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Relevant bibliographies by topics / Geology Southern Hemisphere

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Academic literature on the topic 'Geology Southern Hemisphere'

Author: Grafiati

Published: 4 June 2021

Last updated: 7 February 2022

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Journal articles on the topic "Geology Southern Hemisphere"

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Sykes, T. J. S., J. Y. Royer, A. T. S. Ramsay, and R. B. Kidd. "Southern hemisphere palaeobathymetry." Geological Society, London, Special Publications 131, no. 1 (1998): 1–42. http://dx.doi.org/10.1144/gsl.sp.1998.131.01.02.

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Aoyama, Michio, Pavel P. Povinec, and Joan-Albert Sanchez-Cabeza. "The Southern Hemisphere Ocean Tracer Studies (SHOTS) project." Progress in Oceanography 89, no. 1-4 (2011): 1–6. http://dx.doi.org/10.1016/j.pocean.2010.12.002.

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Murray, D. S., A. E. Carlson, B. S. Singer, et al. "Northern Hemisphere forcing of the last deglaciation in southern Patagonia." Geology 40, no. 7 (2012): 631–34. http://dx.doi.org/10.1130/g32836.1.

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Dudeney, J. R., K. B. Baker, P. H. Stoker, and A. D. M. Walker. "The Southern Hemisphere Auroral Radar Experiment (SHARE)." Antarctic Science 6, no. 1 (1994): 123–24. http://dx.doi.org/10.1017/s0954102094000155.

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The near Earth space environment (known as Geospace) is dominated by the interaction between the solar wind and the geomagnetic field, which creates the magnetosphere. Considerable energy flows from the solar wind into the magnetosphere and ends up in the Earth's upper atmosphere (the thermosphere and ionosphere). The coupling of the geomagnetic field with that of the solar wind (known as the interplanetary magnetic field, or IMF) produces a variety of electro-dynamic responses with signatures such as electric fields and currents in the polar ionospheres. These produce, inter alia, motion of the ionospheric plasma (at altitudes between 100 and 1000kms) which can be monitored from the ground using radar techniques. Analysis of such plasma motion provides a very powerful means of investigating the nature of the interactions taking place at the boundaries between the magnetosphere and the solar wind. To do this effectively requires simultaneous measurements over as large an area (in latitude and longitude) as possible.

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Han, Zhong, Xiumian Hu, Marcelle BouDagher-Fadel, Hugh C. Jenkyns, and Marco Franceschi. "Early Jurassic carbon-isotope perturbations in a shallow-water succession from the Tethys Himalaya, southern hemisphere." Newsletters on Stratigraphy 54, no. 4 (2021): 461–81. http://dx.doi.org/10.1127/nos/2021/0650.

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Morgan, Vin. "A new Southern Hemisphere climate clock." Quaternary Science Reviews 24, no. 12-13 (2005): 1331–32. http://dx.doi.org/10.1016/j.quascirev.2005.04.001.

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Belenkaya, E. S., S. W. H. Cowley, V. V. Kalegaev, O. G. Barinov, and W. O. Barinova. "Magnetic interconnection of Saturn's polar regions: comparison of modelling results with Hubble Space Telescope UV auroral images." Annales Geophysicae 31, no. 8 (2013): 1447–58. http://dx.doi.org/10.5194/angeo-31-1447-2013.

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Abstract. We consider the magnetic interconnection of Saturn's northern and southern polar regions controlled by the interplanetary magnetic field (IMF), studying in particular the more complex and interesting case of southward IMF, when the Kronian magnetospheric magnetic field structure is the most twisted. The simpler case of northward IMF is also discussed. Knowledge of the magnetospheric magnetic field structure is very significant, for example, for investigation of the electric fields and field-aligned currents in Saturn's environment, particularly those which cause the auroral emissions. Here we modify the paraboloid magnetospheric magnetic field model employed in previous related studies by including higher multipole terms in Saturn's internal magnetic field, required for more detailed considerations of inter-hemispheric conjugacy, together with inclusion of a spheroidal boundary at the ionospheric level. The model is employed to map Southern Hemisphere auroral regions observed by the Hubble Space Telescope (HST) in 2008 under known IMF conditions to both the equatorial plane and the northern ionosphere. It is shown that the brightest auroral features map typically to the equatorial region between the central ring current and the outer magnetosphere, and that auroral features should be largely symmetric between the two hemispheres, except for a small poleward displacement and latitudinal narrowing in the Northern Hemisphere compared with the Southern Hemisphere due to the quadrupole field asymmetry. The latter features are in agreement with the conjugate auroras observed under near-equinoctial conditions in early 2009, when IMF data are not available.

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Stephenson, M. H., L. Angiolini, P. Cózar, et al. "Northern England Serpukhovian (early Namurian) farfield responses to southern hemisphere glaciation." Journal of the Geological Society 167, no. 6 (2010): 1171–84. http://dx.doi.org/10.1144/0016-76492010-048.

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Mayr, C., A. Lücke, S. Wagner, et al. "Intensified Southern Hemisphere Westerlies regulated atmospheric CO2 during the last deglaciation." Geology 41, no. 8 (2013): 831–34. http://dx.doi.org/10.1130/g34335.1.

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Vaishnav, Rajesh, Erik Schmölter, Christoph Jacobi, Jens Berdermann, and Mihail Codrescu. "Ionospheric response to solar extreme ultraviolet radiation variations: comparison based on CTIPe model simulations and satellite measurements." Annales Geophysicae 39, no. 2 (2021): 341–55. http://dx.doi.org/10.5194/angeo-39-341-2021.

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Abstract. The ionospheric total electron content (TEC) provided by the International GNSS Service (IGS) and the TEC simulated by the Coupled Thermosphere Ionosphere Plasmasphere Electrodynamics (CTIPe) model have been used to investigate the delayed ionospheric response against solar flux and its trend during the years 2011 to 2013. The analysis of the distinct low-latitude and midlatitude TEC response over 15∘ E shows a better correlation of observed TEC and the solar radio flux index F10.7 in the Southern Hemisphere compared to the Northern Hemisphere. Thus, a significant hemispheric asymmetry is observed. The ionospheric delay estimated using model-simulated TEC is in good agreement with the delay estimated for observed TEC against the flux measured by the Solar Dynamics Observatory (SDO) extreme ultraviolet (EUV) Variability Experiment (EVE). The average delay for the observed (modeled) TEC is 17(16) h. The average delay calculated for observed and modeled TEC is 1 and 2 h longer in the Southern Hemisphere compared to the Northern Hemisphere. Furthermore, the observed TEC is compared with the modeled TEC simulated using the SOLAR2000 and EUVAC flux models within CTIPe over northern and southern hemispheric grid points. The analysis suggests that TEC simulated using the SOLAR2000 flux model overestimates the observed TEC, which is not the case when using the EUVAC flux model.

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Dissertations / Theses on the topic "Geology Southern Hemisphere"

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McGlue, Michael Matthew. "LATE QUATERNARY PALEOLIMNOLOGY IN THE SOUTHERN HEMISPHERE TROPICS." Diss., The University of Arizona, 2011. http://hdl.handle.net/10150/204064.

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Lake deposits are widespread throughout the Phanerozoic rock record and have long intrigued geologists and paleobiologists in search of natural resources or fossil biota. Low-energy lacustrine depositional environments, characterized by relatively rapid sediment influx rates and shallow zones of bioturbation, likewise produce highly-resolved archives of climate and ecosystems evolution. This dissertation describes four studies that use lake sediments for Quaternary environmental analysis. In East Africa, many decades of prior study provided the critical framework necessary for in-depth paleoenvironmental research at Lake Tanganyika (3° - 9°S). Seismic stratigraphic analysis integrated with radiocarbon-dated sediment cores from the Kalya horst and platform document a dramatic lake level lowstand prior to ~106 ka and a minor, short-lived regression during the Last Glacial Maximum (32 - 14 ka). Paleobathymetric maps reveal that Lake Tanganyika remains a large, connected water body even during episodes of extreme drought, which has implications for local and regional fauna. Over shorter timescales, geochronological, taphonomic and sedimentological analyses of shell beds around Kigoma (central Lake Tanganyika) document three distinct facies-types that are time-averaged over the latest Holocene. Lake level fluctuations associated with the termination of the Little Ice Age (~ 16th century CE) and subsequent encrustation played a key role in shell bed formation and persistence along high-energy littoral platforms, which has implications for structuring specialized communities of benthic fauna. In central South America (18° - 22°S), we studied the limnogeology of small lakes in the Puna and the Pantanal. Analyses of these sites were undertaken to: 1) ascertain how the lakes act as depositional basins; 2) assess sedimentation rates; and 3) construct limnogeological databases to guide future interpretations of ancient sediment cores. At Laguna de los Pozuelos (Argentine Puna), linear sedimentation rates approach 0.14 cm*y⁻¹ in the playa-lake center, and litho- and organo-facies development are dominantly controlled by basin hydrology, climate and biological feedbacks (both nutrient cycling and bioturbation) from waterbirds. At Lagoas Gaíva, Mandioré and Vermelha (Brazilian Pantanal), short-lived radioisotopes indicate uninterrupted depositional rates of 0.11 - 0.24 cm*y⁻¹, and hydrochemical and depositional patterns respond sensitively to changes in the seasonal flooding cycle of the Upper Paraguay River.

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Books on the topic "Geology Southern Hemisphere"

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Fossil Conchostraca of the Southern Hemisphere and continental drift: Paleontology, biostratigraphy, and dispersal. Geological Society of America, 1987.

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Book chapters on the topic "Geology Southern Hemisphere"

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Rogers, John J. W., and M. Santosh. "History of Continents after Rifting from Pangea." In Continents and Supercontinents. Oxford University Press, 2004. http://dx.doi.org/10.1093/oso/9780195165890.003.0012.

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As continents moved from Pangea to their present positions, they experienced more than 100 million years of geologic history. Compressive and extensional stresses generated by collision with continental and oceanic plates formed mountain belts, zones of rifting and strike-slip faulting, and magmatism in all of these environments. In this chapter we can only provide capsule summaries of this history for each of the various continents, but many of their salient features have been discussed as examples of tectonic processes in earlier chapters. The final section analyzes the breakup of Pangea as part of the latest cycle of accretion and dispersal of supercontinents. Because it involves continuation of this cycle into the future, it is necessarily very speculative. Figure 10.1 shows approximate patterns of movement of each continent from its position in Pangea to the present. The dominant feature of this pattern is northward movement of all continents except Antarctica, which has remained over the South Pole for more than 250 million years. Shortly after geologists recognized the concept of continental drift, this movement was referred to by the German word “Polflucht” (flight from the pole) because all of the continents were seen to be fleeing from the South Pole. The only continent that did not simply move northward was Eurasia, which essentially rotated clockwise and changed its orientation from north–south to east–west. Comparison of fig. 10.1 with fig. 8.12a (locations of continents shortly before the assembly of Gondwana) shows that the net effect of the last 580 million years of earth history has been a transfer of most continental crust from the southern hemisphere to the northern hemisphere. Accretion and compression against the southern margin of Eurasia constructed a series of mountain belts from the Pyrenees in the west to the numerous ranges of Southeast Asia in the east. This collision generated extensional and transtensional forces that opened rifts and pull-apart basins. Tectonic loading created foreland basins with sediment thicknesses of several kilometers. Opposite the area where the collision of India caused the most intense compression, the extensional basins are interspersed with mountain ranges that were lifted up intracontinentally. We divide the discussion of Eurasia into a section where compression dominates to the south (present orientation) of the former margin of Pangea and a section that describes processes within the landmass to the north.

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Elias, Scott. "Millennial and Century Climate Changes in the Colorado Alpine." In Climate Variability and Ecosystem Response in Long-Term Ecological Research Sites. Oxford University Press, 2003. http://dx.doi.org/10.1093/oso/9780195150599.003.0033.

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Ecosystems are the products of regional biotic history, shaped by environmental changes that have occurred over thousands of years. Accordingly, ecological changes take place at many timescales, but perhaps none is more significant than the truly long-term scale of centuries and millennia, for it is at these timescales that ecosystems form, break apart, and reform in new configurations. This is certainly true in the alpine regions, where glaciations have dominated the landscape for perhaps 90% of the last 2.5 million years (Elias 1996a). In the alpine tundra zone, the periods between ice ages have been relatively brief (10,000–15,000 years), whereas glaciations have been long (90,000–100,000 years). Glacial ice has been the dominant force in shaping alpine landscapes. Glacial climate has been the filter through which the alpine biota has had to pass repeatedly in the Pleistocene. This chapter discusses climatic events during the last 25,000 years (figure 18.1). At the beginning of this interval, temperatures cooled throughout most of the Northern Hemisphere, culminating in the last glacial maximum (LGM), about 20,000–18,000 yr b.p. (radiocarbon years before present). The Laurentide and Cordilleran ice sheets advanced southward, covering most of Canada and the northern tier of the United States. Glaciers also crept down from mountaintops to fill high valleys in the Rocky Mountains. In the Southern Rockies, the alpine tundra zone crept downslope into what is now the subalpine, beyond the reach of the relatively small montane glaciers. By about 14,000 yr b.p., the glacier margins began to recede, leading eventually to the postglacial environments of the Holocene. It is now becoming apparent that the climate changes that drove these events were surprisingly rapid and intense. This chapter examines the evidence for these climatic changes and the biotic response to them in the alpine zone of Colorado. To reconstruct the environmental changes of this period, we must rely on proxy data, that is, the fossil record of plants and animals, combined with geologic evidence, such as the age and location of glacial moraines in mountain valleys. As of this writing, the principal biological proxy data that have been studied in the Rocky Mountains are fossil pollen and insects.

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