Chemical Formula: NaFe3+Si2O6 Locality: Norway, Buskerud, Kongsberg. Magnet Cove, Hot Spring County, Arkansas. Name Origin: Named after the Teutonic god of the sea. Acmite is from the Greek “point” in allusion to the pointed crystals.
Aegirine is a member of the clinopyroxene group of inosilicates. Aegirine is the sodium endmember of the aegirine-augite series. Aegirine has the chemical formula NaFe3+Si2O6 in which the iron is present as Fe3+. In the aegirine-augite series the sodium is variably replaced by calcium with iron(II) and magnesium replacing the iron(III) to balance the charge. Aluminium also substitutes for the iron(III). It is also known as acmite, which is a fibrous, green-colored variety.
Aegirine occurs as dark green monoclinic prismatic crystals. It has a glassy luster and perfect cleavage. The Mohs hardness varies from 5 to 6 and the specific gravity is 3.2 to 3.4.
Commonly occurs in alkalic igneous rocks, nepheline syenites, carbonatites and pegmatites. Also in regionally metamorphosed schists, gneisses, and iron formations; in blueschist facies rocks, and from sodium metasomatism in granulites. It may occur as an authigenic mineral in shales and marls. It occurs in association with potassic feldspar, nepheline, riebeckite, arfvedsonite, aenigmatite, astrophyllite, catapleiite, eudialyte, serandite and apophyllite.
Localities include Mont Saint-Hilaire, Quebec, Canada; Kongsberg, Norway; Narsarssuk, Greenland; Kola Peninsula, Russia; Magnet Cove, Arkansas, USA; Kenya; Scotland and Nigeria.
It was first described in 1835 for an occurrence in Rundemyr, Øvre Eiker, Buskerud, Norway. Aegirine was named after Ægir, the Teutonic god of the sea. A synonym for the mineral is acmite (from Greek ἀκμή “point, edge”) in reference to the typical pointed crystals.
Physical Properties
Color: Green, Greenish black, Reddish brown, Black. Density: 3.5 – 3.54, Average = 3.52 Diaphaneity: Subtransparent to translucent to opaque Fracture: Brittle – Generally displayed by glasses and most non-metallic minerals. Hardness: 6-6.5 – Orthoclase-Pyrite Luminescence: Non-fluorescent. Luster: Vitreous – Resinous Streak: yellowish gray
The Cascade Volcanoes (also known as the Cascade Volcanic Arc or the Cascade Arc) are a number of volcanoes in a volcanic arc in western North America, extending from southwestern British Columbia through Washington and Oregon to Northern California, a distance of well over 700 mi (1,100 km). The arc has formed due to subduction along the Cascadia subduction zone. Although taking its name from the Cascade Range, this term is a geologic grouping rather than a geographic one, and the Cascade Volcanoes extend north into the Coast Mountains, past the Fraser River which is the northward limit of the Cascade Range proper.
Some of the major cities along the length of the arc include Portland, Seattle, and Vancouver, and the population in the region exceeds 10,000,000. All could be potentially affected by volcanic activity and great subduction-zone earthquakes along the arc. Because the population of the Pacific Northwest is rapidly increasing, the Cascade volcanoes are some of the most dangerous, due to their past eruptive history, potential eruptions and because they are underlain by weak, hydrothermally altered volcanic rocks that are susceptible to failure. Mount Rainier is one of the Decade Volcanoes due to the danger it poses to Seattle and Tacoma. Many large, long-runout landslides originating on Cascade volcanoes have inundated valleys tens of kilometers from their sources, and some of the inundated areas now support large populations.
The Cascade Volcanoes are part of the Pacific Ring of Fire, the ring of volcanoes and associated mountains around the Pacific Ocean. All of the known historic eruptions in the contiguous United States have been from the Cascade Volcanoes. Two most recent were Lassen Peak in 1914 to 1921 and a major eruption of Mount St. Helens in 1980. It is also the site of Canada’s most recent major eruption about 2,350 years ago at the Mount Meager volcanic complex.
Geology
The Cascade Arc includes nearly 20 major volcanoes, among a total of over 4,000 separate volcanic vents including numerous stratovolcanoes, shield volcanoes, lava domes, and cinder cones, along with a few isolated examples of rarer volcanic forms such as tuyas. Volcanism in the arc began about 37 million years ago, however, most of the present-day Cascade
Map of the Cascadia Volcanic Arc.
volcanoes are less than 2,000,000 years old, and the highest peaks are less than 100,000 years old. Twelve volcanoes in the arc are over 10,000 ft (3,000 m) in elevation, and the two highest, Mount Rainier and Mount Shasta, exceed 14,000 ft (4,300 m). By volume, the two largest Cascade volcanoes are the broad shields of Medicine Lake Volcano and Newberry Volcano, which are about 145 mi³ (600 km³) and 108 mi³ (450 km³) respectively. Mount Garibaldi and Glacier Peak are the only two Cascade volcanoes that are made exclusively of dacite.
Over the last 37 million years, the Cascade Arc has been erupting a chain of volcanoes along the Pacific Northwest. Several of the volcanoes in the arc are frequently active. The volcanoes of the Cascade Arc share some general characteristics, but each has its own unique geological traits and history. Lassen Peak in California, which last erupted in 1917, is the southernmost historically active volcano in the arc, while Mount Meager in British Columbia, which erupted about 2,350 years ago, is generally considered the northernmost member of the arc. A few isolated volcanic centers northwest of Mount Meager such as the Silverthrone Caldera, which is a circular 20 km wide, deeply dissected caldera complex, may also be the product of Cascadia subduction because andesite, basaltic andesite, dacite and rhyolite can be found at these volcanoes and elsewhere along the subduction zone. At issue are the current plate configuration and rate of subduction but based on chemistry is for these volcanoes to be subduction related and are therefore part of the Cascade Volcanic Arc. The Cascade Volcanic Arc appears to be segmented; the central portion of the arc is the most active and the northern end least active.
Lavas representing the earliest stage in the development of the Cascade Volcanic Arc mostly crop out south of the North Cascades proper, where uplift of the Cascade Range has been less, and a thicker blanket of Cascade Arc volcanic rocks has been preserved. In the North Cascades, geologists have not yet identified with any certainty any volcanic rocks as old as 35 million years, but remnants of the ancient arc’s internal plumbing system persist in the form of plutons, which are the crystallized magma chambers that once fed the early Cascade volcanoes. The greatest mass of exposed Cascade Arc plumbing is the Chilliwack batholith, which makes up much of the northern part of North Cascades National Park and adjacent parts of British Columbia beyond. Individual plutons range in age from about 35 million years old to 2.5 million years old. The older rocks invaded by all this magma were affected by the heat. Around the plutons of the batholith, the older rocks recrystallized. This contact metamorphism produced a fine mesh of interlocking crystals in the old rocks, generally strengthening them and making them more resistant to erosion. Where the recrystallization was intense, the rocks took on a new appearance dark, dense and hard. Many rugged peaks in the North Cascades owe their prominence to this baking. The rocks holding up many such North Cascade giants, as Mount Shuksan, Mount Redoubt, Mount Challenger, and Mount Hozomeen, are all partly recrystallized by plutons of the nearby and underlying Chilliwack batholith.
The Pemberton Volcanic Belt is an eroded volcanic belt north of the Garibaldi Volcanic Belt, which appears to have formed during the Miocene before fracturing of the northern end of the Juan de Fuca Plate. The Silverthrone Caldera is the only volcano within the belt that appears related to seismic activity since 1975.
The Garibaldi Volcanic Belt is the northern extension of the Cascade Arc. Volcanoes within the volcanic belt are mostly stratovolcanoes along with the rest of the arc, but also include calderas, cinder cones, and small isolated lava masses. The eruption styles within the belt range from effusive to explosive, with compositions from basalt to rhyolite. Due to repeated continental and alpine glaciations, many of the volcanic deposits in the belt reflect complex interactions between magma composition, topography, and changing ice configurations. Four volcanoes within the belt appear related to seismic activity since 1975, including: Mount Meager, Mount Garibaldi and Mount Cayley.
Mount Meager is the most unstable volcanic massif in Canada. It has dumped clay and rock several meters deep into the Pemberton Valley at least three times during the past 7,300 years. Recent drilling into the Pemberton Valley bed encountered remnants of a debris flow that had travelled 50 kilometers from the volcano shortly before it last erupted 2350 years ago. About 1,000,000,000 m³ of rock and sand extended over the width of the valley. Two previous debris flows, about 4,450 and 7,300 years ago, sent debris at least 32 kilometers from the volcano. Recently, the volcano has created smaller landslides about every ten years, including one in 1975 that killed four geologists near Meager Creek. The possibility of Mount Meager covering stable sections of the Pemberton Valley in a debris flow is estimated at about one in 2400 years. There is no sign of volcanic activity with these events. However scientists warn the volcano could release another massive debris flow over populated areas anytime without warning.
In the past, Mount Rainier has had large debris avalanches, and has also produced enormous lahars due to the large amount of glacial ice present. Its lahars have reached all the way to the Puget Sound. Around 5,000 years ago, a large chunk of the volcano slid away and that debris avalanche helped to produce the massive Osceola Mudflow, which went all the way to the site of present-day Tacoma and south Seattle. This massive avalanche of rock and ice took out the top 1,600 feet (500 m) of Rainier, bringing its height down to around 14,100 feet (4,300 m). About 530 to 550 years ago, the Electron Mudflow occurred, although this was not as large-scale as the Osceola Mudflow.
While the Cascade volcanic arc (a geological term) includes volcanoes such as Mount Meager and Mount Garibaldi, which lie north of the Fraser River, the Cascade Range (a geographic term) is considered to have its northern boundary at the Fraser.
Cascadia subduction zone
Area of the Cascadia subduction zone, including Cascade volcanoes (red triangles)
The Cascade Volcanoes were formed by the subduction of the Juan de Fuca, Explorer and the Gorda Plate (remnants of the much larger Farallon Plate) under the North American Plate along the Cascadia subduction zone. This is a 680 mi (1,094 km) long fault, running 50 mi (80 km) off the west-coast of the Pacific Northwest from northern California to Vancouver Island, British Columbia. The plates move at a relative rate of over 0.4 inches (10 mm) per year at a somewhat oblique angle to the subduction zone.
Because of the very large fault area, the Cascadia subduction zone can produce very large earthquakes, magnitude 9.0 or greater, if rupture occurred over its whole area. When the “locked” zone stores up energy for an earthquake, the “transition” zone, although somewhat plastic, can rupture. Thermal and deformation studies indicate that the locked zone is fully locked for 60 kilometers (about 40 miles) downdip from the deformation front. Further downdip, there is a transition from fully locked to aseismic sliding.
Plate tectonics of the Cascade Range
Unlike most subduction zones worldwide, there is no oceanic trench present along the continental margin in Cascadia. Instead, terranes and the accretionary wedge have been uplifted to form a series of coast ranges and exotic mountains. A high rate of sedimentation from the outflow of the three major rivers (Fraser River, Columbia River, and Klamath River) which cross the Cascade Range contributes to further obscuring the presence of a trench. However, in common with most other subduction zones, the outer margin is slowly being compressed, similar to a giant spring. When the stored energy is suddenly released by slippage across the fault at irregular intervals, the Cascadia subduction zone can create very large earthquakes such as the magnitude 9 Cascadia earthquake of 1700.
The Caribbean Plate is a mostly oceanic tectonic plate underlying Central America and the Caribbean Sea off the north coast of South America.
Roughly 3.2 million square kilometers (1.2 million square miles) in area, the Caribbean
Plate borders the North American Plate, the South American Plate, the Nazca Plate and the Cocos Plate. These borders are regions of intense seismic activity, including frequent earthquakes, occasional tsunamis, and volcanic eruptions.
Boundary types
Caribbean Plate.
The northern boundary with the North American plate is a transform or strike-slip boundary which runs from the border area of Belize, Guatemala (Motagua Fault), and Honduras in Central America, eastward through the Cayman trough on south of the southeast coast of Cuba, and just north of Hispaniola, Puerto Rico, and the Virgin Islands. Part of the Puerto Rico Trench, the deepest part of the Atlantic Ocean (roughly 8,400 meters), lies along this border. The Puerto Rico trench is at a complex transition from the subduction boundary to the south and the transform boundary to the west.
The eastern boundary is a subduction zone, the Lesser Antilles subduction zone, where oceanic crust of the South American Plate is being subducted under the Caribbean Plate. Subduction forms the volcanic islands of the Lesser Antilles Volcanic Arc from the Virgin Islands in the north to the islands off the coast of Venezuela in the south. This boundary contains seventeen active volcanoes, most notably Soufriere Hills on Montserrat;, Mount Pelée on Martinique; La Grande Soufrière on Guadeloupe; Soufrière Saint Vincent on Saint Vincent; and the submarine volcano Kick-’em-Jenny which lies about 10 km north of Grenada. Large historical earthquakes in 1839 and 1843 in this region are possibly megathrust earthquakes.
Along the geologically complex southern boundary, the Caribbean Plate interacts with the South American Plate forming Barbados, Trinidad and Tobago (all on the Caribbean Plate), and islands off the coast of Venezuela (including the Leeward Antilles) and Colombia. This boundary is in part the result of transform faulting along with thrust faulting and some subduction. The rich Venezuelan petroleum fields possibly result from this complex plate interaction.
The western portion of the plate is occupied by Central America. The Cocos Plate in the Pacific Ocean is subducted beneath the Caribbean Plate, just off the western coast of Central America. This subduction forms the volcanoes of Guatemala, El Salvador, Nicaragua, and Costa Rica, also known as the Central America Volcanic Arc.
Origin
There are two contending theories as to the origin of the Caribbean Plate.
One holds that it is a large igneous province that formed in the Pacific Ocean tens of millions of years ago. As the Atlantic Ocean widened, North America and South America were pushed westward, separated for a time by oceanic crust. The Pacific Ocean floor subducted under this oceanic crust between the continents. The Caribbean Plate drifted into the same area, but as it was less dense (although thicker) than the surrounding oceanic crust, it did not subduct, but rather overrode the ocean floor, continuing to move eastward relative to North America and South America. With the formation of the Isthmus of Panama 3 million years ago, it ultimately lost its connection to the Pacific.
A more recent theory asserts that the Caribbean Plate came into being from an Atlantic hotspot which no longer exists. This theory points to evidence of the absolute motion of the Caribbean Plate which indicates that it moves westward, not east, and that its apparent eastward motion is only relative to the motions of the North American Plate and the South American Plate.
The Alpine Fault is a geological fault, specifically a right-lateral strike-slip fault, that runs almost the entire length of New Zealand’s South Island. It forms a transform boundary between the Pacific Plate and the Indo-Australian Plate. Earthquakes along the fault, and the associated earth movements, have formed the Southern Alps. The uplift to the southeast of the fault is due to an element of convergence between the plates, meaning that the fault has a significant high-angle reverse oblique component to its displacement.Transform Boundary – Alpine Fault, South Island, New Zealand The Alpine Fault is a geological fault, specifically a right-lateral strike-slip fault, that runs almost the entire length of New Zealand’s South Island. It forms a transform boundary between the Pacific Plate and the Indo-Australian Plate. Earthquakes along the fault, and the associated earth movements, have formed the Southern Alps. The uplift to the southeast of the fault is due to an element of convergence between the plates, meaning that the fault has a significant high-angle reverse oblique component to its displacement.
The Alpine Fault is believed to align with the Macquarie Fault Zone in the Puysegur Trench off the southwestern corner of the South Island. From there, the Alpine Fault runs along the western edge of the Southern Alps, before splitting into a set of smaller dextral strike-slip faults north of Arthur’s Pass, known as the Marlborough Fault System. This set of faults, which includes the Wairau Fault, the Hope Fault, the Awatere Fault, and the Clarence Fault, transfer displacement between the Alpine Fault and the Hikurangi subduction zone to the north. The Hope fault is thought to represent the primary continuation of the Alpine fault.
Tectonic setting of New Zealand: astride a plate boundary which includes the Alpine Fault
New Zealand lies at the edge of both the Australian and Pacific tectonic plates. To the northeast of New Zealand, and underneath North Island, the Pacific Plate is moving towards, and being subducted below the Australian Plate. To the south of New Zealand, and underneath Fiordland, the two plates are also moving toward each other but here the Australian Plate is being subducted under the Pacific Plate.
The Australian and Pacific Plates generally don’t move smoothly past each other. They move in a series in a small rapid motions each of which is accompanied by one or more earthquakes.
Deep earthquakes under North Island form a well defined band (seismic zone) running northeast from Marlborough through White Island. Shallow earthquakes tend to occur to the southeast of this seismic zone, while the deeper ones occur towards the northwest. The earthquakes form this pattern occur where the Pacific Plate is being subducted under the Australian Plate. This pattern of deeper earthquakes towards the northwest of North Island reflects the northwest dip (or slope) of the boundary between the two plates (the Benioff zone).
Conversely, in the southwest of South Island where the Australian Plate is being subducted below the Pacific Plate, the deeper earthquakes occur on the southeast edge of the seismic zone where the Benioff zone dips steeply to the southeast.
Volcanoes
As the Pacific Plate is subducted below North Island, the part of the Australian Plate that makes up the central North Island is stretched and has, over many millions of years, become thinner than normal crust. Water released from the Pacific Plate deep under North Island combines with the hot rock of the Australian Plate at about 100km depth and causes a small amount of that rock to melt. This molten rock rises to the surface through the thinned crust and is either erupted from volcanoes like Ruapehu, Tongariro and Ngaruhoe or sits within the crust and heats it, and the water it contains, up causing geothermal activity around Taupo and Rotorua. The area of volcanic activity is referred to as the Taupo Volcanic Zone (see map above).
South Island Faults
The subduction zone in the north is linked to the subduction zone in the south by a series of very large faults that run through Marlborough (Marlborough Fault System) and down the west coast of South Island (Alpine Fault). The Marlborough Fault System is a series of subparallel strike-slip faults which run northeast-southwest. Relative movement across the Marlborough Fault System is dextral or right-lateral.
Note : The above story is reprinted from materials provided by Wikipedia & Department of Geology, University of Otago, New Zealand Plate Boundary By : USGS
The Kuril islands, extending from north to south for 1200 km, are a part of the submarine
Fig(1)
uplift located between the Sea of Okhotsk basin and the Kuril oceanic trench*. The archipelago comprises 30 large islands and numerous small ones. Two sectors, different in the history of development and morphology are distinguished within the archipelago (Luchitsky, 1974; Piskunov, 1987). The inner arc, known as the Greater Kuril,
extends from Shumshu island to Kunashir and the outer arc, termed the Lesser Kuril, which includes Shikotan and the small isles of the Habomai group (Figure1).
Tectonics and Environmental Change
Tectonically the Kurils belong to the Kuril-Kamchatka island arc which is related, as all island arcs, to an oceanic trench located 150-170 km from the volcanic front. Pronounced seismic activity is associated with the arc and the Benioff zone can be traced to a depth of 650 km (Tarakanov, 1972). The Greater Kurils and the Lesser Kurils differ in their morphology, geological structure, and history of development.
The Lesser Kurils, as well as the submarine Vityaz uplift to which they are connected and the peninsulas of eastern Kamchatka, are interpreted as an outer non-volcanic arc of the Kuril-Kamchatka system. The Lesser Kurils are formed mainly by late Cretaceous volcanic rocks. Volcanism of a submarine nature, as a result of which the islands emerged, was active in the Campanian (85-80 Ma BP) and the geological complex of this age is represented mainly by basalts. In the Maastrichtian (73-65 Ma BP), volcanic activity faded and flysh with olistostromes accumulated. Volcanic activity of the time was represented mainly by magmatic intrusions into sediments (Piskunov and Sergeev, 1992). At the end of the Cretaceous, volcanism occurred in terrestrial conditions. The completion of the magmatic activity was marked by gabbro intrusions. At present, there are no active volcanoes in the Lesser Kurils. The ancient calderas have been eroded and gentle hills with a height of 150-250 m dominate the islands.
The Greater Kurils are a younger formation where volcanism commenced at about 30 Ma BP in the late Oligocene-early Miocene. There were three major stages of arc development and these are reflected in the sequence of Cenozoic rocks (Fedorchenko et al., 1989; Piskunov and Sergeev, 1992). The most ancient rocks of the lower Miocene age comprise basalts, andesites, rhyolites, and their tuffs. The latter are abundant and can be correlated with the Green Tuff Formation of Japan. During the next stage in the middle Miocene, volcanism occurred mainly under terrestrial conditions and the stratigraphy is characterized by the occurrence of both volcanic rocks and flysh-type sequences.
Clastic material contains rocks which are not found in the Greater Kurils and which have apparently been derived from the dissected terrain in the back-arc area. The composition of these sequences shows that the Sea of Okhotsk basin did not exist at the time, while their inclined position reflects block rotation along faults during rifting and the opening of the Sea of Okhotsk basin at about 15 Ma BP (Zonenshain et al., 1990). The latest stage, during which the modern volcanic cones emerged, began in the late Miocene and is continuing at present. Its geology is a typical cal-calkaline volcanic sequence.
Similarly to Kamchatka, there were major periods of enhanced volcanic activity in the Kurils in the late Pleistocene and early Holocene (e.g., the Medeleev and Golovnin calderas formed 38-40 Ka BP). Over a hundred terrestrial volcanoes occur on the islands at present and 39 of them are active. The most active volcanoes are the tallest Kuril volcano, the Alaid (2339 m) located in the north of the arc and the Sarychev located on Matua island. The last powerful eruption of the Alaid occurred in 1972 when a new slag cone 150 m high formed in the centre of the volcano. The Sarychev is known for its regular activity. The most violent eruptions occurred in 1930 and 1946 when the ashfalls reached central Kamchatka. By contrast, another major volcano, the Golovnin caldera (the southernmost Kuril volcano located in Kunashir island) has not erupted for more than a century although it accommodates geothermal springs and two large lakes formed 640-680 years BP (Razjigaeva et al., 1998).
Typical of the Kurils is low to middle mountainous relief with altitudes of 500-1300 m. Five major morphological types of relief are distinguished: volcanic, seismo-tectonic, erosive-denudational, coastal (of abrasion and accumulation types), and aeolian (Grabkov and Isachenko, 1982). Aeolian forms date back to about 4.5-4.7 Ka BP when an extensive marine regression occurred (Bazarova et al., 1998). Most islands have volcanic relief and the landscape is that of individual volcanoes or volcanic ridges linked by sediment-filled isthmuses. Six to seven marine terraces occur in the coastal zone with altitudes ranging between 2-3 and 200-250 m a.s.l. Both marine terraces and volcanic massifs are strongly dissected which indicates a high rate of erosion and marine abrasion.
The landscapes of the Kuril islands were formed under the influence of two major factors: volcanism and seismic activity, and climate change. Climate is strongly influenced by the physical and chemical properties of the ocean, such as sea surface temperature and salinity, and variability in the paths of the oceanic currents may result in regional climatic change. Periodic changes in ocean circulation patterns due to changes in trade wind intensity in the eastern equatorial North Pacific Ocean and movements of the ocean plate have been discussed in relation to the warm Kuroshio current and climate change in Japan (Taira, 1980; Sawada and Handa, 1998). The islands of Japan and the Kurils are located in close proximity (as early as in the middle Holocene the islands of Hokkaido and Kunashir were connected by a landbridge) and climatic and environmental changes in northern Japan and the southern Kurils are closely correlated (Bazarova et al., 1998). However, the paleooceanography of the Kurils and its impact on the landscape development require further independent investigation.
*Kuril–Kamchatka Trench
The Kuril–Kamchatka Trench or Kuril Trench (Russian: Курило-Камчатский жёлоб) is an oceanic trench in the northwest Pacific Ocean. It lies off the southeast coast of Kamchatka and parallels the Kuril Island chain to meet the Japan Trench east of Hokkaido. It extends from a triple junction with the Ulakhan Fault and the Aleutian Trench near the Commander Islands, Russia, in the northeast, to the intersection with the Japan Trench in the southwest.
The trench formed as a result of the subduction zone, which formed in the late Cretaceous, that created the Kuril island arc as well as the Kamchatka volcanic arc. The Pacific Plate is being subducted beneath the Okhotsk Plate along the trench, resulting in intense volcanism.
Convergent Boundary – India and Asia – Himalaya Range
The geology of the Himalaya is a record of the most dramatic and visible creations of modern plate tectonic forces. The Himalayas, which stretch over 2400 km between the Namche Barwa syntaxis in Tibet and the Nanga Parbat syntaxis in Pakistan, are the result of an ongoing orogeny — the result of a collision between two continental tectonic plates. This immense mountain range was formed by tectonic forces and sculpted by weathering and erosion.
The Himalaya-Tibet region supplies freshwater for more than one-fifth of the world population, and accounts for a quarter of the global sedimentary budget. Topographically, the belt has many superlatives: the highest rate of uplift (nearly 10 mm/year at Nanga Parbat), the highest relief (8848 m at Mt. Everest Chomolangma), among the highest erosion rates at 2–12 mm/yr, the source of some of the greatest rivers and the highest concentration of glaciers outside of the polar regions. This last feature earned the Himalaya its name, originating from the Sanskrit for “the abode of the snow”.
The making of the Himalaya
During Late Precambrian and the Palaeozoic, the Indian sub-continent, bounded to the
Fig 1
north by the Cimmerian Superterranes, was part of Gondwana and was separated from Eurasia by the Paleo-Tethys Ocean (Fig. 1). During that period, the northern part of India was affected by a late phase of the Pan-African orogeny which is marked by an unconformity between Ordovician continental conglomerates and the underlying Cambrian marine sediments. Numerous granitic intrusions dated at around 500 Ma are also attributed to this event.
In the Early Carboniferous, an early stage of rifting developed between the Indian continent and the Cimmerian Superterranes. During the Early Permian, this rift developed into the Neotethys ocean (Fig. 2). From that time on, the Cimmerian Superterranes drifted away from Gondwana towards the north. Nowadays, Iran, Afghanistan and Tibet are partly made up of these terranes.
Fig 2
In the Norian (210 Ma), a major rifting episode split Gondwana in two parts. The Indian continent became part of East Gondwana, together with Australia and Antarctica. However, the separation of East and West Gondwana, together with the formation of oceanic crust, occurred later, in the Callovian (160-155 Ma). The Indian plate then broke off from Australia and Antarctica in the Early Cretaceous (130-125 Ma) with the opening of the “South Indian Ocean” (Fig. 3).
In the Upper Cretaceous (84 Ma), the Indian plate began its
Fig 3
very rapid northward drift covering a distance of about 6000 km, with the oceanic-oceanic subduction continuing until the final closure of the oceanic basin and the obduction of oceanic ophiolite onto India and the beginning of continent-continent tectonic interaction starting at about 65 Ma in the Central Himalaya. The change of the relative speed between the Indian and Asian plates from very fast (18-19.5 cm/yr) to fast (4.5 cm/yr) at about 55 Ma is circumstantial support for collision then. Since then there has been about 2500 km of crustal shortening and rotating of India by 45° counterclockwise in Northwestern Himalaya to 10°-15° counterclockwise in North Central Nepal relative to Asia (Fig. 4).
While most of the oceanic crust was “simply” subducted below the Tibetan block during the northward motion of India, at least three major mechanisms have been put forward, either separately or jointly, to explain what happened, since collision, to the 2500 km of “missing continental crust”. The first mechanism also calls upon the subduction of the Indian continental crust below Tibet. Second is the extrusion or escape tectonics mechanism (Molnar & Tapponnier 1975) which sees the Indian plate as an indenter that squeezed the Indochina block out of its way. The third proposed mechanism is that a large part (~1000 km (Dewey, Cande & Pitman 1989) or ~800 to ~1200 km) of the 2500 km of crustal shortening was accommodated by thrusting and folding of the sediments of the passive Indian margin together with the deformation of the Tibetan crust.
Even though it is more than reasonable to argue that this huge amount of crustal shortening most probably results from a combination of these three mechanisms, it is nevertheless the last mechanism which created the high topographic relief of the Himalaya.
Fig 4
Fig 1: The earth in the Early Permian. At that time, India is part of Gondwana and bordered to the north by the Cimmerian Superterrane. Paleogeographic reconstructions. By Dèzes (1999), based on Stampfli & Borel (2002) and Patriat & Achache (1984)
Fig 2: The earth at the Permian-Triassic boundary. The opening of the Neotethys separates the Cimmeridian Superterrane from Gondwana. Based on Stampfli & Borel (2002) and Patriat & Achache (1984)
Fig 3: The earth in the Cretaceous. The Cimmeridian Superterrane has accreted to Mega Laurasia, the oceanic crust of the Neotethys is subducted to the north along the Dras volcanic arc , the Shigatze Ocean opens as a consequence of back-arc spreading, India is separated from Africa and E. Gondwana and the Indian Ocean opens. Paleogeographic reconstructions based by Dèzes (1999), on Stampfli & Borel (2002) and Patriat & Achache (1984).
Fig 4: The northward drift of India from 71 Ma ago to present time. Note the simultaneous counter-clockwise rotation of India. Collision of the Indian continent with Eurasia occurred at about 55 Ma. Source: www.usgs.org (modified)
The Mid-Atlantic Ridge (MAR) is a mid-ocean ridge, a divergent tectonic plate boundary located along the floor of the Atlantic Ocean, and the longest mountain range in the world.
It separates the Eurasian Plate and North American Plate in the North Atlantic, and the African Plate from the South American Plate in theSouth Atlantic.
The Ridge extends from a junction with the Gakkel Ridge (Mid-Arctic Ridge) northeast of Greenland southward to the Bouvet Triple Junction in the South Atlantic. Although the Mid-Atlantic Ridge is mostly an underwater feature, portions of it have enough elevation to extend above sea level. The section of the ridge which includes the island of Iceland is also known as the Reykjanes Ridge. The average spreading rate for the ridge is about 2.5 cm per year.
Discovery
A ridge under the Atlantic Ocean was first inferred by Matthew Fontaine Maury in 1850. The ridge was discovered during the expedition of HMS Challenger in 1872. A team of scientists on board, led by Charles Wyville Thomson, discovered a large rise in the middle of the Atlantic while investigating the future location for a transatlantic telegraph cable. The existence of such a ridge was confirmed by sonar in 1925 and was found to extend around the Cape of Good Hope into the Indian Ocean by the German Meteor expedition.
In the 1950s, mapping of the Earth’s ocean floors by Bruce Heezen, Maurice Ewing, Marie Tharp and others revealed the Mid-Atlantic Ridge to have a strange bathymetry of valleys and ridges, with its central valley being seismologically active and the epicentre of many earthquakes. Ewing and Heezen discovered the ridge to be part of a 40,000-km-long essentially continuous system of mid-ocean ridges on the floors of all the Earth’s oceans. The discovery of this worldwide ridge system led to the theory of seafloor spreading and general acceptance of Wegener’s theory of continental drift and expansion as plate tectonics.
Geology
The ridge sits atop a geologic feature known as the Mid-Atlantic Rise which is a progressive bulge that runs the length of the Atlantic Ocean, with the ridge resting on the highest point of this linear bulge. This bulge is thought to be caused by upward convective forces in the asthenosphere pushing the oceanic crust and lithosphere.
This divergent boundary first formed in the Triassic period when a series of three-armed grabens coalesced on the supercontinent Pangaea to form the ridge. Usually only two arms of any given three-armed graben become part of a divergent plate boundary. The failed arms are called aulacogens, and the aulacogens of the Mid-Atlantic Ridge eventually became many of the large river valleys seen along the Americas and Africa (including the Mississippi River, Amazon River and Niger River).
The ridge is about 2,500 meters (8,200 ft) below sea level, while its flank is about 5,000 metres deeper.
The Fundy Basin on the Atlantic coast of North America between New Brunswick and Nova Scotia in Canada is evidence of the ancestral Mid-Atlantic Ridge.
Notable Features Along the Ridge
The Mid-Atlantic Ridge includes a deep rift valley which runs along the axis of the ridge along nearly its entire length. This rift marks the actual boundary between adjacent tectonic plates, where magma from the mantle reaches the seafloor, erupting as lava and producing new crustal material for the plates.
Near the equator, the Mid-Atlantic Ridge is divided into the North Atlantic Ridge and the South Atlantic Ridge by the Romanche Trench, a narrow submarine trench with a maximum depth of 7,758 m (25,453 ft), one of the deepest locations of the Atlantic Ocean. This trench, however, is not regarded as the boundary between the North and South American Plates, nor the Eurasian and African Plates.
Islands on the Mid-Atlantic Ridge
The islands, from north to south, with their respective highest peaks and location, are:
Northern Hemisphere (North Atlantic Ridge):
– Jan Mayen in the Arctic Ocean Iceland through which the ridge runs
– Azores (Ponta do Pico or Pico Alto, on Pico Island)
– Bermuda was formed on the ridge, but is now considerably west of it
– Saint Peter and Paul Rocks
Southern Hemisphere (South Atlantic Ridge):
– Ascension Island (The Peak, Green Mountain) Tristan da Cunha (Queen Mary’s Peak)
The Aleutian Trench (or Aleutian Trough) is a subduction zone and oceanic trench which runs along the southern coastline of Alaska and the adjacent waters of northeastern Siberia off the coast of Kamchatka Peninsula. It is classified as a “marginal trench” in the east as it runs along the margin of the continent.
The trench gives rise to the island arc Aleutian Islands where it runs through the open sea. The trench extends for 3,400 km from a triple junction in the west with the Ulakhan Fault and the northern end of the Kuril-Kamchatka Trench, to a junction with the northern end of the Queen Charlotte Fault system in the east. The Aleutian Trench is a convergent plate boundary. The trench forms part of the boundary between two tectonic plates. Here, the Pacific Plate is being subducted under the North American Plate at an angle of nearly 45 degrees. The rate of closure is 3in. (8 cm) per year.
The Aleutian Islands are a chain of 14 large volcanic islands and 55 smaller ones, forming part of the Aleutian Arc in the Northern Pacific Ocean, occupying an area of 6,821 sq mi (17,666 km²) and extending about 1,200 mi (1,900 km) westward from the Alaska Peninsula toward the Kamchatka Peninsula, marking a line between the Bering Sea and the Pacific Ocean. Crossing longitude 180°, they are the westernmost part of the United States . Nearly all the archipelago is part of Alaska and usually considered as being in the “Alaskan Bush”, but at the extreme western end the small, geologically related, and remote Commander Islands are in Russia. The islands, with their 57 volcanoes, are in the northern part of the Pacific Ring of Fire. The Alaska Marine Highway (a ferry service) passes through the islands.
The north side of the trench slopes 3°–4° and the south side l°–4°. This process has created the Aleutian Arc. The deepest part of the Aleutian trench has been measured at 7,822 metres (25,663 ft) at 51.21°N, 174.83°E., located about 145 km SSW of Buldir Island. North of the trench, a string of volcanoes and associated islands have formed where melting of the crust has been caused by the descending plate beneath them. Center pressure: 10762psi (732atm), 74 MPa (732atm) Metric units.[ Variations in total magnetic intensity (residual) of more than 600 γ were found in the center of the trench and more than 1100 γ on the southern flank.
More Information About : Plate Tectonics Map Plate Boundary Map Note : The above story is reprinted from materials provided by Wikipedia Plate Boundary By : USGS
The Red Sea was formed by Arabia being split from Africa by movement of the Red Sea Rift. This split started in the Eocene and accelerated during the Oligocene. The sea is still widening, and it is considered that it will become an ocean in time (as proposed in the model of John Tuzo Wilson). In 1949, a deep water survey reported anomalously hot brines in the central portion of the Red Sea. Later work in the 1960s confirmed the presence of hot, 60 °C (140 °F), saline brines and associated metalliferous muds. The hot solutions were emanating from an active subseafloor rift. The high salinity of the waters was not hospitable to living organisms.
Sometimes during the Tertiary period the Bab el Mandeb closed and the Red Sea evaporated to an empty, hot, dry salt-floored sink. Effects causing this would have been:
A “race” between the Red Sea widening and Perim Island erupting filling the Bab el Mandeb with lava.
The lowering of world sea level during the Ice Ages because of much water being locked up in the ice caps.
A number of volcanic islands rise from the center of the sea. Most are dormant, but in 2007 Jabal al-Tair island, in the Bab el Mandeb strait, erupted violently. An eruption among the nearby Zubair islands followed in 2011.
Mineral resources
In terms of mineral resources the major constituents of the Red Sea sediments are as follows:
A schematic cross section of the Earth’s interior below oceanic ridges shows the conditions of magma generation. Through experimentation on mantle rocks, Rice University researchers found evidence that magma forms as deep as 250 kilometers inside the Earth’s, much deeper than previously thought. Such melting would help explain apparent geophysical and geochemical contradictions that have puzzled geologists for years. (Credit: Graphic by Dasgupta Group)
Magma forms far deeper than geologists previously thought, according to new research at Rice University.
A group led by geologist Rajdeep Dasgupta put very small samples of peridotite under very large pressures in a Rice laboratory to determine that rock can and does liquify, at least in small amounts, as deep as 250 kilometers in the mantle beneath the ocean floor. He said this explains several puzzles that have bothered scientists.
Dasgupta is lead author of the paper to be published this week in Nature.
The mantle is the planet’s middle layer, a buffer of rock between the crust — the top 5 miles or so — and the core. If one could compress millions of years of observation down to minutes, the mantle would look like a rolling mass of rising and falling material. This slow but constant convection brings materials from deep within the planet to the surface — and occasionally higher through volcanoes.
The Rice team focused on mantle beneath the ocean because that’s where the crust is created and, Dasgupta said, “the connection between the interior and surface world is established.” Silicate melts — aka magma — rise with the convective currents, cool and spread out to form the ocean crust. The starting point for melting has long been thought to be at 70 kilometers beneath the seafloor.
That has confounded geologists who suspected but could not demonstrate the existence of deeper silicate magma, said Dasgupta, an assistant professor of Earth science at Rice.
Scientists determine the mantle’s density by measuring the speed of a seismic wave after an earthquake, from its origin to other points on the planet. These waves travel faster through solids than liquids, and geologists have been surprised to detect waves slowing down through what should be the mantle’s express lane. “Seismologists have observed anomalies in their velocity data as deep as 200 kilometers beneath the ocean floor,” Dasgupta said. “Based on our work, we show that trace amounts of magma are generated at this depth, which would potentially explain that.”
The research also offers clues to the bulk electrical conductivity of the oceanic mantle, he said. “The magma at such depths has a high enough amount of dissolved carbon dioxide that its conductivity is very high,” Dasgupta said. “As a consequence, we can explain the conductivity of the mantle, which we knew was very high but always struggled to explain.”
Because humans have not yet dug deep enough to sample the mantle directly — though some are trying — researchers have to extrapolate data on rocks carried up to the surface. A previous study by Dasgupta determined that melting in Earth’s deep upper mantle is caused by the presence of carbon dioxide. The present study shows that carbon not only leads the charge to make carbonate fluid but also helps to make silicate magma at significant depths.
The researchers also found carbonated rock melts at significantly lower temperatures than non-carbonated rock. “This deep melting makes the silicate differentiation of the planet much more efficient than previously thought,” Dasgupta said. “Not only that, this deep magma is the main agent to bring all the key ingredients for life — water and carbon — to the surface of the Earth.”
In Dasgupta’s high-pressure lab at Rice, volcanic rocks are windows to the planet’s interior. The researchers crushed tiny rock samples that contain carbon dioxide to find out how deep magma forms.
“Our field of research is called experimental petrology,” he said. “We have all the necessary tools to simulate very high pressures (up to nearly 750,000 pounds per square inch for these experiments) and temperatures. We can subject small amounts of rock samples to these conditions and see what happens.”
They use powerful hydraulic presses to partially melt “rocks of interest” that contain tiny amounts of carbon to simulate what they believe is happening under equivalent pressures in the mantle. “When rocks come from deep in the mantle to shallower depths, they cross a certain boundary called the solidus, where rocks begin to undergo partial melting and produce magmas,” Dasgupta said.
“Scientists knew the effect of a trace amount of carbon dioxide or water would be to lower this boundary, but our new estimation made it 150-180 kilometers deeper from the known depth of 70 kilometers,” he said.
“What we are now saying is that with just a trace of carbon dioxide in the mantle, melting can begin as deep as around 200 kilometers. And when we incorporate the effect of trace water, the magma generation depth becomes at least 250 kilometers. This does not generate a large amount, but we show the extent of magma generation is larger than previously thought and, as a consequence, it has the capacity to affect geophysical and geochemical properties of the planet as a whole.”
Co-authors of the paper are Rice graduate student Ananya Mallik and postdoctoral researcher Kyusei Tsuno; Research Professor Anthony Withers and Marc Hirschmann, the George and Orpha Gibson Chair of Earth and Planetary Sciences, at the University of Minnesota, and Greg Hirth, a professor of geological sciences at Brown University.
The study was supported by the National Science Foundation and a Packard Fellowship to Dasgupta.
Note : The above story is reprinted from materials provided by Rice University. The original article was written by Mike Williams.
A Simple Wilson Cycle The Opening and Closing of An Ocean Basin
Wilson cycle
The cyclical opening and closing of ocean basins caused by movement of the Earth’s plates. The Wilson cycle begins with a rising plume of magma and the thinning of the overlying crust. As the crust continues to thin due to extensional tectonic forces, an ocean basin forms and sediments accumulate along its margins. Subsequently subduction is initiated on one of the ocean basin’s margins and the ocean basin closes up. When the crust begins to thin again, another cycle begins. The Wilson cycle is named after the Canadian geophysicist J. Tuzo Wilson (1908-1993).
The Wilson cycle begins in
Stage A with a stable continental craton. A hot spot (not present in the drawings) rises up under the craton, heating it, causing it to swell upward, stretch and thin like taffy, crack, and finally split into two pieces. This process not only splits a continent in two it also creates a new divergent plate boundary.
Stage B – the one continent has been separated into two continents, east and west, and a new ocean basin (the ophiolite suite) is generated between them. The ocean basin in this stage is comparable to the Red Sea today. As the ocean basin widens the stretched and thinned edges where the two continents used to be joined cool, become denser, and sink below sea level. Wedges of divergent continental margins sediments accumulate on both new continental edges.
Stage C – the ocean basin widens, sometimes to thousands of miles; this is comparable to the Atlantic ocean today. As long as the ocean basin is opening we are still in the opening phase of the Wilson cycle.
Stage D – the closing phase of the Wilson Cycle begins when a subduction zone (new convergent plate boundary) forms. The subduction zone may form anywhere in the ocean basin, and may face in any direction. In this model we take the simplest situation; a subduction zone developing under the edge of one continent. Once the subduction zone is active the ocean basin is doomed; it will all eventually subduct and disappear. These are remnant ocean basins.
Stage E – most of the remnant ocean basin has subducted and the two continents are about to collide. Subduction under the edge of a continent has a lot of results. Deep in the subduction zone igneous magma is generated and rises to the surface to form volcanoes, that build into a cordilleran mountain range (e.g. the Cascade mountains of Washington, Oregon, and northern California.) Also, a lot of metamorphism occurs and folding and faulting.
Stage F – the two continents, separated in Stages A and B now collide. The remnant ocean basin is completely subducted. Technically the closing phase of the Wilson cycle is over. Because the subduction zone acts as a ramp the continent with the subduction zone (a hinterland) slides up over the edge of the continent without out it (a foreland).
Stage G – once the collision has occurred the only thing left for the mountain to do is erode down to sea level – a peneplain. The stage G drawing is a distortion, however. With the collision the continental thickness doubles, and since continental rock is light weight, both will rise as the mountain erodes, much like a boat rises when cargo is taken off of it. Thus, in reality, most of the hinterland continent will be eroded away, and the foreland continent will eventually get back to the earth’s surface again.
Note : The above story is reprinted from materials provided by James Madison University
Though churning smokestacks, cud-chewing cows and gasoline-burning vehicles are contributing constantly to greenhouse gas emissions, there are also many processes that do the reverse, pulling molecules like carbon dioxide out of the atmosphere. One of these is chemical weathering, which occurs when rock turns into soil. Carbon dioxide molecules and rain combine to dissolve rock, and the weathering products, including sediment, eventually make their way through waterways to the ocean where some become trapped on the ocean bottom and in coral reefs and seashells.
For years, geologists believed that mountains, due to their steep slopes and high rates of erosion, were large contributors to this “carbon draw down” effect. But a new study led by the University of Pennsylvania’s Jane Willenbring suggests that mountains do not play a significant role in this activity, turning a geological paradigm on its head.
Willenbring, an assistant professor in the Department of Earth and Environmental Science, led the research, working with Alexandru Codilean of the GFZ German Research Center for Geosciences and Brandon McElroy of the University of Wyoming.
“High mountains have been the go-to field area for people interested in studying how much sediment goes into the ocean and how tectonics perturbs global climate,” Willenbring said. “But what we found was that mountains contribute only a small amount of the total sediment produced on Earth.”
This finding, published in the journal Geology, directly challenges previous studies, which suggested that small mountain rivers contributed most of the sediment to the world’s oceans.
What these other scientists neglected to account for, according to Willenbring, was that even the steepest, most erosion- and weathering-prone slopes take up only a tiny fraction of Earth’s surface. So while these steep protrusions have very high rates of carbon absorption per unit area, they are far outstripped by the much more abundant expanses of gently sloping land.
“These small mountain streams are packing a big punch for their size,” Willenbring said. “But even though they have a lot of erosion going on, the amount of the Earth covered by mountain ranges is too small to produce the amount of sediment that less steeply sloped areas produce.”
The previous studies lacked access to a new investigative technique that was developed relatively recently. The method involves an examination of cosmogenic nuclides, which are rare forms of chemical elements produced only when supernovas explode, sending high-energy radiation to Earth and breaking up other atoms. Counting these chemical isotopes allows researchers to determine how long sediment has remained in a particular watershed over long time periods.
In contrast, techniques used previously, which involve physically measuring sediment flow in rivers and streams, only capture a snapshot of sediment erosion and deposition rates over a short time frame.
The researchers analyzed published data on cosmogenic nuclide concentrations from around the world to determine the levels of sediment flux over a time frame of thousands to hundreds of thousands of years. They also gathered topographical data to determine the slopes of the surrounding areas. They then extrapolated these rates of sediment deposition to the whole Earth’s surface.
“What the cosmogenic nuclides tell us is that chemical weathering still happens in these low sloping areas,” Willenbring said.
Other scientists had believed these gently rolling or flat areas, such as floodplains, to be “trappers” of sediment, but the research team’s analysis demonstrated that, despite being areas of net deposition, they are in fact still drawing large amounts of carbon dioxide from the atmosphere.
Given these findings, geologists interested in understanding the contribution of erosion to climate fluctuations may want to spend less time on mountaintops and more time in big, lower-lying rivers like the Mississippi and the Amazon, Willenbring said.
“We’re going to need to start studying ‘boring’ rivers if we’re going to understand carbon and sediment cycling.”
Note : The above story is reprinted from materials provided by University of Pennsylvania.
Basalt. (Credit: Courtesy of the U.S. Forest Service)
Oceanic crust covers two-thirds of Earth’s solid surface, but scientists still don’t entirely understand the process by which it is made. Analysis of more than 600 samples of oceanic crust by a team including Carnegie’s Frances Jenner reveals a systemic pattern that alters long-held beliefs about how this process works, explaining a crucial step in understanding Earth’s geological deep processes.
Their work is published in Nature on November 29.
Magmas generated by melting of Earth’s mantle rise up below the oceanic crust and erupt on Earth’s surface at mid-ocean ridge systems, the longest mountain ranges in the world. When the magma cools it forms basalt, the planet’s most-common rock and the basis for oceanic crust.
It has long been assumed that the composition of magmas erupting out of mid-ocean ridges is altered when minerals that form during cooling sink out of the remaining liquid, a process called fractional crystallization. In theory, trace elements that are not included in the crystallizing minerals should be little affected by this process, and their ratios should be the same in the erupting magma as they were in the original magma before cooling. If this is true, trace element ratios in magmas erupting at mid-ocean ridges should represent those of the original parental magma that formed deep in Earth’s mantle. However, this process doesn’t account for the high abundance of trace elements found in samples of basalt from mid-ocean ridges around the world, so the reality of the situation is obviously more complicated than previous theories indicated.
Using the extensive array of samples and advanced modeling, Jenner and her research partner Hugh O’Neill of the Australian National University demonstrated that the concentration of trace elements is due to the process by which the magma is cycled through the oceanic crust prior to being erupted on the sea floor at the mid-ocean ridges.
Magma collects under Earth’s surface in a pool of liquid rock called a magma chamber. Each chamber is frequently flushed with new magma, which mixes with the old magma that was already there, and then this blended magma erupts out onto the ocean floor. Following the influx of new magma and eruption, the remaining magma undergoes fractional crystallization. This means that minerals are separated out from the magma as it cools. However, these minerals contain only minor amounts of the trace elements. As a result, trace elements build up in the magma over time, as the magma chamber is continually replenished by new magma coming in to the system. “It’s a simple idea, but it fits remarkably well,” Jenner said. “These new findings will permit us to explore the conditions of mantle melting and production of the Earth’s most-common rock.”.
Note : The above story is reprinted from materials provided by Carnegie Institution.
Formula: Bi System: Trigonal Lustre: Metallic Hardness: 2 – 2½ Locality: Schneeberg District, Erzgebirge, Saxony, Germany. Name Origin: Probably from the Arabic bi ismid, meaning having the properties of antimony.
Bismuth is a chemical element with the symbol Bi and atomic number 83. Bismuth, a pentavalent post-transition metal and one of the pnictogens, chemically resembles its lighter homologs arsenic and antimony. Elemental bismuth may occur naturally, although its sulfide and oxide form important commercial ores. The free element is 86% as dense as lead. It is a brittle metal with a silvery white color when freshly produced, but surface oxidation can give it a pink tinge. Bismuth is the most naturally diamagnetic element, and has one of the lowest values of thermal conductivity among metals.
Bismuth metal has been known since ancient times, although it was often confused with lead and tin, which share some physical properties. The etymology is uncertain, but possibly comes from Arabic bi ismid, meaning having the properties of antimony or the German words weiße Masse or Wismuth (“white mass”), translated in the mid-sixteenth century to New Latin bisemutum.
Bismuth was long considered the element with the highest atomic mass that is stable. However, in 2003 it was discovered to be weakly radioactive: its only primordial isotope, bismuth-209, decays via alpha decay with a half life more than a billion times the estimated age of the universe. Because of its tremendously long half-life, bismuth may still be considered stable for almost all purposes.
Physical Properties of Bismuth
Cleavage: {0001} Perfect Color: Silver white, Pinkish white, Red. Density: 9.7 – 9.8, Average = 9.75 Diaphaneity: Opaque Fracture: Uneven – Flat surfaces (not cleavage) fractured in an uneven pattern. Hardness: 2-2.5 – Gypsum-Finger Nail Luminescence: Non-fluorescent. Luster: Metallic Magnetism: Nonmagnetic Streak: silver white
Scientists probe Canadian sulfide ore to confirm microbial activity in seawater 2.7 billion years ago. (Credit: Image courtesy of McGill University)
An analysis of sulfide ore deposits from one of the world’s richest base-metal mines confirms that oxygen levels were extremely low on Earth 2.7 billion years ago, but also shows that microbes were actively feeding on sulfate in the ocean and influencing seawater chemistry during that geological time period.
The research, reported by a team of Canadian and U.S. scientists in Nature Geoscience, provides new insight into how ancient metal-ore deposits can be used to better understand the chemistry of the ancient oceans — and the early evolution of life.
Sulfate is the second most abundant dissolved ion in the oceans today. It comes from the “rusting” of rocks by atmospheric oxygen, which creates sulfate through chemical reactions with pyrite, the iron sulfide material known as “fool’s gold.”
The researchers, led by PhD student John Jamieson of the University of Ottawa and Prof. Boswell Wing of McGill, measured the “weight” of sulfur in samples of massive sulfide ore from the Kidd Creek copper-zinc mine in Timmins, Ontario, using a highly sensitive instrument known as a mass spectrometer. The weight is determined by the different amounts of isotopes of sulfur in a sample, and the abundance of different isotopes indicates how much seawater sulfate was incorporated into the massive sulfide ore that formed at the bottom of ancient oceans. That ancient ore is now found on Earth’s surface, and is particularly common in the Canadian shield.
The scientists found that much less sulfate was incorporated into the 2.7 billion-year-old ore at Kidd Creek than is incorporated into similar ore forming at the bottom of oceans today. From these measurements, the researchers were able to model how much sulfate must have been present in the ancient seawater. Their conclusion: sulfate levels were about 350 times lower than in today’s ocean. Though they were extremely low, sulfate levels in the ancient ocean still supported an active global population of microbes that use sulfate to gain energy from organic carbon.
“The sulfide ore deposits that we looked at are widespread on Earth, with Canada and Quebec holding the majority of them,” says Wing, an associate professor in McGill’s Department of Earth and Planetary Science. “We now have a tool for probing when and where these microbes actually came into global prominence.”
“Deep within a copper-zinc mine in northern Ontario that was once a volcanically active ancient seafloor may not be the most intuitive place one would think to look for clues into the conditions in which the earliest microbes thrived over 2.7 billion years ago,” Jamieson adds. “However, our increasing understanding of these ancient environments and our abilities to analyze samples to a very high precision has opened the door to further our understanding of the conditions under which life evolved.”
The other members of the research team were Prof. James Farquhar of the University of Maryland and Prof. Mark D. Hannington of the University of Ottawa.
The Natural Sciences and Engineering Research Council of Canada made this study possible through fellowships to Jamieson and a Discovery grant to Wing.
Note : The above story is reprinted from materials provided by McGill University.
Geology professor Qing-zhu Yin holds a fragment of the meteorite that exploded over the Sierra foothills this past spring. (Credit: Gregory Urquiaga/UC Davis photo)
A meteorite that exploded as a fireball over California’s Sierra foothills this past spring was among the fastest, rarest meteorites known to have hit Earth, and it traveled a highly eccentric orbital route to get here.
An international team of scientists presents these and other findings in a study published Dec. 21, in the journal Science. The 70-member team included nine researchers from UC Davis, along with scientists from the SETI Institute, NASA and other institutions.
The researchers found that the meteorite that fell over Northern California on April 22 was the rarest type known to have hit Earth — a carbonaceous chondrite. It is composed of cosmic dust and presolar materials that helped form the planets of the solar system.
The scientists learned that the meteorite formed about 4.5 billion years ago. It was knocked off its parent body, which may have been an asteroid or a Jupiter-family comet, roughly 50,000 years ago. That began its journey to Sutter’s Mill, the gold discovery site that sparked the California Gold Rush.
As it flew toward Earth, it traveled an eccentric course through the solar system, flying from an orbit close to Jupiter toward the sun, passing by Mercury and Venus, and then flying out to hit Earth.
The high-speed, minivan-sized meteorite entered the atmosphere at about 64,000 miles per hour. The study said it was the fastest, “most energetic” reported meteorite that’s fallen since 2008, when an asteroid fell over Sudan.
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“If this were a much bigger object, it could have been a disaster,” said co-author and UC Davis geology professor Qing-zhu Yin. “This is a happy story in this case. ”
Before entering Earth’s atmosphere, the meteorite is estimated to have weighed roughly 100,000 pounds. Most of that mass burned away when the meteorite exploded. Scientists and private collectors have recovered about 2 pounds remaining.
UC Davis is 60 miles west of the El Dorado county towns of Coloma and Lotus, where pieces of the meteorite were found on residents’ driveways and in local forests and parks.
When the meteorite fell, Yin, whose lab contains some of the country’s most specialized equipment to measure the age and composition of meteorites, searched for and collected pieces of the fallen meteorite with students and volunteers. He also led a 35-member subgroup of international researchers to study and share information about the meteorite’s mineralogy, internal textures, chemical and isotopic compositions and magnetic properties.
Meteorites like Sutter’s Mill are thought to have delivered oceans of water to Earth early in its history. Using neutron-computed tomography, UC Davis researchers helped identify where hydrogen, and therefore water-rich fragments, resides in the meteorite without breaking it open.
For the first time, the Doppler weather radar network helped track the falling carbonaceous chondrite meteorite pieces, aiding scientists in the quick recovery of them, the study reports. Yin expects that the weather radar data in the public domain could greatly enhance and benefit future meteorite recoveries on land.
“For me, the fun of this scientific gold rush is really just beginning,” said Yin. “This first report based on the initial findings provides a platform to propel us into more detailed research. Scientists are still finding new and exciting things in Murchison, a similar type of meteorite to Sutter’s Mill, which fell in Victoria, Australia, in 1969, the same year Apollo astronauts Neil Armstrong and Buzz Aldrin returned the first lunar samples to the Earth. We will learn a lot more with Sutter’s Mill.”
Note : The above story is reprinted from materials provided by University of California – Davis.
Debris flow channel with deposits left after 2010 storms in Ladakh, NW Indian Himalaya. Note coarse bouldery levees on both sides of the channel, and poorly sorted rocks on the channel floor.
Debris flows are fast moving, liquefied landslides of mixed and unconsolidated water and debris that look like flowing concrete. They are defined by their non-newtonian flow dynamics, and behave as Bingham plastics. This characteristic can lead to the formation of levees at the margins of unconstrained debris flows as the margins of the flow freeze.
They are differentiated from mudflows by their coarser and more poorly sorted sediment load. Flows can carry material ranging in size from clay to boulders, and may contain a large amount of woody debris such as logs and tree stumps. Flows can be triggered by intense rainfall, glacial melt, or a combination of the two. Speed of debris flows can vary from 5 km/h to up to 80 km/h in extreme cases.
Volumes of material delivered by single events vary from less than 100 to more than 100,000 cubic metres. Variables considered important in debris flow initiation include slope angle, available loose sediment, and degree of land disturbance by activities such as forest harvesting.
Debris flows are often more frequent following forest and brush fires, as experience in southern California clearly demonstrates. Debris flows are extremely destructive to life and property, and claim thousands of lives world-wide in any given year.
They are a particular problem in steep mountainous areas subjected to intense rainstorms, and have received particular attention from researchers in Japan, Western USA, Western Canada, New Zealand, the European Alps, and Kazakhstan.
Features and behavior
Debris flows generally form when unconsolidated material becomes saturated and unstable, either on a hillslope or in a stream channel.
Flows are accelerated downhill by gravity and tend to follow steep mountain channels. The front, or ‘head’ of debris flow often contains a great deal of coarser material such as boulders and logs. Trailing behind this frontal lobe is the less viscous, main part of the flow that contains sand, silt and clay.
Debris flows eventually become ‘thinner’, or less viscous, muddy flood waters as they deposit their coarser components in areas of reduced gradient. Debris flows tend to move in pulses, or discrete surges, as friction or other barriers are overcome during the flow. Sometimes earlier pulses or previous debris flow deposits form levees which confine the flow until they are breached by later, larger flows.
The presence of older levees (a.k.a. lateral deposits) provides some idea of the magnitudes of previous debris flows in a particular area, and through dating of trees growing on such deposits, may indicate the approximate frequency of destructive debris flows.
This is important information for land development in areas where debris flows deposit material, known as debris fans and alluvial fans. The big debris flow or landslide is called yamatsunami (山津波), literally mountain tsunami in Japan.
Types
Other geological flows can also be described as debris flows, though are typically given more specific names. These include:
Lahar
A lahar is a debris flow related in some way to volcanic activity, either directly as a result of an eruption, or indirectly by the collapse of loose material from the flanks of a volcano. A variety of factors may trigger a lahar, including melting of glacial ice due to volcanic activity or climate change, intense rainfall on loose pyroclastic material, or the out bursting of a lake that was previously dammed by pyroclastic or glacial material. The word lahar is of Indonesian origin, but is now routinely used by geologists world-wide to describe volcanogenic debris flows.
Jökulhlaup
A jökulhlaup is a debris flow that originates from a glacial outburst flood. Jökulhlaup is an Icelandic word which refers specifically to floods having a glacial trigger. In the case of Iceland, many such floods are triggered by sub-glacial volcanic eruptions, since Iceland sits atop the Mid-Atlantic Ridge. Elsewhere, a more common cause of jökulhlaups is the breaching of ice-dammed or moraine-dammed lakes. Such breaching events are often caused by the sudden calving of glacier ice into a lake, which then causes a displacement wave to breach a moraine or ice dam. Downvalley of the breach point, a jökulhlaup may increase greatly in size through entrainment of loose sediment and water from the valley through which it travels. Travel distances may exceed 100 km.
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Debris flow channel in Ladakh, NW Indian Himalaya, produced in the storms of August 2010. Note coarse, bouldery levees on both sides of the channel, high abundance of mud, and poorly sorted sediments, DanHobleyTertiary debris flow deposit, Resting Springs Pass, California.Almaty, Kazakhstan, after the catastrophic debris flow of 1921. A number of facilities, including the Medeu Dam, have been built since to prevent flows of this kind from reaching the cityDebris flow scars formed in 1968-1969 in greater Los Angeles. The image taken months after the debris flows occurred. Daniel Collins
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Dickinsonia fossils in South Australia, shown here, were likely formed by lichen or other microbial consortia, not from marine invertebrates or giant protists as previously theorized. (Credit: Courtesy of Greg Retallack)
fossils long thought to be ancestors of early marine life are remnants of land-dwelling lichen or other microbial colonies, says University of Oregon scientist Gregory J. Retallack, who has been studying fossil soils of South Australia.
Ediacaran (pronounced EDI-akran) fossils date to 542-635 million years ago. They’ve been considered fossil jellyfish, worms and sea pens, but are preserved in ways distinct from marine invertebrate fossils. The fossils — first discovered in 1946 in Australia’s Ediacara Hills — are found in iron-colored impressions similar to plant fossils and microbes in fossil soils.
Retallack, a native of Australia, examined ancient Ediacaran soils with an array of state-of-the-art chemical and microscopic techniques, including an electron microprobe and scanning electron microscope in the UO’s CAMCOR Microanalytical Facility headed by John Donovan and rock-analysis technology in the UO’s stable isotope laboratory of Ilya Bindeman.
The soils with fossils, Retallack writes in his study, “are distinguished by a surface called ‘old elephant skin,’ which is best preserved under covering sandstone beds.” The healed cracks and lumpy appearance of sandy “old elephant skin” are most like the surface of microbial soil crusts in modern deserts.
“This discovery has implications for the tree of life, because it removes Ediacaran fossils from the ancestry of animals,” said Retallack, professor of geological sciences and co-director of paleontological collections at the UO’s Museum of Natural and Cultural History. His evidence, mostly gathered from a site in the Flinders Ranges, is presented in a paper placed online ahead of print by the journal Nature.
These fossils have been a first-class scientific mystery,” he said. “They are the oldest large multicellular fossils. They lived immediately before the Cambrian evolutionary explosion that gave rise to familiar modern groups of animals.”
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Retallack studied numerous Ediacaran fossils and determined that the diversity reflects a preference by the ancient organisms for “unfrozen, low salinity soils, rich in nutrients, like most terrestrial organisms.” Thus the fossils in Australia’s iconic red-rock ranges, he concludes, were landlubbers. In his closing paragraph, Retallack outlines implications for a variety of other Edicaran fossils, that could have been lichens, other microbial consortia, fungal fruiting bodies, slime molds, flanged pedestals of biological soil crusts, and even casts of needle ice.
Ediacaran fossils, he said, represent “an independent evolutionary radiation of life on land that preceded by at least 20 million years the Cambrian evolutionary explosion of animals in the sea.” Increased chemical weathering by large organisms on land may have been needed to fuel the demand of nutrient elements by Cambrian animals. Independent discoveries of Cambrian fossils comparable with Ediacaran ones is evidence, he said, that even in the Cambrian, more than 500 million years ago, life on land may have been larger and more complex than life in the sea.
Retallack leaves open the possibility that some Ediacaran fossils found elsewhere in the world may not be land-based in origin, writing in his conclusion that the many different kinds of these fossils need to be tested and re-evaluated.
“The key evidence for this new view is that the beds immediately below the cover sandstones in which they are preserved were fossil soils,” he said. “In other words the fossils were covered by sand in life position at the top of the soils in which they grew. In addition, frost features and chemical composition of the fossil soils are evidence that they grew in cold dry soils, like lichens in tundra today, rather than in tropical marine lagoons.”
Fossil soils are usually recognized from root traces, soil horizons and soil structures, but in rocks of Ediacaran age, before the advent of rooted plants, only the second two criteria can be used to recognize fossil soils. Ediacaran fossil soils, Retallack said, represent ecosystems less effective at weathering than the modern array of ecosystems, so that soil horizons and soil structures are not as well developed as they are in modern soils.
“The research conducted by Dr. Retallack helps to unravel the mystery of very ancient life on Earth,” said Kimberly Andrews Espy, UO vice president for research and innovation, and dean of the graduate school. “It also serves as an example of how technology, some of it developed at the University of Oregon, can be used to analyze materials from anywhere in the world.”
The American Chemical Society’s Petroleum Research Fund supported the fieldwork.
Note : The above story is reprinted from materials provided by University of Oregon.
Ol Doinyo Lengai is an active volcano located in the north of Tanzania and is part of the volcanic system of the East African Rift. It is located in the eastern Rift Valley, or Gregory Rift, south of both Lake Natron and Kenya. It is unique among active volcanoes in that it produces natrocarbonatite lava, a unique occurrence of volcanic carbonatite. Further, the temperature of its lava as it emerges is only around 510 °C (950 °F). A few older extinct carbonatite volcanoes are located nearby, including Homa Mountain.
The volcano has immense ecological, geological and cultural value. The Engaresero village located on the Western shores of Lake Natron, close to Ol Doinyo Lengai, has been chosen by the government of Tanzania to exemplify the Maasai pastoral system given its singularity, integrity, high diversity of habitats and biodiversity. The community has demonstrated a strong resilience in facing threats to their systems, and has maintained associated social and cultural institutions, which ensure its sustainability under prevailing environmental conditions.
Geology
“Ol Doinyo Lengai” means “The Mountain of God” in the Maasai language of the native people. The record of eruptions on the mountain dates to 1883, and flows were also recorded between 1904 and 1910 and again between 1913 and 1915. A major eruption took place in June 1917, which resulted in volcanic ash being deposited about 48 kilometres away.
A similar eruption took place for several months in 1926 and between July and December 1940, resulting in the ash being deposited as far as Loliondo, which is 100 kilometres away. Several minor eruptions of lava were observed in 1954, 1955, 1958 the early 1960s.
When Ol Doinyo Lengai erupted on August 14, 1966, two geologists — J. B. Dawson and G. C. Clark — who visited the crater a week later, reported seeing “a thick column of black ash” that rose for approximately three thousand feet above the volcano and drifted away northwards towards Lake Natron. When the two climbed the cone-shaped vent, they reported seeing a continuous discharge of gas and whitish-grey ash and dust from the centre of the pit.
Volcanic activity in the mountain caused daily earth tremors in Kenya and Tanzania beginning on July 12, 2007. The latest to hit parts of Nairobi city was recorded on July 18, 2007 at 8.30pm (Kenyan Time). The strongest tremor measured 6.0 on the Richter scale. Geologists suspected that the sudden increase of tremors was indicative of the movement of magma through the Ol Doinyo Lengai. The volcano finally erupted on September 4, 2007, sending a plume of ash and steam at least 18 kilometers downwind and covering the north and west flanks in fresh lava flows. The eruption has continued intermittently into 2008, as of the end of February it was reported that the eruption appeared to be gathering strength, with a major outburst taking place on March 5. During April periods of inactivity have been followed by eruptions on April 8 and 17. Eruptive activity continued until late August 2008. A visit to the summit in September 2008 discovered that lava emission had resumed from two vents in the floor of the new crater. Visits to the crater in March/April 2009 showed that even this activity appears to have ceased.
Lava
Whereas most lavas are rich in silicate minerals, the lava of Ol Doinyo Lengai is a carbonatite. It is rich in the rare sodium and potassium carbonates, nyerereite and gregoryite. Due to this unusual composition, the lava erupts at relatively low temperatures of approximately 500-600 degrees Celsius. This temperature is so low that the molten lava appears black in sunlight, rather than having the red glow common to most lavas. It is also much more fluid than silicate lavas, often less viscous than water. The sodium and potassium carbonate minerals of the lavas formed by Ol Doinyo Lengai are unstable at the Earth’s surface and susceptible to rapid weathering, quickly turning from black to grey in color. The resulting volcanic landscape is different from any other in the world.
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Photo Gallery
Ol Doinyo Lengai Volcano erupting mountain in Tanzania. Spectacular view from Cessna.
Crater of Ol Doinyo Lengai in January 2011, Tanzania , Albert BackerAfter explosive eruptions, ash covers the surrounding landscape. The explosive eruptions built a cone over 100 meters high that enclosed a steep-walled crater. The new cone and crater are clearly visible in the centre of the image. The dark spot in the crater may be fresh lava erupted from a new volcanic vent. Gray ash covers the volcano and much of the surrounding landscape.Flying over Oldoinyo Lengai. Taken with a fisheye photo looking toward the north-east ,Aaron Cawsey
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