https://ogma.newcastle.edu.au/vital/access/ /manager/Index en-au 5 https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:765 Wed 11 Apr 2018 11:33:21 AEST ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:8024 Sat 24 Mar 2018 08:36:49 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1902 Sat 24 Mar 2018 08:33:09 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1256 Sat 24 Mar 2018 08:32:48 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1317 Sat 24 Mar 2018 08:32:33 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:885 Sat 24 Mar 2018 08:31:32 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:2515 Sat 24 Mar 2018 08:31:00 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:2241 Sat 24 Mar 2018 08:29:04 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1406 Ni(II)>Zn(II)>Mn(III)>Cu(II), with Mn(II) undergoing oxidation by H₂O₂ under the reaction conditions. The order likely corresponds to a combination of the catalytic abilities of the transition metal-substituted lacunary anions in conjunction with their rates of decomposition by H₂O₂, and/or the catalytic abilities of the freed transition metals and peroxo-products themselves]]> Sat 24 Mar 2018 08:28:16 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1500 Sat 24 Mar 2018 08:28:14 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1499 Sat 24 Mar 2018 08:28:13 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:2480 Sat 24 Mar 2018 08:27:44 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:2499 Sat 24 Mar 2018 08:27:42 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:1701 0 °C at a time when MIS 6 ice volumes were close to their maximum. High stable carbon isotope (δ¹³C) values (−2.8‰ to +3.1‰) throughout the stalagmite's growth reflect a persistently low input of biogenic CO², indicating that the steep, barren and alpine-like recharge area of today has been in existence for at least the last ∼380 kyr. During MIS 9, the lowest δ¹³C values occur well after maximum interglacial conditions, suggesting a lag in the development of post-glacial soils in this high-altitude karst. The stable oxygen isotope (δ¹⁸O) trends match the main structural features of the major climate proxy records (SPECMAP, Vostok and Devils Hole), suggesting that the δ¹⁸O of CC1 has responded to global-scale climate changes, whilst remarkable similarity exists between CC1 δ¹⁸O and regional sea-surface temperature reconstructions from North Atlantic core ODP980 and southwest Pacific marine core MD97-2120 through the most detailed part of the CC1 record, MIS 9–8. The results suggest that CC1 and other stalagmites from the cave have the potential to capture a long record of regional temperature trends, particularly in regards to the relative severity of Pleistocene glacial stages.]]> Sat 24 Mar 2018 08:27:20 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:2295 Sat 24 Mar 2018 08:26:57 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:19913 w=5–72 kg mol⁻¹). Transmission electron microscopy (TEM) and scanning electron microscopy (SEM) have been used to support the STXM data. We find that unannealed P3HT:PCBM nanoparticles (NPs) exhibit a common core–shell morphology, with a PCBM-rich core and P3HT-rich shell. The morphology of the thermally annealed NP films is highly dependent upon the molecular weight of the P3HT and is determined by PCBM diffusion through the P3HT matrix. Two PCBM diffusion mechanisms operate within this system: (1) at high molecular weights diffusion of molecular PCBM dominates whilst, (2) at low molecular weights diffusion of the PCBM cores is significant. The Stokes–Einstein continuum model for diffusion has been used to determine a threshold molecular weight at which the diffusion of PCBM cores is activated in these films. The calculated value (M_w~38–25 kg mol⁻¹) is shown to agree very well with experimental observations. Finally, a model for the morphological evolution of annealed P3HT:PCBM NP films is developed.]]> Sat 24 Mar 2018 08:03:45 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3323 Sat 24 Mar 2018 07:23:19 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3320 Sat 24 Mar 2018 07:23:18 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3228 Sat 24 Mar 2018 07:22:15 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3220 Sat 24 Mar 2018 07:22:13 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3403 Sat 24 Mar 2018 07:21:41 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3401 Sat 24 Mar 2018 07:21:41 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3418 Sat 24 Mar 2018 07:21:38 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3404 400 Ma. A transverse (Rheic–Tethyian) subduction system splits the Pangaean cell. Poloidal plate motion in the oceanic cell reflects circumferential pull of Panthalassan slabs, but toroidal flow in the Pangaean cell, reflected by vortex-type motion of continents toward the Altaids of central-east Asia throughout the Phanerozoic, has resulted from the competing slab-pull forces of both cells. The combined slab-pull effects from both cells also controlled Pangaean assembly and dispersal. Assembly occurred during Palaeozoic clockwise toroidal motion in the Pangaean cell, when Gondwana was pulled into Pangaea by the NE-trending Rheic subduction zone, forming the Appalachian–Variscide–Altaid chain. Pangaean dispersal occurred when the Rheic trench re-aligned in the Jurassic to form the NW-trending Tethyside subduction system, which pulled east Gondwanan fragments in the opposite direction to form the Cimmerian–Himalayan–Alpine chain. This re-alignment also generated a new set of (Indian) mid-ocean ridge systems which dissected east Gondwana and facilitated breakup. 100–200-Myr-long Phanerozoic Wilson cycles reflect rifting and northerly migration of Gondwanan fragments across the Pangaean cell into the Rheic–Tethyian trench. Pangaean dispersal was amplified by retreat of the Panthalassan slab away from Europe and Africa, which generated mantle counterflow currents capable of pulling the Americas westward to create the Atlantic Ocean. Thermal blanketing beneath Pangaea and related hotspot activity were part of a complex feedback mechanism that established the breakup pattern, but slab retreat is considered to have been the main driving force. The size and longevity of the two cells, organised and maintained by long-lived slab-pull forces, favours deep mantle convection as the dominant circulation process during the Phanerozoic.]]> Sat 24 Mar 2018 07:21:36 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3256 Sat 24 Mar 2018 07:21:21 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3253 Sat 24 Mar 2018 07:21:20 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3257 Sat 24 Mar 2018 07:21:20 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3475 Sat 24 Mar 2018 07:20:27 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3381 Sat 24 Mar 2018 07:19:00 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3379 Sat 24 Mar 2018 07:18:59 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3393 Sat 24 Mar 2018 07:18:58 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3385 Sat 24 Mar 2018 07:18:58 AEDT ]]> https://ogma.newcastle.edu.au/vital/access/ /manager/Repository/uon:3386 Sat 24 Mar 2018 07:18:57 AEDT ]]>