Jma Cross Reference Software 23

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This product includes CPT which is commercial technical data and/or computer data bases and/or commercial computer software and/or commercial computer software documentation, as applicable which were developed exclusively at private expense by the American Medical Association, 515 North State Street, Chicago, Illinois, 60610. U.S. Government rights to use, modify, reproduce, release, perform, display, or disclose these technical data and/or computer data bases and/or computer software and/or computer software documentation are subject to the limited rights restrictions of DFARS 252.227-7015(b)(2)(June 1995) and/or subject to the restrictions of DFARS 227.7202-1(a)(June 1995) and DFARS 227.7202-3(a)(June 1995), as applicable for U.S. Department of Defense procurements and the limited rights restrictions of FAR 52.227-14 (June 1987) and/or subject to the restricted rights provisions of FAR 52.227-14 (June 1987) and FAR 52.227-19 (June 1987), as applicable, and any applicable agency FAR Supplements, for non-Department Federal procurements.

jma cross reference software 23

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In contrast to the 2014/15 European emergence of HPAI H5N8, when a single lineage of HPAI spread across Europe, the chain of events during the 2016/17 HPAI H5 emergence shows more similarities to the 2014/15 situation in the United States (US), where the HPAI H5N8 group A viruses reassorted with local LPAI viruses causing massive and long lasting detection in both poultry and wild birds and local die-offs in wild birds [6]. While this manuscript was in preparation, detections of HPAI H5 clade 2.3.4.4 virus in Europe were still reported in Belgium, Luxembourg, the Netherlands and the United Kingdom [18], even though migrating birds had largely left their European wintering sites, suggesting that virus amplification was now occurring in local resident birds. This is a cause of concern, as establishment of HPAI viruses among wild birds is difficult to control and may give rise to a situation comparable to that in Asia with new outbreaks in wild birds and poultry not being caused by novel introductions of HPAI viruses from distant areas, but from within the local populations. It remains unclear, however, what drivers are responsible for the duration of virus circulation in a wild bird population, either long (US 2014/15 and Europe 2016/17) or short (Europe 2014/15), and based on current knowledge we cannot predict how the H5 situation among wild birds in Europe will evolve.

The lithosphere is the outermost, relatively rigid shell of the Earth, made up of the crust and the underlying lithospheric mantle. Beneath the continents, the subcontinental lithospheric mantle (SCLM) varies widely in thickness, from a few tens of kilometers beneath active rift zones to >250 km beneath some ancient cratonic blocks. The SCLM, as sampled by xenoliths in volcanic rocks and some exposed massifs, consists almost entirely of peridotitic rocks (olivine + orthopyroxene garnet clinopyroxene spinel). Re-Os isotopic studies show that beneath some Archean cratons, the SCLM is at least as old as the oldest known crustal rocks (Carlson et al., 1999; Griffin et al., 2004; references therein).

The secular evolution of SCLM composition has major consequences for the nature of crustal tectonics through time. Archon SCLM is buoyant relative to the underlying asthenosphere, and this buoyancy may have played an important role in the stabilization of cratons (Poudjom Djomani et al., 2001). Tecton SCLM, being less depleted, is buoyant relative to the asthenosphere as long as its geotherm remains elevated, but on cooling it is likely to become unstable, and may delaminate and sink. At some convergent margins, crustal thickening and the transformation of mafic lower crust to eclogite may result in a more continuous drip-style of lithosphere removal (e.g., Sobolev et al., 2005). In either case, the ensuing upwelling of asthenospheric material can lead to widespread crustal melting, as in the Central Asian Orogenic Belt (Zheng et al., 2006; references therein). Refertilization of older SCLM by asthenosphere-derived melts leads to an increase in SCLM density, enhancing the probability of delamination. The nature and history of the SCLM therefore will affect the response of the overlying crust to tectonic stresses. Lithospheric architecture, and particularly the presence of boundaries between domains with different types of SCLM, will be important in controlling crustal tectonics, and especially the transport of fluids and magmas from depth. This control may have important implications for the distribution of major ore deposits; an understanding of crust-mantle linkages and lithospheric architecture therefore has direct economic relevance.

Most of our detailed knowledge of SCLM composition comes from the study of xenoliths and xenocrysts brought up in volcanic rocks (Griffin et al., 1999; O'Reilly and Griffin, 2006; references therein). However, these samples are scattered in time and space, and are not available for large areas of the continents. To map the SCLM, and to understand its evolution, we must turn to geophysical data, and learn to interpret these data in terms of SCLM composition and evolution.

This brief review of the complex basement geology of Africa (Fig. 1) focuses primarily on the timing and nature of major tectonothermal events that have affected specific areas. It is intended to provide a background for examining correlations between mantle composition, the geophysical signature of the SCLM, and the evolution of the overlying crust. Details of age relationships and alternative structural interpretations have necessarily been subordinated to this larger aim. To simplify reading, key references are gathered at the beginning of each section.

In this depth slice, the cratons show up as red to white, indicating higher Vs, whereas the East Africa Rift shows as a dark-blue zone, denoting very low Vs. Areas of intermediate velocity (light green to yellow) extend westward across the Sudan, Chad, and Nigeria, and northward from the Hoggar Swell in southern Algeria. The East Saharan Craton (or Sahara Metacraton) is visible as a series of knobs with higher Vs. The high-Vs core of the West African Craton has relatively sharp, straight boundaries on the W, SW, S, SE, and NE sides, with several protrusions around the northern boundary. The center of the Craton, beneath the Taoudeni Basin, has subtly lower Vs than the immediately surrounding areas. The Congo Craton is seen as an ovoid block with weakly curved edges on the N, NW, SE, and NE sides; the W flank extends well out beneath the Atlantic, and the NW edge corresponds to the NE-SW Cameroon Line of volcanic islands. A large block with higher Vs lies offshore from the Namibia-Angola border. The Congo Craton is linked by a NW-SE belt of higher Vs to the Kalahari Craton, which consists of several centers of high Vs (Zimbabwe Craton and Kaapvaal Craton), separated by zones of slightly lower Vs. Part of the Tanzanian Craton is visible as a knob of low to intermediate Vs (green-yellow) on the S end of the East African Rift low-Vs zone. The Damara Orogen and the Namaqua-Natal Belt, like the Oubanguides Belt, are underlain by material of intermediate Vs with local higher Vs subdomains.

At this depth the Sahara Metacraton appears to consist of several distinct blocks of intermediate Vs, with low-Vs zones between them. Similar material extends across Algeria N of the Hoggar low-Vs feature. The zone of higher Vs material off the coast of northern Namibia persists to these depths, and is separated from the Congo Craton by a belt of (mostly) low-Vs material that extends down into the Damara Orogen.

Chemical tomography sections for a number of localities across southern Africa can be used to illustrate the correlations between mantle type and Vs, and to provide a basis for interpreting the seismic tomography images in terms of SCLM composition and history. An example is shown in Figure 11; vertical variations in rock types and degree of metasomatism are reflected in calculated Vs. Different styles of metasomatism have different effects on bulk composition and seismic velocity. Thus lherzolitic rocks produced dominantly by phlogopite-related metasomatism (green in Fig. 11) may still be relatively magnesian, whereas the melt-related metasomatism (red in Fig. 11) signature is typical of sheared lherozlite xenoliths, which have low Mg# and compositions approaching that of the convecting mantle, and hence lower Vs. The petrological data thus provide information on the vertical variation of Vs at a scale that rarely can be imaged by seismic techniques, but which can help to interpret the mean seismic velocities of individual areas.

Alkali basalts scattered across northern Africa and along the East Africa Rift carry spinellherzolite xenoliths of fertile to moderately depleted compositions. Worldwide, such basalts are erupted along elevated advective geotherms similar to the well-defined southeast Australia xenolith geotherm (O'Reilly and Griffin, 1985; Xu et al., 2000), and typical SCLM thicknesses are

The Archean cratons of West Africa, including greater Leo-Man-Ghana, Taoudeni, and Reguibat, probably were widely separated at this time. By ca. 2.8 Ga the core of the Congo Craton was 2000 km across; on the southern edge the small Kasai Craton probably was accreted during Neoarchean time. The Zimbabwe Craton was amalgamated by a series of east-directed collisions between 2.68 Ga and the docking of the Limpopo microcontinent by ca. 2.60 Ga (Dirks and Jelsma, 2002). Collision of this combined Craton with the Kaapvaal Craton to form the Kalahari Craton occurred at either ca. 2.61 Ga (Griffin et al., 2005), or perhaps at ca. 2.0 Ga. The northern and southern Angolan Craton joined perhaps as early as ca. 2.64 Ga. Re-Os data on mantle peridotite xenoliths from the Kaapvaal Craton suggest that individual terranes carried their own SCLM roots into these collisions (Griffin et al., 2004). These events produced cratonic nuclei large enough to survive (at least in part) subsequent modification. 2ff7e9595c