It decoded the video signal into its red, green and blue components allowing for complex mixing and interlayering of colours and images. The device allowed “video” to be “played live” like a musical instrument. Utilising the Videokalos synthesiser, Donebauer founded the Video And Music Performers (VAMP) delivering live interactive performances created between video and music performers.
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The 10-meter-thick Lower Hamstead Member follows directly upon the Bembridge Marls Member with a 40-centimetre-thick olive to black seam, the Black Band. This layer is very rich in organic matter and was deposited under freshwater conditions. At its base it carries calcrete nodules and rootlets. The Black Band is overlain by roughly 4 metres of a greenish- greyish clay-silt interlayering.
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The Upper Hamstead Member can reach a thickness of 60 meters. It starts with a 3-meter thick interlayering of greenish-greyish clay and silt bearing decalcified Polymesoda shells. Roughly 10 metres above the base follows the Eomys bed and immediately above it the White Band also containing Polymesoda shells. After the Crocodile bed the member ends with 8 meters of turquoise, plastic clays with orange-red freckles.
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In windier regions, as in the Southern Ocean, frazil ice accumulation may occur along the downwind side of leads. If the ice on that side is thin, the frazil may be driven below that ice (resulting in a complex interlayering pattern). Leads affect global water circulation. As ice begins to form inside a lead, it incorporates some of the salt in the seawater This is why sea ice is saline.
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A well-documented example of flooding caused by isostatic depression is the case of Charlotte, The Vermont Whale,Wright, W.A., 2000, Charlotte, The Vermont Whale An Electronic Museum. University of Vermont, Burlington, Vermont a fossil whale found in the deposits of the former Champlain Sea. Like many similar marine deposits, the sediments, which accumulated within the Champlain Sea lack the physical characteristics; i.e. sedimentary structures, interlayering, and textures, that characterize sediments deposited by a mega-tsunami.
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In the northern Dinaride Mountains, flysch several meters thick grades from Maastrichtian sandstone, siltstone and shale into Paleocene calcite shale, calcareous sandstone, sandy limestones and limestones. The flysch is overlain by more limestone from the Middle Eocene. In some cases, the interlayering of Late Cretaceous-Paleogene flysch with volcanic rocks has resulted in medium-pressure metamorphism. Rock sequences prograde from sandstone, shale, marl and limestone to slate and meta-sandstone along with greenschist, mica schist, amphibolite, gneiss and phyllite.
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Kennedy Ranges, near Gascoyne Junction, Western Australia in the permanent collection of The Children's Museum of Indianapolis. The characteristing banding and ribbon-like layering often observed in radiolarites is primarily due to changing sediment influx, which is secondarily enhanced by diagenetic effects. In the simple two component system clay/silica with constant clay supply the rhythmically changing radiolarian blooms are responsible for creating a clay-chert interlayering. These purely sedimentary differences become enhanced during diagenesis as the silica leaves the clayey layers and migrates towards the opal-rich horizons.
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After an interlude of grey, nodular, goniatite-bearing limestones, the Upper Cherts were deposited during the Viséan—grey or green cherts sometimes interlayered with pyroclastics and ending with grey nodular limestones. The Mississippian later on changes into the nearly 1000 m thick detrital, syn-orogenic sediments of the Kulm–facies. An exception are the western Pyrenees, where, during the Serpukhovian, dark grey, laminated limestones precede the Kulm. The diachronous Kulm sediments are a flysch-like (turbidites) interlayering of sandstones and dark shales—harbingers of the Variscan tectonic movements.
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As inferred from relict structures and textures, the Brahma Schist is composed of mafic to felsic-composition metavolcanic rocks. The Rama Schist consists of massive, fine-grained quartzofeldspathic schist and gneiss that likely are probable felsic metavolcanic rocks. On the basis of the presence of relict pillow structures, interlayering of metavolcanic strata, and the large volumes of metavolcanic rocks, the Brahma and Rama schists are interpreted to consist of metamorphosed, volcanic island-arc and associated submarine volcanic rocks. These metavolcanic rocks are locally overlain by the metamorphosed submarine sedimentary rocks of the Vishnu Schist that are interpreted to have accumulated in oceanic trenches.
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The complex intercalation of carbonate and clastic sediments within the Kaibab Limestone reflects the deposition of sediments within a gently sloping continental margin during a period of frequent, high-frequency sea level changes. Relatively minor changes in sea level caused major lateral shifts in the position of supratidal, subtidal, and shallow-marine environments during the deposition of the Kaibab Limestone. The shifting sea levels and associated depositional environments created a complex interlayering of different types of carbonate and clastic sediments in the strata that comprise the Kaibab Limestone. The gently sloping continental margin on which the Kaibab Limestone accumulated, extended seaward from northern Arizona to southern Nevada, at times exceeding 200 miles (125 km) in width.
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