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Notes: Zusammenfassung Druck-Lösungserscheinungen sind nicht auf stylolithische Kontakte beschränkt. Die Mehrzahl der Druck-Lösungsflächen ist glatt und nicht als solche erkennbar. Bei Abwesenheit von Stylolithisierung wird Druck-Lösungsrückstand meistens fälschlich als primäres Sediment angesprochen. Druckgelöstes Material wandert von Becken aus. Auf Schwellen führt es zu erhöhtem Stoffangebot für chemische und organische Ablagerung. Druckunlösliches Material konzentriert sich passiv in den Becken. Die Unterschiede zwischen benachbarten lithologischen Horizonten werden in stratigraphischen Abfolgen während der Diagenese über Druck-Lösungstätigkeit verstärkt. Wechsellagerungen können entstehen, indem relativ „reine“, fast monomineralische Horizonte (Kalkspat, Dolomit, Quarz) von Druck-Lösung kaum betroffen werden, während etwas mehr „verunreinigte“ Schichten, besonders bei Gegenwart von Tonmineralien, bis auf ihren Lösungsrückstand zusammenschrumpfen können. Die während Faltung und Schieferung fortdauernde Druck-Lösungstätigkeit bewirkt weiteren Gesteinsschwund. Hauptsächlich synsedimentäre Lagerstätten können über Druck-Lösungsvorgänge während Diagenese und Orogenese eine weitere Anreicherung erfahren, indem Wertmineralien im Lösungsrückstand zurückbleiben. Verstärkte Anreicherungen sind in Richtung der Becken und Faltenschenkel zu erwarten.

Notes: Abstract The Earth's stress field is composed of 4 sub-fields that are induced by 1. the gravitational force (impacts, etc; geodynamic theories on the expansion or contraction of the globe); 2. the centrifugal force of the spinning Earth (models on continental drift explaining the equatorial Alpine-Himalayan collisional mountain belt and longitudinally orientated rifts or oceans); 3. thermal convection (plate tectonic model); 4. tidal forces (extended plate tectonic model). A standard global stress field results from a combination of these four sub-stress-fields. From the existence of six otherwise inexplicable geodynamic phenomena, it has to be concluded that the standard global stress field of the present can only be an instantaneous (still) photograph of a field that constantly migrates eastwards relative to the Earth's continents. This disclosure can be explained with an extended plate tectonic model, in which the Earth's surface is subdivided by the circum-Pacific ring of subduction zones, into a Pacific area and a continental or Pangaea area with intra-Pangaea oceans (Atlantic, Indian Ocean, etc.). The Pangaea area in turn is subdivided into a North Pangaea area and a South Pangaea area. Due to the off-centre rotation of the spinning Earth around the gravitational centre of the Earth-Moon (-Sun) system (tidal forces), the lower mantle, the Pacific basin, area or state (Pacific crust = lower mantle?), the remaining states that together with the Pacific state compose the Wilson Cycle of ocean opening and closing (Rift/Red Sea state, Atlantic state, Pacific state, Collision/Himalayas state), the ocean sequence of which is permanently arranged from E to W through 360° around the globe, and the standard global stress field as an expression of the Wilson Cycle, are constantly displaced eastwards relative to the upper mantle, the continents or the North and South Pangaea areas with Intra-Pangaea oceans, completing one full turn around the globe in 200 to 250 my (principle of hypocycloid gearing). The continents migrate westwards around the globe and around the Pacific basin in the N and S hemispheres, through sequences of plate tectonic settings of the Oceanic or Wilson Cycle that possess distinct regional stress fields as parts of the standars global stress field, or else the continents are subjected to eastward migrating sequences of settings with distinct regional stress fields as parts of the Wilson Cycle/standard global stress field. By rotations and N-S migrations of the individual continents dissected in all directions by groups of parallel structural planes (fracture systems) through the standard global stress field, the orientation of which is aligned with the spinning Earth's axis and equator and that constantly migrates eastwards relative to the continents, the amount and nature of stress (compression, tension, shearing) a given fracture system is subjected to is constantly altered and the tectonic activity may gradually be transferred from the system under consideration to another fracture system, with slightly different strike directions. Every 400 to 500 my or each Pangaea Cycle (two complete W-E/E-W displacements around the globe between the continents/Pangaea areas with Intra-Pangaea Oceans/upper mantle on the one side and the lower mantle/Pacific basin/ sequence of ocean states and local stress fields of the Wilson Cycle and the standard global stress field on the other) the inhomogeneous standard global stress field is reversed in the N-S direction. Any model proposing the long-time existence of extended lineaments or fracture systems that do not end at the margin of the respective continent or at an orogen/suture zone/former continental margin, in the event of being older than the respective orogenesis, but which cross the surrounding ocean or the younger orogen and continue in the neighbouring continents or former independent continents or even encompass the whole globe, and which puts foreward simultaneous tectonic activity along the whole length of such lineament or fracture system and proposes their longevity or permanent existence, contradicts the physical laws that are the foundation of plate tectonics and mobilism.

Notes: Note by the Editor Communication between Dr. Aksirov and Dr. Trurnit has shortly before printing resulted in more preciseness (Tab 1 in Aksirov's paper). It was no more possible to adapt Dr. Trurnit's Comments correspondingly. The editor apologizes for this shortcoming; he believes, however, that the theme is still thought-provoking and worthwhile to read.

Notes: Abstract Due to the westward-directed off-centre rotation of the spinning Earth around the gravitational centre of the Earth-Moon (-Sun) system the lower mantle should be displaced eastwards in relation to the upper mantle-crust system (principle of hypocycloid gearing). In consequence, the shape of the Pacific is displaced eastwards above gravity anomalies of the lower mantle in relation to the Earth's crust (once around the globe in 200 to 250 my; 20 to 16 cm/y East drift), thus causing the Global Tectonic Megacycles (Oceanic/Wilson Cycle, Orogenic Cycle, Cycle of the Collisional Mountain Belt, etc.) The continents migrate westwards around the shape of the Pacific in the N and S. They collide sequentially W of the Pacific continuously adding segments to a collisional mountain belt, that becomes older towards the W (zip fastener principle) and since the Permian has lapped some 1 1/3 times around the cratonic nucleus of Laurasia in the form of a spiral (explanation for lateral continental growth and the cyclical repetition of orogenic events for a certain continental margin). Following half an E drift lapping of the Earth's crust by the shape of the Pacific, the Pacific appears again in the W. In the Mediterranean/Caribbean setting (tongue of the Pacific) the continents of the N and S hemispheres that had previously collided sequentially W of the Pacific separate again (rift propagation towards the E), whereby parts of the N margins of the S continents remain attached to the N continents in the form of tectonostratigraphic terranes, which will subsequently migrate westwards around the shape of the Pacific in the N. The Earth's crust is subdivided into a Pacific area and a continental or Pangaea area with Intra-Pangaea Oceans (Atlantic, Red Sea-Indian Ocean, etc.). The Pangaea area in turn is subdivided into a North Pangaea area and a South Pangaea area with the North and South Pangaea continents broadly distributed over the N and S hemispheres. The Earth's history appears to be subdivided into alternating North Pangaea growth/South Pangaea breakup eras (Permian to present Alpine Cycle; Late Proterozoic Panafrican-Brasiliano Cycle) and South Pangaea growth/North Pangaea breakup eras (Late Proterozoic and Early to Middle Paleozoic Baikalian-Caledonian Cycle; Middle Proterozoic Kibaran-Grenvillian Cycle). In the hemisphere of the Pangaea growing (since the Permian the N hemisphere) the continents are subjected to pendular movements (alternating clockwise and counterclockwise rotations combined with movements between high and low latitudes). They always face either the equator or the Pacific with the same margin. Otherwise, a collisional mountain belt would not form. The remaining two margins alternate between an Arctic- and a North Atlantic-type setting. The Cordilleran-type margin of the NE-Pacific is therefore the forerunner of the NW-Pacific island arc-type and both types are one-sided, embryonic states of the two-sided collisional mountain belt forming at the equator W of the Pacific. Since the Jurassic/Cretaceous, the Pacific margins of the N hemisphere are remobilized segments from the older lap of the North Pangaea collisional mountain belt spiral. In the hemisphere of the Pangaea breaking up (since the Permian the S hemisphere) a continent passing through the Antarctica setting rotates through approximately 120° (clockwise during a South Pangaea breakup — Permian to present; counterclockwise during a North Pangaea breakup — Late Proterozoic and Early to Middle Paleozoic) and breaks up into several India-, Australia- and Antarctica-size fragments. The one-sided Andes-type margin of the SE-Pacific (previously evolved from a West Africa-type margin) develops therefore into a one-sided New Guinea-type and into the equatorwards facing thrust zone of the two-sided collisional mountain belt forming at the equator W of the Pacific. On the other hand the SW-Pacific island arc-type margin has evolved from a North-type that might still carry fragments from the older lap of the collisional mountain belt (Atlas, parts of the N Andes and West Antarctica, New Zealand), the main parts of which migrate around the shape of the Pacific in the N in the form of tectonostratigraphic terranes. Due to the pendular movements of a continent from the Pangaea growing and the 120° rotation of a continent from the Pangaea breaking up passing through the Antarctica setting, between its birth in a rift and its death in the collision zone at the equator W of the Pacific, a continental margin will normally need much more time (Cycle of Continental Margins) than the 200 to 250 my necessary for one E drift lapping of the Earth's crust by the shape of the Pacific and the ocean states of the Wilson Cycle or Oceanic Cycle. The eugeosynclinal evolution of an ocean in most cases will therefore be comparatively shorter than the miogeosynclinal evolution of the continental margins bordering that ocean.