Journal articles on the topic 'Secondary recrystallisation'

The idea that a single subgrain is sufficient to produce a single recrystallised grain is the simplest explanation for the recrystallisation process. Likewise, a single Goss oriented grain arising from the primary recrystallisation process is the simplest unit which can give rise to a secondary Goss oriented grain. More complicated cluster models, for example subgrain coalescence is also considered feasible for primary recrystallisation, clusters of Goss oriented grains might be another mechanism for forming Goss oriented secondary grains. This paper examines the cluster theory using material which is produced by the ARMCO process which requires two stages of rolling. In order to achieve this aim it is necessary to destroy the connectivity between individual Goss oriented grains by using thin foils derived from sheet which gives a strong Goss texture on conventional annealing. The foils were sectioned from the subsurface which had a strong η fibre after primary recrystallisation, and ranged in thickness from 18μm (the average grain size after primary recrystallisation) up to 80μm, which is the approximate thickness of the η textured layer. The central layer, which had the classical {111}<hkl> primary recrystallised texture, was similarly processed, but this did not produce secondary recrystallisation. The experiment followed the secondary recrystallisation process in the same area using sequential annealing in a vacuum furnace by a combination of EBSD and Channelling contrast microscopy. The data does not support the high energy boundary hypothesis nor the CSL explanation. But it is clear that connectivity is important, because when this is destroyed by the thin foil two dimensional morphology, as it is in the thinnest foil, secondary recrystallisation does not occur.

In this study, we investigated the recrystallisation kinetics of Ti-stabilised interstitial-free (IF) steel manufactured by the Mexican steel industry through the route of electric arc furnace with vacuum degassing, secondary refining, and subsequent continuous casting. The IF steel was hot-rolled at 950°C and then cold-rolled until deformation of 94% was attained, followed by recrystallisation at different times at a constant temperature of 780°C. In addition, the mechanical properties of the IF steel were assessed as a function of recrystallisation time. The results obtained from the mechanical property tests were presented in the form of plots of microhardness, yield strength, ultimate tensile stress, and deformation percent as functions of the recrystallised fraction with an indirect dependence on recrystallisation time. A graphical model of the recrystallisation behaviour showed the evolution of the microstructure, including phase transformations, hardness, and the mechanical properties determined from the tensile tests. In view of subsequent recovery and recrystallisation, stored energy analysis derived from the strain induced by deformation was presented. Furthermore, we determined the precipitates formed in the different processing stages of IF steel.

Orientation microscopy in TEM and SEM is a particularly well suited tool to study recrystallisation processes because these are always associated with orientation and microstructure changes. The present work discusses the possibilities and limits of the TEM and SEM based techniques and illustrates their use by means of 3 different examples. The examples include studies on nucleation mechanisms of primary recrystallisation where the techniques meet their limits in spatial resolution. The problem of in-situ observations of annealing processes is discussed and it is shown how recrystallisation simulation techniques based on experimental data may be used. Furthermore the new technique of 3-dimensional EBSD in a focused-ion-beam (FIB) SEM is presented with one example. Finally, the statistical analysis of very large orientation data sets is discussed by an example of secondary recrystallisation in electrical steels.

Primary recrystallised sheets of 3% silicon steel from two different industrial processing routes have been examined after laboratory annealing to initiate secondary recrystallisation. Metallography included etching to reveal individual dislocations and sub-boundaries as well as EBSD in scanning electron microscopy. Residual low angle boundaries are not normally observed inside the secondary grains. The growth of secondaries appears to occur in a jerky manner, associated with local intrusions into the primary matrix that destabilise the interface. The frequency of occurrence of special low energy grain boundaries such as 9 and 5 is believed to dictate the selectivity of the Goss orientation in both types of steel sheet.

Heat treatment has a significant impact on the microstructure and the mechanical properties of Al-Mg-Si alloys. The present study presents a first Phase-Field modelling approach on the recrystallisation and grain growth mechanism during annealing. It focuses on the precipitate fraction, radius, and Mg-Si concentration in the matrix phase, which are used as input data for the calculation of the yield strength and hardness at the end of different ageing treatments. Annealing and artificial ageing simulations have been conducted on the MultiPhase-Field based MICRESS@ software, while the ThermoCalc@ software has been used to construct the pseudo-binary Al-Mg phase-diagrams and the atomic-mobility databases of MgxSiy precipitates. Recrystallisation simulation estimates the recrystallisation kinetics, the grain growth, and the interface mobility with the presence/absence of secondary particles, selecting as annealing temperature 400 °C and a microstructure previously subjected to cold rolling. The pinning force of secondary particles decelerates the overall recrystallisation time, causing a slight decrease in the final grain radius due to the reduction of interface mobility. The ageing simulation examines different ageing temperatures (180 and 200 °C) for two distinct ternary systems (Al-0.9Mg-0.6Si/Al-1.0Mg-1.1Si wt.%) considering the interface energy and the chemical free energy as the driving force for precipitation. The combination of Phase-Field and the Deschamps–Brechet model predicted the under-ageing condition for the 180 °C ageing treatment and the peak-ageing condition for the 200 °C ageing treatment.

The present work is an attempt to understand the recrystallisation mechanisms in Fe-3% Si alloys used in transformer cores. After secondary recrystallisation silicon steels exhibit a Goss texture with a more or less important spread depending on the details of the processing route, namely, Conventional Grain Orientation CGO or High Permeability Hi-B. The mechanisms of Goss grain formation during hot rolling and primary recrystallisation, as well as those controlling the first steps of abnormal growth, are not yet well understood. The present work mainly deals with texture characterization of the hot rolled state. Surface, quarter and half thickness samples are prepared from hot-rolled sheet. Global and local textures are characterized by neutron diffraction and electron backscattered diffraction, respectively. The Orientation Distribution Functions and the volume fraction of the different texture components are calculated. The components from global texture measurements are (001)[1-10], (112)[1-10] (α fiber ), (011)[100] (Goss) and (111)[1-21] (111) [1-10](γ fiber). EBSD measurements have shown large variations of texture from the surface to the half thickness of the sheet. These local measurements are related to the global results by rotation about the transverse direction. Moreover, the grain size appears to be inhomogeneous.

The formation of the Goss texture in electrical steels is one of the most distinct phenomena of texture research. Nevertheless, disregarding 60 years of research the mechanisms which let only Goss-oriented grains grow abnormally during a secondary recrystallisation annealing are still not completely understood. The present paper reviews some of the mechanisms of growth selection and oriented nucleation and discusses them in the light of observations made by the authors. We conclude that no mechanism proposed so far is able to explain all experimental observations. This points out the need for the search for a different mechanism.

Island grains have been studied in iron samples that had been treated by critical-strainannealing and in commercial silicon iron alloy sheets after incomplete secondary recrystallisation. Such islands remain behind because their boundaries have such a low mobility that the grains cannot shrink away in the time available during annealing. Misorientations of these islands in relation to the grains surrounding them were measured using EBSD. Similar results were observed in both materials. A small number of low angle boundaries were found and also many twin boundaries. The most remarkable observation, however, was the presence of many general high angle boundaries that did not correspond to any evident coincidence relation.

The dynamic strain-induced transformation (DSIT) of ferrite from austenite in intense deformation at temperatures close to Ar3 were applied to one C-Mn steel and several Nb and Nb-Ti microalloy steels to obtain an ultrafine ferrite grain size. As another route the static recrystallisation of severely cold-rolled martensite (SRM) was utilized. It was found that in the DSIT route a fine prior austenite grain size was crucial to form ferrite with the grain size of 1-3 µm with a considerable fraction of a secondary phase, carbide aggregate/pearlite or martensite. Grain sizes achieved were somewhat finer in steels with a higher microalloying content. In the SRM route, the ferrite grain size of 1-1.5 µm was obtained by using the cold rolling of 80-90% reduction. Thermal stability of the ultrafine-grained structures, especially those from the DSIT route, was found to be excellent. In electron or laser beam welding of 1-2.5 mm sheets neither any coarse-grained zone existed in the heat-affected zone, nor did form any softened zone.

With the rising importance of aluminum sheets for automotive applications, the influence of microstructure and texture on mechanical properties and on forming behavior has gained re-increased interest in recent years. This paper provides an introduction to the topic and demonstrates the evolution of microstructure and texture in the standard alloys EN AW-5182 and EN AW-6016 for different processing scales. Moreover, strategies for texture and microstructure characterization of automotive Al-sheets are discussed. As the development of alloys or processes usually starts in laboratory facilities, the transferability to the industrial scale of the results thereof is studied. A detailed analysis of the entire processing chain shows good conformity of careful laboratory production with the industrial production concerning microstructure as well as qualitative and quantitative texture evolution for EN AW-5182. While comparable grain sizes can be achieved in final annealed sheets of EN AW-6016, quantitative discrepancies in texture occur between the different production scales for some sample states. The results are discussed in light of the basics of plasticity and recrystallisation including the effect of solutes, primary phases, and secondary phases in the alloys.

The microstructure evolution and softening processes occurring in 22Cr-19Ni-3Mo austenitic and 21Cr-10Ni-3Mo duplex stainless steels deformed in torsion at 900 and 1200 °C were studied in the present work. Austenite was observed to soften in both steels via dynamic recovery (DRV) and dynamic recrystallisation (DRX) for the low and high deformation temperatures, respectively. At 900 °C, an “organised”, self-screening austenite deformation substructure largely comprising microbands, locally accompanied by micro-shear bands, was formed. By contrast, a “random”, accommodating austenite deformation substructure composed of equiaxed subgrains formed at 1200 °C. In the single-phase steel, DRX of austenite largely occurred through strain-induced grain boundary migration accompanied by (multiple) twinning. In the duplex steel, this softening mechanism was complemented by the formation of DRX grains through subgrain growth in the austenite/ferrite interface regions and by large-scale subgrain coalescence. At 900 °C, the duplex steel displayed limited stress-assisted phase transformations between austenite and ferrite, characterised by the dissolution of the primary austenite, formation of Widmanstätten secondary austenite and gradual globularisation of the transformed regions with strain. The softening process within ferrite was classified as “extended DRV”, characterised by a continuous increase in misorientations across the sub-boundaries with strain, for both deformation temperatures.

Severe plastic deformation (SPD) has led to the discovery of ever stronger materials, either by bulk modification or by surface deformation under sliding contact. These processes increase the strength of an alloy through the transformation of the deformation substructure into submicrometric grains or twins. Here, surface SPD was induced by plastic deformation under frictional contact with a spherical tool in a hot rolled CuAlBe-shape memory alloy. This created a microstructure consisting of a few course martensite variants and ultrafine intersecting bands of secondary martensite and/or austenite, increasing the nanohardness of hot-rolled material from 2.6 to 10.3 GPa. In as-cast material the increase was from 2.4 to 5 GPa. The friction coefficient and surface damage were significantly higher in the hot rolled condition. Metallographic evidence showed that hot rolling was not followed by recrystallisation. This means that a remaining dislocation substructure can lock the martensite and impedes back-transformation to austenite. In the as-cast material, a very fine but softer austenite microstructure was found. The observed difference in properties provides an opportunity to fine-tune the process either for optimal wear resistance or for maximum surface hardness. The modified hot-rolled material possesses the highest hardness obtained to date in nanostructured non-ferrous alloys.

The 56 ka Monte Epomeo Green Tuff (MEGT) resulted from the largest volume explosive eruption from Ischia island (south Italy). Its tephra is one of the main stratigraphic markers of the central Mediterranean area. Despite its importance, a detailed characterisation of the petrography and mineral chemistry of MEGT is lacking. To fill this gap, we present detailed petrographic description and electron microprobe mineral chemistry data on samples collected on-land from the MEGT. Juvenile clasts include pumice, scoria, and obsidian fragments with porphyritic/glomeroporphyritic, vitrophyric, and fragmental textures. The porphyritic index is 13–40 vol.%, and phenocryst phases include alkali-feldspar, plagioclase, clinopyroxene, ferrian phlogopite, and titano-magnetite, in order of decreasing abundance; accessory phases include sphene, hydroxy-fluor-apatite, and rare edenite. Plagioclase varies from predominant andesine to subordinate oligoclase, whereas alkali-feldspar is more variable from sanidine to anorthoclase; quasi-pure sanidine commonly occurs as either rim or recrystallisation overgrowth of large phenocrysts due to hydrothermal alteration. Secondary minerals include veins and patches of carbonate minerals, Fe-Mn oxyhydroxides, clay minerals, and zeolites. Clinopyroxene is ferroan diopside (En45–29Fs7–27) and never reaches Na-rich compositions. This feature allows the discrimination of MEGT from aegirine-bearing, distal tephra layers erroneously attributed to MEGT, with implications for the areal distribution of Ischia explosive deposits.

Our laboratory developed and tested experimental and calculation techniques for quantitative texture analysis based on the ODF combined with the diffraction of thermal neutrons. In our work the texture of the Fe-3%Si sheets was investigated after different stages of their processing, i.e. hot-rolled strips, first cold rolling, first inter-annealing, second cold rolling, second annealing and secondary recrystallisation. The texture experiments were carried out on the KSN-2 diffractometer which is equipped with the TG-1 texture goniometer with automatic data collection for transmission and reflection geometry. TODFND (the cubic symmetry of the crystals and orthorhombic symmetry of the specimen) was used and the ODF values were obtained together with all texture characteristics (pole figures, inverse pole figures, ODF - f (g) values, fibre texture with <110> and <001> axis parallel to rolling direction, parameters of the ideal orientations (HKL)<uvw>, texture index J, volume fraction coefficient f. The comparison of the texture parameters of the six samples with the different technologic history is given and the magnetic anisotropy of all measured samples was determined by means of the quantitative texture analysis (ODF-the matrix Cl nµ) for all samples. Results achieved in our study confirm that the quantitative texture analysis in connection with neutron diffraction can help to improve the technology of the preparation of oriented magnetic steel sheets.

The aim of the present work was to undertake a detailed investigation of the softening mechanisms during hot deformation of a 21Cr-10Ni-3Mo (steel A) and a 21Cr-8Ni-3Mo (steel B) austenite/ferrite duplex stainless steels containing about 60% and 30% of austenite, respectively. The steels were subjected to hot deformation in torsion performed at 900 °C and 1200 °C using a strain rate of 0.7 s-1 to several strain levels. Quantitative optical and transmission electron microscopy were used in the investigation. Austenite was observed to soften via dynamic recovery (DRV) and dynamic recrystallisation (DRX) accompanied by DRV for the deformation temperatures of 900 °C and 1200 °C, respectively, for the both steels studied. DRX of austenite largely occurred through strain-induced grain boundary migration, complemented by (multiple) twinning, and developed significantly faster in steel A than in steel B, indicating that considerably larger strains partitioned into austenite in the former steel during deformation at 1200 °C. The above softening mechanism was accompanied by the formation of DRX grains from subgrains along the austenite/ferrite interface and by large-scale subgrain coalescence. At 900°C, stressassisted phase transitions between austenite and ferrite were observed, characterised by dissolution of the primary austenite, formation of Widmanstätten secondary austenite and gradual globularisation of the microstructure with increasing strain. These processes appeared to be significantly more widespread in steel B. The softening mechanism within ferrite for the both steels studied was classified as “continuous DRX”, characterised by a gradual increase in misorientations between neighbouring subgrains with strain, for the both deformation temperatures.

Abstract Introduction and geodynamic setting. – Syn-rift exhumation of mantle rocks in a continental breakup zone was highlighted along the present-day west Iberian passive margin [e.g. Boillot et al., 1988, 1995; Whitmarsh et al., 1995, 2001; Beslier et al., 1996; Brun and Beslier, 1996; Boillot and Coulon, 1998; Krawczyk et al., 1996; Girardeau et al., 1998] and along the fossil Tethyan margins [e.g. Froitzheim and Manatschal, 1996; Manatschal and Bernoulli, 1996; Marroni et al., 1998; Müntener et al., 2000; Desmurs et al., 2001]. Along the west Iberian margin, serpentinized peridotite and scarce gabbro and basalt lay directly under the sediments, over a 30 to 130 km-wide transition between the thinned continental crust and the first oceanic crust [Girardeau et al., 1988, 1998; Kornprobst and Tabit, 1988; Boillot et al., 1989; Beslier et al., 1990, 1996; Cornen et al., 1999]. The formation of a wide ocean-continent transition (OCT), mostly controlled by tectonics and associated with an exhumation of deep lithospheric levels, would be an essential stage of continental breakup and a characteristic of magma-poor passive margins. The southwest Australian margin provides an opportunity to test and to generalize the models proposed for the west Iberian margin, as both margins present many analogies. The south Australian margin formed during the Gondwana breakup in the Mesozoic, along a NW-SE oblique extension direction [Willcox and Stagg, 1990]. From north to south, the continental slope is bounded by (1) a magnetic quiet zone (MQZ) where the nature of the basement is ambiguous [Talwani et al., 1979; Tikku and Cande, 1999; Sayers et al., 2001], (2) a zone where the basement shows a rough topography associated with poorly expressed magnetic anomalies [Cande and Mutter, 1982; Veevers et al., 1990; Tikku and Cande, 1999; Sayers et al., 2001], and which is the eastward prolongation of the Diamantina Zone, and (3) an Eocene oceanic domain. The continental breakup zone is believed to be located near or at the southern edge of the MQZ [Cande and Mutter, 1982; Veevers et al., 1990; Sayers et al., 2001]. Breakup is dated at 125 Ma [Stagg and Willcox, 1992], 95 ± 5 Ma [Veevers, 1986] or at 83 Ma [Sayers et al., 2001], and followed by ultra-slow seafloor spreading until the Eocene (43 Ma), and fast spreading afterwards [Weissel and Hayes, 1972; Cande and Mutter, 1982; Veevers et al., 1990; Tikku and Cande, 1999]. The western end of the margin (fig. 1) is starved and bounded in the OCT by basement ridges where peridotite, gabbro and basalt were previously dredged [Nicholls et al., 1981]. Altimetry data [Sandwell and Smith, 1997] show that some of these ridges are continuous over 1500 km along the OCT of the south Australian margin and of the conjugate Antarctic margin. The objectives of the MARGAU/MD110 cruise (May-June 1998; [Royer et al., 1998]; fig. 2) were to define the morpho-structure and the nature and evolution of the basement in the SW Australian OCT. An area of 180 000 km2 was explored with swath bathymetry. Gravimetric data (11382 km) were simultaneously recorded whereas few single channel seismic (1353 km) and magnetic (5387 km) data were obtained due to technical difficulties. Crystalline basement rocks, made of varied and locally well-preserved lithologies, were dredged at 11 sites located on structural highs. Main results. – The bathymetric map unveils three E-W domains (fig. 2). From north to south, they are the continental slope of Australia, prolonged westward by that of the Naturaliste Plateau, a 160 km-wide intermediate flat sedimented area corresponding to the MQZ, and a 100 km-wide zone of rough E-W oriented topography which continues the Diamantina Zone (fig. 3). The first two domains are cut through in three segments by two major fracture zones (FZ), the Leeuwin FZ along the eastern side of the Naturaliste Plateau, and the Naturaliste FZ along its western flank. These NW-SE trending FZ terminate north of the E-W trending fabric of the Diamantina Zone. Accordingly, extension occurred along the NW-SE direction during the formation of the slope and of the MQZ, and then turned to N-S during the formation of the Diamantina Zone. In the Diamantina Zone, the mantle rocks dredged at Site MG-DR02 are mainly lherzolites, rich in pyroxenitic micro-layers, and pyroxenites. They contain spinel rimmed by plagioclase and locally coronas of olivine + plagioclase between opx and spinel, which suggest that they underwent some subsolidus reequilibration in the plagioclase field (fig. 4C). Westward (Site DR09), the mantle rocks are harzburgitic, with lesser pyroxenitic bandings and no plagioclase. The rocks have coarse-grained porphyroclastic textures that are locally overprinted by narrow mylonitic shear bands, and then by a cataclastic deformation, which indicate decreasing temperatures and increasing stresses during their evolution. Basalts were sampled at Sites MG-DR01, −04, −05, and together with gabbros at Sites MG-DR02, -03, -09. They have a transitional composition as shown by their REE patterns, except one sample from site MG-DR-05 which is an alkaline basalt (fig. 5). The gabbros are clearly intrusive in the peridotite at Sites DR02 and -09. They contain olivine and clinopyroxene (cpx) at Site DR02, cpx, plagioclase and hornblende at Site DR03, and cpx and amphibole or orthopyroxene or olivine at Site DR09 (fig. 4D). At that site, a tonalite containing K-feldspar and biotite and alkaline in composition (fig. 5), has also been sampled. All these plutonic rocks display either their primary magmatic textures or secondary porphyroclastic ones that are locally overprinted by mylonitic shear zones (fig. 4E). Retrograde minerals of amphibolite to greenschist facies developed during the deformation. The basalts are clearly intrusive in the gabbros at Site DR03. They are altered and exhibit porphyric textures with abundant plagioclase and plagioclase + olivine phenocrysts at Sites DR03, -04, -08, -10, and have a transitional composition (fig. 5). The nature and evolution of the peridotites and associated gabbros are compatible with an exhumation under a rift zone, on both sides of the Leeuwin FZ. It includes a mylonitic deformation which attests that these rocks underwent a shearing deformation under lithospheric conditions, in probable relation with their exhumation during the early stages of the oceanic opening. The crustal rocks are represented only by intrusive gabbros and by transitional basalts. In the MQZ, the peridotites recovered at Site MG-DR06 are mainly spinel and plagioclase lherzolites (fig. 4B) and a few pyroxenites (fig. 4A) with high temperature porphyroclastic textures. Their discovery indicates that the basement in the MQZ is not exclusively formed of thinned continental crust. Lavas sampled westward of the Leeuwin FZ at Site DR10 have also transitional compositions (fig. 5). On the Australian slope, samples dredged at Site MG-DR07 are continental quartz-bearing rocks (mostly gneisses and rare granites), some showing a high grade paragenesis (upper amphibolite to granulite facies) marked by the presence of K-feldspar, biotite, sillimanite and/or kyanite and garnet, and without primary muscovite (fig. 4G). Some of these rocks underwent an intense mylonitic shear deformation followed by post-tectonic recrystallisation or migmatization. Depending on the age of the high grade evolution (metamorphism and shearing), these rocks document either the syn-rift exhumation of lower continental crust, or the formation of the older Australian craton. On the slope of the Naturaliste Plateau, at Site DR11, rocks of oceanic origin (gabbro-diorites/dolerite/basalt; fig. 4F) were dredged together with acid rocks (gneiss and granites) of probable continental origin, some having a quartz, K-feldspar, biotite and garnet metamorphic paragenesis (fig. 4H). At that site, the transitional basalts intrude the gabbros and associated dolerites. The presence of metamorphic acid rocks indicate that the Naturaliste Plateau is likely a continental fragment that was later intruded by mafic rocks, whose origin and ages of intrusion have to be determined. Discussion and conclusions. – The retrograde tectono-metamorphic evolution of the peridotites recovered in the MQZ, which includes a reequilibration in the plagioclase field (marked by the development of olivine and plagioclase after spinel and pyroxene), is compatible with an exhumation under a rift zone [Girardeau et al., 1988; Kornprobst and Tabit, 1988; Cornen et al., 1999]. By analogy with the Iberia Abyssal Plain, the MQZ could represent a wide OCT where the mantle was exhumed and stretched mostly by amagmatic extension before the initiation of oceanic accretion [Beslier et al., 1996; Boillot and Coulon, 1998] (fig. 6). This hypothesis is supported by the tectonic structures (horsts and grabens) imaged in the seismic data over the MQZ [Boeuf and Doust, 1975]. Accordingly, the limit of the continental crust would be located at the foot of the slope, i.e. 160 km (or 250 km in the NW-SE extension direction) northward of the assumed location of the OCT at the southern edge of the MQZ. The age of the Australia-Antarctic breakup would thus be (1) older than that inferred from the magnetic anomalies (circa 95 Ma [Cande and Mutter, 1982; Veevers, 1986]), which would rather date the onset of oceanic accretion, and (2) older than the age of the breakup unconformity estimated as Santonian (83 Ma), further east, in the Great Australian Bight [Sayers et al., 2001]. The origin of the Naturaliste Plateau, continental or oceanic, is still disputed. The discovery of metamorphic rocks of probable continental origin on the southern flank of the Plateau (Site DR11) shows that it consists at least partially of rocks of the Gondwana continent. All the samples from the Diamantina Zone confirm that its basement is made of a peridotite-gabbro-basalt assemblage. The nature and age of the peridotites and of the associated magmas will help understanding the origin of this domain, which can result either from Neocomian seafloor spreading with further remobilization during the Australia-Antarctic separation, or from post-Neocomian ultra-slow seafloor spreading. Because of the omnipresence of extensive tectonic structures (fig. 3) and of the relatively small proportion of crustal rocks relative to the mantle rocks, we argue that the formation of the Diamantina Zone was mainly controlled by tectonics rather than by magmatic processes. In conclusion, the data collected along the southwest Australian margin during the MARGAU/MD110 survey evidence two major tectonic phases with formation of a wide OCT where abundant mantle rocks, in association with few mafic rocks, outcrop or lay directly beneath the sediments. The evolution of the crystalline rocks is compatible with an exhumation under a rift zone during a phase of magma-poor extension primarily controlled by tectonic processes. The domains where basement highs were sampled seem to be continuous over more than 1500 km eastward along the south Australian margin. Additional evidence on such large-scale structural continuity and on the nature of the associated basement highs may help generalizing the models for continental breakup and formation of non-volcanic passive margins, where oceanic accretion does not immediately follow continental breakup.

Abstract Reconstructed whole-rock and mineral major- and trace-element compositions, as well as new oxygen isotope data, for 22 mantle eclogite xenoliths from the Catoca pipe (Kasai Craton) were used to constrain their genesis and evolution. On the basis of mineralogical and major-element compositions, the Catoca eclogites can be divided into three groups: high-alumina (high-Al) (kyanite-bearing), low-magnesian (low-Mg#), and high-magnesian (high-Mg#) eclogites. The high-Al Catoca eclogites contain kyanite and corundum; high Al2O3 contents in rock-forming minerals; rare earth element (REE) patterns in garnets showing depleted LREEs, positive Eu anomalies (1.03–1.66), and near-flat HREEs; and high Sr contents in garnets and whole-rock REE compositions. All of these features point to a plagioclase-rich protolith (probably gabbro). Reconstructed whole-rock compositions (major elements, MREEs, HREEs, Li, V, Hf, Y, Zr, and Pb) and δ18O of 5.5–7.4‰ of the low-Mg# Catoca eclogites are in good agreement with the compositions of picrite basalts and average mid-ocean ridge basalt (MORB). The depleted LREEs and NMORB-normalised Nd/Yb values of 0.07–0.41 indicate that the degree of partial melting for the majority of the low-Mg# eclogites protolith was ≥30%. The narrow δ18O range of 5.5–7.4‰ near the ‘gabbro–basalt’ boundary (6‰) obtained for the high-Al and low-Mg# Catoca eclogites reflects the influence of subduction-related processes. This case shows that mantle eclogites represented by two different lithologies and originating from different protoliths — plagioclase-rich precursor, presumably gabbro (for high-Al eclogites), and basalt (low-Mg# eclogites) — can provide similar and overlapping δ18O signatures on account of the influence of subduction-related processes. Chemical compositions of the high-Mg# eclogites indicate a complicated petrogenesis, and textural signatures reveal recrystallisation. The presence of Nb-rich rutile (8–12 wt% of Nb2O5) enriched with HFSE (Zr/Hf of 72.6–75.6) and multiple trace-element signatures (including reconstructed whole-rock NMORB-normalised Ce/Yb of 3.9–10.6 and Sr/Y of 5.8–9.6, MgO contents of 15.7–17.9 wt%, and high Ba and Sr) provide strong evidence for deep metasomatic alteration. High Cr contents in clinopyroxene (800–3740 ppm), garnet (430–1400 ppm), and accessory rutile (700–2530 ppm), together with extremely low Li contents of 1.0–2.4 ppm in clinopyroxene, may indicate hybridisation of the eclogites with peridotite. Comparison of the chemical compositions (major and trace elements) of (1) unaltered fresh cores of coarse-grained garnets from the low-Mg# eclogites, (2) secondary garnet rims (ubiquitous in the low-Mg# eclogites), (3) proto-cores in the coarse-grained garnet (high-Mg# eclogites), and (4) homogeneous recrystallised fine-grained garnets (high-Mg# eclogites) suggests that the high-Mg# eclogites formed through recrystallisation of low-Mg# eclogite in the presence of an external fluid in the mantle. Four of the five high-Mg# samples show that mantle metasomatism inside the Kasai craton mantle beneath the Catoca pipe occurred at a depth range of 145–160 km (4.5–4.8 GPa).

AbstractAccording to the International Technology Roadmap for Semiconductors (ITRS), the doping technology requirements for the MOSFET source and drain regions of the future CMOS generations lead to a major challenge. A critical point of this evolution is the formation of ultra-shallow junctions(USJ) for which present technologies, based on ion implantation and rapid thermal annealing, will hardly meet the ITRS specifications. Laser Thermal Processing (LTP) has been shown to be a potential candidate to solve this fundamental problem. In the present paper, LTP experiments have been performed with two XeCl excimer lasers (λ= 308 nm) with different pulse characteristics. The first laser (Lambda Physik, Compex 102) delivers 200 mJ laser pulses with a duration of ∼25 ns. The second laser is an industrial tool (SOPRA, VEL 15) that delivers 16 J laser pulses with a duration of ∼200 ns and allows to anneal a few cm die in a single laser shot. Here we examine the influence of the pulse duration on LTP of B+ (with and without Ge+ pre-amorphization) and BF2 implanted silicon samples on the basis of real-time optical monitoring of the laser induced melting/recrystallisation process, four-point probe resistivity measurements, secondary ion mass spectrometry (SIMS) depth profiles. Experimental results are compared to finite element modelisation (FIDAP Fluent Software) that takes into account both laser pulses. The activated dopant dose, junction depth and sheet resistance, as a function of the laser fluence and shot number for both lasers, confirm the efficiency of laser processing to realize ultra-shallow and highly doped junctions as required by the future CMOS generations. Influence of the pulse duration on the USJ formation process is also discussed.