applied to many accessory minerals in order to understand better the process by which the rock formed and for provenance discrimination. We have determined trace element concentrations of Fe-oxides in massive sulfides that form Ni–Cu–PGE deposits at the base of the Sudbury Igneous Complex in Canada. The samples represent the crystallization products of fractionating sulfide liquids and consist of early-forming Fe-rich monosulfide solution (MSS) cumulates and residual Cu-rich intermediate solid solution (ISS). This study shows that Fe-oxide geochemistry is a sensitive petrogenetic indicator for the degree of fractionation of the sulfide liquid and provides an insight into the partitioning of elements between sulfide and Fe-oxide phases. In addition, it is useful in determining the provenance of detrital Fe-oxide. In a sulfide melt, all lithophile elements (Cr, Ti, V, Al, Mn, Sc, Nb, Ga, Ge, Ta, Hf, W and Zr) are compatible into Fe-oxide. The concentrations of these elements are highest in the early-forming Fe-oxide (titanomagnetite) which crystallized with Fe-rich MSS. Upon the continual crystallization of Fe-oxide from the sulfide liquid, the lithophile elements gradually decrease so that late-forming Fe-oxide (magnetite), which crystallized from the residual Cu-rich liquid, is depleted in these elements. This behavior is in contrast with Fe-oxides that crystallized from a fractionating silicate melt, whereby the concentration of incompatible elements, such as Ti, increases rather than decreases. The behavior of the chalcophile elements in magnetite is largely controlled by the crystallization of the sulfide minerals with only Ni, Co, Zn, Mo, Sn and Pb present above detection limit in magnetite. Nickel, Mo and Co are compatible in Fe-rich MSS and thus the co-crystallizing Fe-oxide is depleted in these elements. In contrast, magnetite that crystallized later from the fractionated liquid with Cu-rich ISS is enriched in Ni, Mo and Co because Fe-rich MSS is absent. The concentrations of Sn and Pb, which are incompatible with Fe-rich MSS, are highest in magnetite that formed from the fractionated Cu-rich liquid. At subsolidus temperatures, ilmenite exsolved from titanomagnetite whereas Al-spinel exsolved from the cores of some magnetite, locally redistributing the trace elements. However, during laser ablation ICP-MS analysis of these Fe-oxides both the magnetite and its exsolution products are ablated so that the analysis represents the original magmatic composition of the Fe-oxide that crystallized from the sulfide melt. [Copyright &y& Elsevier]

brereton l., gardiner c., gott m., ingleton c., barnes s. & carroll c. (2011) The hospital environment for end of life care of older adults and their families: an integrative review. Journal of Advanced Nursing 68(5), 981-993. Abstract Aim. This article is a report of an integrative review to identify key elements of the physical hospital environment for end of life care of older adults and their families as reported by patients, relatives, staff and policy makers. Background. Globally ageing populations and increases in long-term illness mean that more people will need palliative care in the future. Despite policy initiatives to increase end of life care in the community, many older adults prefer, and will require, end of life care in hospital. Providing an appropriate physical environment for older adults requiring end of life care is important given concerns about hospital environments for this group. Data sources. Thirteen databases from 1966 to 2010 were searched including ASSIA, BNI, Cochrane Library, CINAHL, EMBASE, MEDLINE, PsycINFO, Social Science Citation Index, the Science Citation Index, HMIC and the National Research Register. Reference and citation tracking was performed on included publications. Review methods. An integrative review was conducted. Two reviewers independently screened titles and abstracts for inclusion and completed data extraction. Study quality is not reported as this poses methodological difficulties in integrative reviews. Data synthesis involved thematic analysis informed by the findings of included literature. Results. Ten articles were included. Four themes were identified: privacy as needed; proximity (physically and emotionally) to loved ones, home and nature; satisfaction with the physical environment; and deficiencies in physical environment. Conclusion. Little evidence exists about physical hospital environments for end of life care of older adults and their families. More research is required in this field. [ABSTRACT FROM AUTHOR]

Magmatic sulfide deposits consist of pyrrhotite, pentlandite, chalcopyrite (± pyrite), and platinum-group minerals (PGM). Understanding the distribution of the chalcophile and platinum-group element (PGE) concentrations among the base metal sulfide phases and PGM is important both for the petrogenetic models of the ores and for the efficient extraction of the PGE. Typically, pyrrhotite and pentlandite host much of the PGE, except Pt which forms Pt minerals. Chalcopyrite does not host PGE and the role of pyrite has not been closely investigated. The Ni-Cu-PGE ores from the South Range of Sudbury are unusual in that sulfarsenide PGM, rather than pyrrhotite and pentlandite, are the main carrier of PGE, probably as the result of arsenic contribution to the sulfide liquid by the As-bearing metasedimentary footwall rocks. In comparison, the North Range deposits of Sudbury, such as the McCreedy East deposit, have As-poor granites in the footwall, and the ores commonly contain pyrite. Our results show that in the pyrrhotite-rich ores of the McCreedy East deposit Os, Ir, Ru, Rh (IPGE), and Re are concentrated in pyrrhotite, pentlandite, and surprisingly in pyrite. This indicates that sulfarsenides, which are not present in the ores, were not important in concentrating PGE in the North Range of Sudbury. Palladium is present in pentlandite and, together with Pt, form PGM such as (PtPd)(TeBi). Platinum is also found in pyrite. Two generations of pyrite are present. One pyrite is primary and locally exsolved from monosulfide solid solution (MSS) in small amounts (<2 wt.%) together with pyrrhotite and pentlandite. This pyrite is unexpectedly enriched in IPGE, As (± Pt) and the concentrations of these elements are oscillatory zoned. The other pyrite is secondary and formed by alteration of the MSS cumulates by late magmatic/hydrothermal fluids. This pyrite is unzoned and has inherited the low concentrations of IPGE and Re from the pyrrhotite and pentlandite that it has replaced. [ABSTRACT FROM AUTHOR]

Concentrations of platinum group elements (PGE), Ag, As, Au, Bi, Cd, Co, Mo, Pb, Re, Sb, Se, Sn, Te, and Zn, have been determined in base metal sulfide (BMS) minerals from the western branch (402 Trough orebodies) of the Creighton Ni-Cu-PGE sulfide deposit, Sudbury, Canada. The sulfide assemblage is dominated by pyrrhotite, with minor pentlandite, chalcopyrite, and pyrite, and they represent monosulfide solid solution (MSS) cumulates. The aim of this study was to establish the distribution of the PGE among the BMS and platinum group minerals (PGM) in order to understand better the petrogenesis of the deposit. Mass balance calculations show that the BMS host all of the Co and Se, a significant proportion (40-90%) of Os, Pd, Ru, Cd, Sn, and Zn, but very little (<35%) of the Ag, Au, Bi, Ir, Mo, Pb, Pt, Rh, Re, Sb, and Te. Osmium and Ru are concentrated in equal proportions in pyrrhotite, pentlandite, and pyrite. Cobalt and Pd (∼1 ppm) are concentrated in pentlandite. Silver, Cd, Sn, Zn, and in rare cases Au and Te, are concentrated in chalcopyrite. Selenium is present in equal proportions in all three BMS. Iridium, Rh, and Pt are present in euhedrally zoned PGE sulfarsenides, which comprise irarsite (IrAsS), hollingworthite (RhAsS), PGE-Ni-rich cobaltite (CoAsS), and subordinate sperrylite (PtAs), all of which are hosted predominantly in pyrrhotite and pentlandite. Silver, Au, Bi, Mo, Pb, Re, Sb, and Te are found predominantly in discrete accessory minerals such as electrum (Au-Ag alloy), hessite (AgTe), michenerite (PdBiTe), and rhenium sulfides. The enrichment of Os, Ru, Ni, and Co in pyrrhotite, pentlandite, and pyrite and Ag, Au, Cd, Sn, Te, and Zn in chalcopyrite can be explained by fractional crystallization of MSS from a sulfide liquid followed by exsolution of the sulfides. The early crystallization of the PGE sulfarsenides from the sulfide melt depleted the MSS in Ir and Rh. The bulk of Pd in pentlandite cannot be explained by sulfide fractionation alone because Pd should have partitioned into the residual Cu-rich liquid and be in chalcopyrite or in PGM around chalcopyrite. The variation of Pd among different pentlandite textures provides evidence that Pd diffuses into pentlandite during its exsolution from MSS. The source of Pd was from the small quantity of Pd that partitioned originally into the MSS and a larger quantity of Pd in the nearby Cu-rich portion (intermediate solid solution and/or Pd-bearing PGM). The source of Pd became depleted during the diffusion process, thus later-forming pentlandite (rims of coarse-granular, veinlets, and exsolution flames) contains less Pd than early-forming pentlandite (cores of coarse-granular). [ABSTRACT FROM AUTHOR]

Platinum-group elements (PGE) are typically hosted in base metal sulfides and by platinum-group minerals (PGM) in Ni-Cu-PGE sulfide deposits. At Sudbury, it appears that the majority of PGE are hosted in PGM. In order to understand why this is the case we have investigated the origin of PGM from the 402 trough orebodies of the Creighton deposit located on the South Range of Sudbury. These predominantly pyrrhotite-rich sulfides, with low (Pt + Pd)/(Os + Ir + Ru + Rh) whole-rock ratios, represent cumulates of monosulfide solid solution (MSS) that crystallized early from the sulfide melt, collected in troughs and embayments at the base of the Sudbury Igneous Complex, and formed small pendants of ore in the footwall country rock. The majority of PGE (Ir, Rh, Pt ± Os, Ru) show a stronger affinity for the sulfarsenide phases than the cocrystallizing sulfide phases which are strongly depleted in these PGE. The precious metal mineralogy is dominated by PGE sulfarsenides (86%) with subordinate sperrylite (PtAs2: 9%), michenerite (PdBiTe: 5%), and electrum (AgAg2: 0.1%). These discrete minerals are predominantly hosted within pyrrhotite and pentlandite except, however, a large proportion of michenerite is hosted either entirely by silicates and/or juxtaposed against silicates. The PGE sulfarsenides are euhedrally zoned with an irarsite (IrAsS) core, an outer layer of hollingworthite (RhAsS), and a PGE-rich Ni cobaltite rim (CoAsS). Rhenium sulfides, some of which are Os bearing, are documented for the first time at Sudbury. Platinum-group minerals may crystallize directly from sulfide melt, form by exsolution during cooling of die base metal sulfides or recrystallize from them during metamorphism. We propose that zoned PGE sulfarsenides and sperrylite crystallized from a sulfide melt at high temperatures (1,200°-900°C) and were subsequently surrounded by MSS cumulates, even by disseminated sulfides, that crystallized from the now It, Rh, Pt ± Os, Ru-depleted immiscible sulfide liquid. The base metal sulfides recrystallized with secondary hydrosilicates at a late magmatic and/or hydrothermal stage (<540°(2) at which time michenerite formed. The magmatic zoning of the PGE sulfarsenides was preserved during later deformation in shear zones but these PGM were corroded, fractured, and juxtaposed against silicates. [ABSTRACT FROM AUTHOR]