By Freysteinn Sigmundsson
This e-book presents a precis of geodynamic effects from Iceland that almost immediately are present in a number of medical articles, yet haven't been amassed sooner than in a booklet. The ever expanding variety of scientists drawn to geology and geophysics of Iceland should still locate the publication a "must" to realize wisdom approximately past paintings and the prestige of data approximately Iceland.
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Extra resources for Iceland Geodynamics: Crustal Deformation and Divergent Plate Tectonics
Saemundsson, 1992). Between the northern ends of the WVZ and EVZ lies the HofsjoÈkull Volcanic Zone as de®ned here. 12). 13) is the direct onshore continuation of the MAR. Its structure diers from the rest of the volcanic zones because its overall trend is highly oblique to the plate spreading; a high amount of shearing and relatively little spreading perpendicular to its axis characterizes this volcanic zone. The division into volcanic systems is not particularly clear, and the volcanic centres are not associated with silicic rocks except at the eastern end of the zone at Hengill.
Many of them are associated with silicic rocks, high-temperature geothermal areas, and some have developed a caldera. Volcanism is frequent at the central volcanoes. Both inside and outside the central volcanoes, monogenetic crater rows, formed in ®ssure eruptions, often group together with an array of normal faults. Such zones of extensive ®ssuring and normal faulting have in Iceland been termed ``®ssure swarms''. Central volcanoes within the volcanic rifts Sec. 3 Segmentation of the volcanic zones: volcanic systems 39 in Iceland are, as a rule, transected by ®ssure swarms.
The model only resolves structures in the uppermost mantle and has a horizontal resolution of a few hundred kilometres, extending to about a 400-km depth. , 1996, 1998). The mantle transition zone between 410 and 660 km under Iceland has been inferred to be anomalously thin, and this observation is taken as an indication of mantle upwelling. Excessive temperature within a mantle plume in¯uences the 410- and 660-km phase boundaries in a dierent manner, causing upward shift of the 660-km discontinuity and downward shift in the 410-km discontinuity.