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Rising currents have apparently occurred largely in oceanic areas, bringing new mantle material to the surface in the oceans and sweeping older oceanic rocks towards and perhaps beneath the high-standing continents.
Much of the heat flow from the solid Earth into the oceans results from the slow cooling of the oceanic rocks.
The segments are differentiated by their relative abundances of Mesozoic-Cenozoic, metamorphic, and oceanic rocks and are divided into Northern, Central and Southern sectors.
Because limestone is comparatively less dense than adjacent oceanic rocks, such as basalt or chert, many of the Permian reef limestones were not as readily subducted.
As the oceanic rocks cool they become slightly denser, and isostatic adjustment causes them to subside slightly so that oceanic depths become greater.
Nearly all oceanic rocks are fairly young, mostly Jurassic or younger (i.e., less than 200,000,000 years old), but relics of ocean floor rocks have been found in ophiolite complexes as old as 3.8 billion years.
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Such is this vertiginous scene of terrible and uncontrollable chaos, with its oceanic rocking motion.
Their ratio reflects past melting of the mantle rock that gave rise to oceanic rock as well as the passage of time.
These rock assemblages, comprising oceanic igneous rocks progressively overlain by pelagic sedimentary rocks (chert and/or limestone) and trench-fill clastic sedimentary rocks (mostly sandstone, shale/mudstone), have been called ocean plate stratigraphy (OPS).
This environment lasted about 250 million years and is typified by both downwarped oceanic sedimentary rocks and terrestrial volcanic rocks.
Buoyant upwelling motions in the mantle force the plates apart at rift zones (such as along the middle of the Atlantic Ocean floor), where magmas from the underlying mantle rise to form new oceanic crustal rocks.
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