Quantitative or qualitative development in decision making?

A key question in the developmental sciences is whether developmental differences are quantitative or qualitative. For example, does age increase the speed in processing a task (quantitative differences) or does age affect the way a task is processed (qualitative differences)? Until now, findings in the domain of decision making have been based on the assumption that developmental differences are either quantitative or qualitative. In the current study, we took a different approach in which we tested whether development is best described as being quantitative or qualitative. We administered a judgment version and a choice version of a decision-making task to a developmental sample (njudgment = 109 and nchoice = 137; Mage = 12.5 years, age range = 9–18). The task, the so-called Gambling Machine Task, required decisions between two options characterized by constant gains and probabilistic losses; these characteristics were known beforehand and thus did not need to be learned from experience. Data were analyzed by comparing the fit of quantitative and qualitative latent variable models, so-called multiple indicator multiple cause (MIMIC) models. Results indicated that individual differences in both judgment and choice tasks were quantitative and pertained to individual differences in “consideration of gains,” that is, to what extent decisions were guided by gains. These differences were affected by age in the judgment version, but not in the choice version, of the task. We discuss implications for theories of decision making and discuss potential limitations and extensions. We also argue that the MIMIC approach is useful in other domains, for example, to test quantitative versus qualitative development of categorization, reasoning, math, and memory

Geology and mineralization of the Mt Carbine Tungsten Deposit, Northern Queensland, Australia

The Mt Carbine quartz-wolframite-scheelite sheeted vein deposit is located ~80 km NW of Cairns, Northern Queensland. It was the largest vein type W deposit in Australia and accounted for 43% of Australia’s annual W production in 1986, prior to closure because of international Sn-W market crash. The hard rock resources at Mt Carbine include indicated resources of 18 Mt at 0.14% WO3 and inferred resources of 29.3 Mt at 0.12% WO3 (Carbine Tungsten Limited Annual Report 2014). The vein system in Mt Carbine is hosted in Ordovician to Devonian Hodgkinson Formation metasedimentary rocks, which include turbiditic metasediments composed mainly of greywacke, siltstone-shale, slate, basalt, conglomerates and chert. There are four 30-40 m wide vein zones in the open pit with different orientations, with Zones 1 - 3 being ~300°/80° (strike/dip) with dip direction of 210°, 210° and 20°, respectively, and Zone 4 270°/65° with dip direction of 180° to 185°. Based on drill core logging and open pit observation, the paragenesis sequence has been established. Stage 0 is represented by deformed curvy and discontinuous quartz-dominant veins with minor to none W mineralization. Stage I continuous quartz-dominant veins have straight and continuous margin, and are composed of wolframite±scheelite± K-feldspar±biotite±tourmailine±apatite. Stage II veins are straight & continuous, quartz-dominant with sharp boundaries, and contain chlorite±scheelite±wolframite± cassiterite±muscovite. Stage III is represented by undeformed straight and continuous quartz±chlorite± muscovite±molybdenite±arsenopyrite±chalcopyrite±pyrite± pyrrhotite±sphalerite veins, without W mineralization. Stage IV veins are featured by the undeformed straight and continuous shape and quartz ± calcite ± fluorite mineralogy without any W mineralization. The W mineralization is mostly in stage II quartz veins, with less economic W mineralization in the other 3 stages of veins. Ore minerals are wolframite and scheelite. Wolframite is typically euhedral and occurs in quartz veins, while the occurrences of scheelite are: (1) euhedral grains in quartz vein and, (2) pseudomorphing wolframite grains or cutting across wolframite grains as veinlets. There are at least 3 felsic igneous rock types in the mining district, including porphyritic biotite granite, equigranular coarse-grained biotite granite and fine-grained felsic dykes that cuts across the ore body. There is no observable contact between granite and the W veins, thus their relationship is unclear. Mineralized quartz veins and chlorite alteration occur in the porphyritic biotite granite, whereas no quartz vein and alteration are present in the fine-grained felsic dyke, indicating that the porphyritic biotite granite was earlier than mineralization and the felsic dyke later than mineralization. This observation is consistent with the latest dating results: the LA-ICP-MS zircon U-Pb age of the porphyritic biotite granite is 298±3 Ma and the felsic dyke 261±7 Ma, whereas the molybdenite Re-Os age from the mineralized quartz vein is 28 ±1 Ma, and the muscovite 40Ar-39Ar ages are 282-277 (±1-2) Ma. There is no overlap between the 2 muscovite 40Ar-39Ar ages, probably indicates there was some post-mineralization tectono-thermal activities. Preliminary fluid inclusion studies reveal that most of them are primary, with sizes up to 26 μm. The homogenization temperatures range from 210 to 290°C, final ice-melting temperatures are between 0 and −3.7°C. Laser Raman analysis identified CH4 in the vapor bubble. The δ34S values of sulphides range from -9.1 to -6.0‰, and O-H isotopes largely overlap with metamorphic water

A Method to Determine the In-Air Spatial Spread of Clinical Electron Beams

We propose and analyze in detail a method to measure the in-air spatial spread parameter of clinical electron beams. Measurements are performed at the center of the beam and below the adjustable collimators sited in asymmetrical configuration in order to avoid the distortions due to the presence of the applicator. The main advantage of our procedure lies in the fact that the dose profiles are fitted by means of a function which includes, additionally to the Gaussian step usually considered, a background which takes care of the dose produced by different mechanisms that the Gaussian model does not account for. As a result, the spatial spread is obtained directly from the fitting procedure and the accuracy permits a good determination of the angular spread. The way the analysis is done is alternative to that followed by the usual methods based on the evaluation of the penumbra width. Besides, the spatial spread found shows the quadratic-cubic dependence with the distance to the source predicted by the Fermi-Eyges theory. However, the corresponding values obtained for the scattering power are differing from those quoted by ICRU nr. 35 by a factor ~2 or larger, what requires of a more detailed investigation.Comment: 11 pages, 5 Postscript figures, to be published in Medical Physic

Vein-type graphite deposits in Sri Lanka: the ultimate fate of granulite fluids

The world-best vein graphite deposits in Sri-Lanka occur scattered through the high-grade terrain of the Wanni and Highland Complexes of Sri-Lanka. The Wanni Complex (amphibolite to granulite grade) consists of ~770-1100 Ma metagranitoids, metagabbro, charnockite, enderbitic gneisses, migmatites, clastic metasediments, including garnet-cordierite gneisses, rare to minor calc-silicate rocks as well as late to post-tectonic granites (Kröner et al., 2013). Higher metamorphic grade, reaching in places UHT-conditions (T>1000 °C) characterizes the Highland Complex. Peak metamorphism occurred during the Neoproterozoic Pan-African orogeny (~620-535 Ma), which led to the accretion of terrains in Sri Lanka and played a key role for the amalgamation of the Gondwana supercontinent (Tsunogae and Santosh, 2010). Structurally disposed in extensional fractures post-dating the Pan-African ductile structures (Kehelpannala, 1999), the graphite veins equilibrated at relatively low temperature (500-600 °C). However, the presence of mesoperthites indicate that graphite precipitation may have started at higher temperature. Samples from khondalite host rocks and quartz co-precipitated with graphite from the Bogala and Kahatagana graphite mines in the Wanni Complex were studied. Host-rocks show spectacular decompression reaction aureoles around feldspars and garnet. They contain small CO2 inclusions in garnet cores or quartz in decompression reaction aureoles. Larger, highly transposed brine inclusions are more abundant and are responsible for metasomatic features (feldspar leaching and deposition) observed in the aureoles. Fluid inclusions in vein minerals are dominantly aqueous, rarely mixed H2O+CO2. Fluid inclusions and petrographic data suggest that graphite has been deposited from fluids at decreasing pressure and temperature at relatively reduced redox conditions. Carbon isotope data indicate a dominant mantle source, mixed with small quantities of light C-bearing fluids. It has been proposed that large quantities of mantle-derived CO2 fluid have infiltrated the lower crust during the final stage of Gondwana supercontinent amalgamation (Touret et al., 2016). Formed during strong decompression at the end of a long (up to a few 10 Ma) period of isobaric cooling, the graphite veins in Sri-Lanka (and elsewhere in the former Gondwana) reflects the escape of these granulite fluids to higher crustal levels. In this respect, they are comparable to the quartz-carbonates mega-shear zones found in other granulite terranes (Newton and Manning, 2002). Depending on the redox conditions, former lower crustal fluids (mantle-derived CO2 and/or brines) may either result in mid to upper-crustal quartz-carbonate or graphite veins

Widespread CO2-rich cordierite in the UHT Bakhuis granulite belt, Surinam

The Bakhuis Granulite Belt, approx. 30 x 100 km, transects the large Paleoproterozoic greenstone belt along the north-eastern coast of South America. Part of the Granulite belt witnessed typical Ultrahigh-Temperature Metamorphism (UHTM). A metapelite area in the NE of the belt shows assemblages characteristic of UHTM: aluminous (up to 10 wt.%) orthopyroxene + sillimanite +/- sapphirine. Leucosomes commonly show mesoperthite or K-rich antiperthite. Ternary feldspar thermometry indicates a peak temperature of 1000-1050°C and pressure is estimated to have been around 9 kbar. Metapelites elsewhere in the belt lack mineral assemblages characteristic of UHTM. However, feldspar thermometry for these metapelites as well as for mesoperthite granulites indicates that peak temperatures were 900°C or higher throughout the belt and locally reached 1000-1050°C. It is, therefore, concluded that the other parts of the belt also witnessed UHTM, despite their lack of typical UHTM assemblages. Study of peak assemblages in metapelites in these parts is hampered by varying, but usually considerable retrograde metamorphism. The main mafic mineral in metapelites is coarse Mg-rich cordierite, accompanied by coarse sillimanite. Widespread occurrence of cordierite + sillimanite in metapelites is unusual for UHTM, the more so as UHTM assemblages are commonly formed at the expense of cordierite-bearing assemblages. In a small part of the metapelites cordierite is accompanied by coarse aluminous (up to 9 wt.%) orthopyroxene. Associated cordierite and orthopyroxene appear to have formed in equilibrium with each other. Only the presence of aluminous orthopyroxene (as well as the presence of mesoperthite) is typical for UHTM, but is limited to a small part of the metapelites. Peak P-T conditions for the cordierite-bearing part of the belt are estimated to have been similar to those in the NE area with its characteristic UHTM assemblages. Primary and secondary fluid inclusions in UHT quartz blebs in orthopyroxene consist of pure CO2 and have a high density. Raman spectroscopy indicated a considerable CO2 content in cordierite. Estimated from their birefringence, the CO2 content of most cordierites is in the range of 1-2 wt.% CO2. This corresponds to a substantial filling of the cordierite channels with CO2 and for the higher levels possibly near-saturation with CO2 according to the model of Harley and Thompson for the maximum level of CO2 in cordierite. Thermodynamic data for CO2-rich cordierite are poorly known. However, a high level of CO2 in cordierite has been considered to lead to a substantial expansion of its stability field, also into the field of UHTM, at T > 900°C. This is, therefore, assumed to be the explanation for the unusual, widespread occurrence of cordierite in the UHTM belt. A small part of the metapelite samples shows cordierite of a high birefringence, twice that of quartz. SIMS analysis of such cordierite showed 3.0 wt.% CO2, the highest level known from nature. The level is far too high to have formed at UHTM conditions according to the model of Harley and Thompson and would be possible only at conditions such as 700°C and 10 kbar. It is assumed that locally the CO2 level of cordierite changed after UHTM, by taking up additional CO2. Secondary fluid CO2 inclusions in UHT quartz have a higher density than the primary inclusions, indicating a near-isobaric cooling path down to 700-750°C. In these conditions cordierite probably could steadily re-equilibrate at decreasing temperature while taking up more and more CO2, up to 3 wt.% around 700°C. The heat source for the UHTM in the Bakhuis Granulite belt is considered to be asthenospheric upwelling or mafic underplating, but mafic magmatism of identical age to the UHTM has not yet been found. One mafic intrusion was found to be around 20 Ma older than the UHTM, whereas in the SW of the belt numerous mafic intrusions formed around 70 Ma after UHTM

THEORETICAL REACTION CROSS SECTIONS FOR ALPHA PARTICLES WITH AN OPTICAL MODEL

The transmission coefficients T/sub l/ and total reaction cross sections sigma /sub R/ for alpha particles from 0 to 46 Mev interacting with twenty target nuclei with atomic numbers from 10 to 92 are calculated with optical model program in which a previously determined complex nuclear potential is utilized. The dependence of the T/sub l/ values, and hence of sigma /sub R/, on the Woods- Saxon parameters is investigated as a function of projectile energy. The optical model reaction cross sections are compared with those derived from a square-well potential and a model which approximates the real optical model potential barrier by a parabola and makes use of the Hill-Wheeler penetration formula for a parahelic potential. (auth

High-temperature granulites and supercontinents

The formation of continents involves a combination of magmatic and metamorphic processes. These processes become indistinguishable at the crust-mantle interface, where the pressure-temperature (P-T) conditions of (ultra) high-temperature granulites and magmatic rocks are similar. Continents grow laterally, bymagmatic activity above oceanic subduction zones (high-pressure metamorphic setting), and vertically by accumulation of mantle-derived magmas at the base of the crust (high-temperature metamorphic setting). Both events are separated from each other in time; the vertical accretion postdating lateral growth by several tens of millions of years. Fluid inclusion data indicate that during the high-temperature metamorphic episode the granulite lower crust is invaded by large amounts of low H2O-activity fluids including high-density CO₂ and concentrated saline solutions (brines). These fluids are expelled from the lower crust to higher crustal levels at the end of the high-grade metamorphic event. The final amalgamation of supercontinents corresponds to episodes of ultra-high temperature metamorphism involving large-scale accumulation of these low-water activity fluids in the lower crust. This accumulation causes tectonic instability, which together with the heat input from the subcontinental lithospheric mantle, leads to the disruption of supercontinents. Thus, the fragmentation of a supercontinent is already programmed at the time of its amalgamation.J.L.R. Touret, M. Santosh, J.M. Huizeng