Chemical Formula: Y2Fe2+Be2Si2O10 Locality: Ytterby, Resarö, Sweden. Name Origin: Named after the Finnish chemist, Johan Gadolin (1760-1852), who discovered yttrium. The element gadolinium was also named after Johan Gadolin in 1880.
Gadolinite, sometimes also known as Ytterbite, is a silicate mineral that consists principally of the silicates of cerium, lanthanum, neodymium, yttrium, beryllium, and iron with the formula (Ce,La,Nd,Y)2FeBe2Si2O10. It is called gadolinite-(Ce) or gadolinite-(Y) depending on the prominence of the variable element composition (namely, Y if it has more yttrium, and Ce if it has more cerium). It may contain 35.48% yttria sub-group rare earths, 2.17% ceria earths, up to 11.6% BeO and traces of thorium. It is found in Sweden, Norway, and the USA (Texas and Colorado).
Physical Properties
Cleavage: None Color: Brown, Green, Green black, Light green, Black. Density: 4 – 4.5, Average = 4.25 Diaphaneity: Subtransparent to opaque Fracture: Splintery – Thin, elongated fractures produced by intersecting good cleavages or partings (e.g. hornblende). Hardness: 6.5-7 – Pyrite-Quartz Luminescence: Non-fluorescent. Luster: Vitreous – Greasy Streak: greenish gray
Chemical Formula: Zn2+Fe3+2O4 Locality: Dominant ore mineral at Franklin and Sterling Hill, New Jersey, USA. Name Origin: Named after its locality which was named after Benjamin Franklin (1706-1790), American scientist and inventor.
Franklinite is an oxide mineral belonging to the normal spinel subgroup’s iron (Fe) series, with the formula Zn2+Fe3+2O4.
As with another spinel member magnetite, both ferrous (2+) and ferric (3+) iron may be present in Franklinite samples. Divalent iron and/or manganese (Mn) may commonly accompany zinc (Zn) and trivalent manganese may substitute for some ferric iron.
At its type locality, Franklinite can be found with a wide array of minerals, many of which are fluorescent. More commonly, it occurs with willemite, calcite, and red zincite. In these rocks, it forms as disseminated small black crystals with their octahedral faces visible at times. It may rarely be found as a single large euhedral crystal.
Franklinite was a minor ore of zinc, manganese, and iron. It is named after its local discovery at the Franklin Mine and Sterling Hill Mines in New Jersey.
Physical Properties
Cleavage: None Color: Black, Brownish black. Density: 5.07 – 5.22, Average = 5.14 Diaphaneity: Opaque Fracture: Uneven – Flat surfaces (not cleavage) fractured in an uneven pattern. Hardness: 5.5-6 – Knife Blade-Orthoclase Luminescence: Non-fluorescent. Luster: Sub Metallic Magnetism: Naturally weak Streak: reddish brown
Researchers from Lund University and the Swedish Museum of Natural History have made a unique discovery in a well-preserved fern that lived 180 million years ago. Both undestroyed cell nuclei and individual chromosomes have been found in the plant fossil, thanks to its sudden burial in a volcanic eruption.
The well-preserved fossil of a fern from the southern Swedish county of Skåne is now attracting attention in the research community. The plant lived around 180 million years ago, during the Jurassic period, when Skåne was a tropical region where the fauna was dominated by dinosaurs, and volcanoes were a common feature of the landscape. The fossilised fern has been studied using different microscopic techniques, X-rays and geochemical analysis. The examinations reveal that the plant was preserved instantaneously, before it had started to decompose. It was buried abruptly under a volcanic lava flow.
“The preservation happened so quickly that some cells have even been preserved during different stages of cell division”, said Vivi Vajda, Professor of Geology at Lund University.
Thanks to the circumstances of the fern’s sudden death, the sensitive components of the cells have been preserved. The researchers have found cell nuclei, cell membranes and even individual chromosomes. Such structures are extremely rare finds in fossils, observed Vivi Vajda.
“This naturally leads us to think that there must be more to discover. It isn’t hard to imagine what else could be encapsulated in the lava flows at Korsaröd in Skåne”, said Vivi Vajda.
Professor Vajda has carried out the study with two researchers from the Swedish Museum of Natural History, Benjamin Bomfleur and Stephen McLoughlin. The fern belonged to the family Osmundaceae, Royal Ferns. In modern times, royal ferns grow in the wild in Sweden and are also a common garden plant. Living representatives of this family are very similar in appearance to the Jurassic fossil, which suggests that only limited evolutionary change has taken place over the millennia. By comparing the size of the cell nuclei in the fossilised plant with its living relatives, the researchers have been able to show that the royal ferns have outstanding evolutionary stability.
“Royal Ferns look essentially the same now as they did during the Jurassic Period, and are therefore an excellent example of what we call a living fossil”, said Vivi Vajda.
Professor Vajda has also dated the rocks surrounding the fossil by studying pollen and spores preserved in these rocks. Their analysis revealed that the lava flows are around 180 million years old, from the early Jurassic Period. These results have considerably refined previous radiometric dating conducted on nearby volcano cones. In addition, the research study shows that spores from royal ferns, as well as pollen from coniferous trees, including cypress and cycad, are found in large quantities in the volcanic rock. This is evidence of varied vegetation and a hot, humid climate at the time when the area was engulfed by a disastrous volcanic eruption.
The unique fern fossil was collected in the 1960s, near Korsaröd in central Skåne, by farmer Gustav Andersson who donated the fossil to the Swedish Museum of Natural History. The fossil remained forgotten in the museum’s collections for over 40 years before it came to the attention of the researchers. The research findings have now been published in the latest issue of the journal Science.
Reference:
B. Bomfleur, S. McLoughlin, V. Vajda. Fossilized Nuclei and Chromosomes Reveal 180 Million Years of Genomic Stasis in Royal Ferns. Science, 2014; 343 (6177): 1376 DOI: 10.1126/science.1249884
Schematic diagram illustrating the formation of off-rift volcanoes. Credit: R. Milkereit, GFZ
Volcanoes often develop outside the rift zone in an apparently unexpected location offset by tens of kilometers has remained unanswered. An international team of scientists has shown that the pattern of stresses in the crust changes when the crust thins. As a consequence, the path of the magma pockets ascending from the ponding zone is deviated diagonally to the sides of the rift. Eventually, the magma pockets emerge at distances of tens, sometime hundreds of kilometers from the rift axis.
Rift valleys are large depressions formed by tectonic stretching forces. Volcanoes often occur in rift valleys, within the rift itself or on the rift flanks as e.g. in East Africa. The magma responsible for this volcanism is formed in the upper mantle and ponds at the boundary between crust and mantle. For many years, the question of why volcanoes develop outside the rift zone in an apparently unexpected location offset by tens of kilometers from the source of molten magma directly beneath the rift has remained unanswered.
A team of scientists from the GFZ German Research Centre for Geosciences, University of Southampton and University Roma Tre (Italy) have shown that the pattern of stresses in the crust changes when the crust thins due to stretching and becomes gravitationally unloaded. As a consequence of this stress pattern, the path of the magma pockets ascending from the ponding zone is deviated diagonally to the sides of the rift. Eventually, the magma pockets emerge at distances of tens, sometime hundreds of kilometers from the rift axis, creating the so-called off-rift volcanoes.
The scientists used a numerical model that simulates the propagation of the magma pockets, called dikes, to demonstrate a previously unknown control of rift topography on the trajectory of magma transport. The surface location of the volcanoes depend on the geometry of the rift valleys, explains GFZ researcher Francesco Maccaferri: “We find that in broad, shallow rift valleys, the magma will ascend vertically above the source of magma. In deep, narrow valleys the modification of the stress pattern is very intense and the magma path is strongly deviated.” Since in the latter case the initial path of the dikes is almost horizontal, in extreme cases the magma can arrest as a horizontal intrusion and form a pile of stacked sheet-like bodies without any surface volcanism. This is confirmed in rift valleys around the world.
The phenomenon is a dynamic one: “If the tectonic extension continues and the rift reaches a mature stage of evolution, the pile of the magma sheets can reach the shallow crust. Our model predicts correctly that additional magma-filled sheets will then orient vertically and propagate laterally along the middle of the rift.”adds Eleonora Rivalta from GFZ.
Rift valleys are one of the main tectonic features of our planet. They form both between diverging tectonic plates or within plates which undergo tectonic extension. The generation of magma at depth beneath rift valleys and the divergence of the plates through magma intrusions has been an object of research for tens of years, but the link between deep sources and surface volcanism have previously been missing. The new model may be invoked to explain both off-rift volcanism or the lack of volcanism in million years old rift valleys in Europe.
Reference:
Francesco Maccaferri, Eleonora Rivalta, Derek Keir, Valerio Acocella. Off-rift volcanism in rift zones determined by crustal unloading. Nature Geoscience, 2014; DOI: 10.1038/NGEO2110
Researcher Josh West treks through a valley in Peru in search of evidence of chemical weathering of rocks as they erode. Credit: Mark Torres / USC
Researchers from USC and Nanjing University in China have documented evidence suggesting that part of the reason that the Earth has become neither sweltering like Venus nor frigid like Mars lies with a built-in atmospheric carbon dioxide regulator – the geologic cycles that churn up the planet’s rocky surface.
Scientists have long known that “fresh” rock pushed to the surface via mountain formation effectively acts as a kind of sponge, soaking up the greenhouse gas CO2. Left unchecked, however, that process would simply deplete atmospheric CO2 levels to a point that would plunge the Earth into an eternal winter within a few million years during the formation of large mountain ranges like the Himalayas – which has clearly not happened.
And while volcanoes have long been pointed to as a source of carbon dioxide, alone they cannot balance out the excess uptake of carbon dioxide by large mountain ranges. Instead, it turns out that “fresh” rock exposed by uplift also emits carbon through a chemical weathering process, which replenishes the atmospheric carbon dioxide at a comparable rate.
“Our presence on Earth is dependent upon this carbon cycle. This is why life is able to survive,” said Mark Torres, lead author of a study disclosing the findings that appears in Nature on March 20. Torres, a doctoral fellow at the USC Dornsife College of Letters, Arts and Sciences, and a fellow at the Center for Dark Energy Biosphere Investigations (C-DEBI), collaborated with Joshua West, professor of Earth Sciences at USC Dornsife, and Gaojun Li of Nanjing University in China.
While human-made atmospheric carbon dioxide increases are currently driving significant changes in the Earth’s climate, the geologic system has kept things balanced for million of years.
“The Earth is a bit like a big, natural recycler,” West said. Torres and West studied rocks taken from the Andes mountain range in Peru and found that weathering processes affecting rocks released far more carbon than previously estimated, which motivated them to consider the global implications of CO2 release during mountain formation.
The researchers noted that rapid erosion in the Andes unearths abundant pyrite—the shiny mineral known as “fool’s gold” because of its deceptive appearance—and its chemical breakdown produces acids that release CO2 from other minerals. These observations motivated them to consider the global implications of CO2 release during mountain formation.
Like many other large mountain ranges, such as the great Himalayas, the Andes began to form during the Cenozoic period, which began about 60 million years ago and happened to coincide with a major perturbation in the cycling of atmospheric carbon dioxide. Using marine records of the long-term carbon cycle, Torres, West, and Li reconstructed the balance between CO2 release and uptake caused by the uplift of large mountain ranges and found that the release of CO2 release by rock weathering may have played a large, but thus far unrecognized, role in regulating the concentration of atmospheric carbon dioxide over the last roughly 60 million years.
Note : The above story is based on materials provided by University of Southern California
Chemical Formula: Fe2+(Pb,Sn2+)6Sn24+Sb2S14 Locality: Found in Bolivia at Poopo in Oruro and at Las Aminas, southeast of Chocaya, in Potosi. Name Origin: Named after the mining engineers, Carl and Ernest Francke.
Franckeite, chemical formula Fe2+(Pb,Sn2+)6Sn24+Sb2S14, belongs to a family of complex sulfide minerals. Franckeite is a sulfosalt. It is closely related to cylindrite.
It was first described in 1893 for an occurrence in Chocaya, Potosí Department, Bolivia. It is named after the mining engineers, Carl and Ernest Francke. It can be found in Bolivia at Poopó in Oruro and at Las Aminas, southeast of Chocaya, in Potosi. Franckeite has an average density of 5.7 and can be both grayish black, blackish gray in color.
It occurs in hydrothermal silver-tin deposits in Bolivia and in contact metamorphosed limestone deposit in the Kalkar quarry in California. It occurs with cylindrite, teallite, plagionite, zinkenite, cassiterite, wurtzite, pyrrhotite, marcasite, arsenopyrite, galena, pyrite, sphalerite, siderite and stannite.
Francevillite , Mounanaite , Curienite Locality: Mounana Mine (Mouana Mine), Franceville, Haut-Ogooué Province, Gabon Dimensions: 4 cm x 3.5 cm x 1 cm”Courtesy of Rob Lavinsky, The Arkenstone, www.iRocks.com”
Chemical Formula: (Ba,Pb)(UO2)2V2O8·5(H2O) Locality: Mounana mine, Franceville, Haut-Ogooue, Gabon. Name Origin: Named for the locality
Francevillite is a uranyl-group vanadate mineral in the tyuyamunite series. Its chemical formula is (Ba,Pb)(UO2)2V2O8·5(H2O). Francevillite is a strongly radioactive mineral. It is typically orange, yellow or brownish yellow. It forms a series with curienite.
Occurrence
Francevillite occurs in the oxidized zone of a lead-bearing uranium–vanadium deposits. Francevillite was first described in 1957 for an occurrence in its type locality of the idle Mounana uranium mine, near Franceville, Haut-Ogooué, Gabon and was named for the city.
At its type locality it is associated with curienite (a closely related uranyl vanadate), chevetite (a lead vanadate), and mounanaite (another lead vanadate). At other localities, francevillite is associated with duttonite, vanuralite, mottramite, carnotite, dewindtite, torbernite, uranopilite, johannite and kasolite.
The Carboniferous is a geologic period and system that extends from the end of the Devonian Period, about 358.9 ± 0.4 million years ago, to the beginning of the Permian Period, about 298.9 ± 0.15 Ma. The name Carboniferous means “coal-bearing” and derives from the Latin words carbo (coal) and fero, fers (to carry), and was coined by geologists William Conybeare and William Phillips in 1822. Based on a study of the British rock succession, it was the first of the modern ‘system’ names to be employed, and reflects the fact that many coal beds were formed globally during this time. The Carboniferous is often treated in North America as two geological periods, the earlier Mississippian and the later Pennsylvanian.
Terrestrial life was well established by the Carboniferous period. Amphibians were the dominant land vertebrates, of which one branch would eventually evolve into reptiles, the first fully terrestrial vertebrates. Arthropods were also very common, and many (such as Meganeura), were much larger than those of today. Vast swaths of forest covered the land, which would eventually be laid down and become the coal beds characteristic of the Carboniferous system. A minor marine and terrestrial extinction event occurred in the middle of the period, caused by a change in climate. The later half of the period experienced glaciations, low sea level, and mountain building as the continents collided to form Pangaea.
Subdivisions
In the United States the Carboniferous is usually broken into Mississippian (earlier) and Pennsylvanian (later) Periods. The Mississippian is about twice as long as the Pennsylvanian, but due to the large thickness of coal bearing deposits with Pennsylvanian ages in Europe and North America, the two subperiods were long thought to have been more or less equal. The faunal stages from youngest to oldest, together with some of their subdivisions, are:
Late Pennsylvanian: Gzhelian (most recent)
Noginskian / Virgilian (part)
Late Pennsylvanian: Kasimovian
Klazminskian
Dorogomilovksian / Virgilian (part)
Chamovnicheskian / Cantabrian / Missourian
Krevyakinskian / Cantabrian / Missourian
Middle Pennsylvanian: Moscovian
Myachkovskian / Bolsovian / Desmoinesian
Podolskian / Desmoinesian
Kashirskian / Atokan
Vereiskian / Bolsovian / Atokan
Early Pennsylvanian: Bashkirian / Morrowan
Melekesskian / Duckmantian
Cheremshanskian / Langsettian
Yeadonian
Marsdenian
Kinderscoutian
Late Mississippian: Serpukhovian
Alportian
Chokierian / Chesterian / Elvirian
Arnsbergian / Elvirian
Pendleian
Middle Mississippian: Visean
Brigantian / St Genevieve / Gasperian / Chesterian
Asbian / Meramecian
Holkerian / Salem
Arundian / Warsaw / Meramecian
Chadian / Keokuk / Osagean (part) / Osage (part)
Early Mississippian: Tournaisian (oldest)
Ivorian / (part) / Osage (part)
Hastarian / Kinderhookian / Chouteau
Paleogeography
A global drop in sea level at the end of the Devonian reversed early in the Carboniferous; this created the widespread epicontinental seas and carbonate deposition of the Mississippian. There was also a drop in south polar temperatures; southern Gondwanaland was glaciated throughout the period, though it is uncertain if the ice sheets were a holdover from the Devonian or not. These conditions apparently had little effect in the deep tropics, where lush coal swamps flourished within 30 degrees of the northernmost glaciers.
Generalized geographic map of the United States in Middle Pennsylvanian time.
A mid-Carboniferous drop in sea level precipitated a major marine extinction, one that hit crinoids and ammonites especially hard. This sea level drop and the associated unconformity in North America separate the Mississippian subperiod from the Pennsylvanian subperiod. This happened about 318 million years ago, at the onset of the Permo-Carboniferous Glaciation.
The Carboniferous was a time of active mountain-building, as the supercontinent Pangaea came together. The southern continents remained tied together in the supercontinent Gondwana, which collided with North America–Europe (Laurussia) along the present line of eastern North America. This continental collision resulted in the Hercynian orogeny in Europe, and the Alleghenian orogeny in North America; it also extended the newly uplifted Appalachians southwestward as the Ouachita Mountains. In the same time frame, much of present eastern Eurasian plate welded itself to Europe along the line of the Ural mountains. Most of the Mesozoic supercontinent of Pangea was now assembled, although North China (which would collide in the Latest Carboniferous), and South China continents were still separated from Laurasia. The Late Carboniferous Pangaea was shaped like an “O.”
There were two major oceans in the Carboniferous—Panthalassa and Paleo-Tethys, which was inside the “O” in the Carboniferous Pangaea. Other minor oceans were shrinking and eventually closed – Rheic Ocean (closed by the assembly of South and North America), the small, shallow Ural Ocean (which was closed by the collision of Baltica and Siberia continents, creating the Ural Mountains) and Proto-Tethys Ocean (closed by North China collision with Siberia/Kazakhstania).
Climate
The early part of the Carboniferous was mostly warm; in the later part of the Carboniferous, the climate cooled. Glaciations in Gondwana, triggered by Gondwana’s southward movement, continued into the Permian and because of the lack of clear markers and breaks, the deposits of this glacial period are often referred to as Permo-Carboniferous in age.
The cooling and drying of the climate led to the Carboniferous Rainforest Collapse (CRC). Tropical rainforests fragmented and then were eventually devastated by climate change
Rocks and coal
Mississippian marble in Big Cottonwood Canyon, Wasatch Mountains, Utah. Photograph taken by Mark A. Wilson (Department of Geology, The College of Wooster).
Carboniferous rocks in Europe and eastern North America largely consist of a repeated sequence of limestone, sandstone, shale and coal beds. In North America, the early Carboniferous is largely marine limestone, which accounts for the division of the Carboniferous into two periods in North American schemes. The Carboniferous coal beds provided much of the fuel for power generation during the Industrial Revolution and are still of great economic importance.
The large coal deposits of the Carboniferous primarily owe their existence to two factors. The first of these is the appearance of bark-bearing trees (and in particular the evolution of the bark fiber lignin). The second is the lower sea levels that occurred during the Carboniferous as compared to the Devonian period. This allowed for the development of extensive lowland swamps and forests in North America and Europe. Based on a genetic analysis of mushroom fungi, David Hibbett and colleagues proposed that large quantities of wood were buried during this period because animals and decomposing bacteria had not yet evolved that could effectively digest the tough lignin. It is assumed that fungi that could break it down did not arise before the end of the period, making future coal formation much more rare. The Carboniferous trees made extensive use of lignin. They had bark to wood ratios of 8 to 1, and even as high as 20 to 1. This compares to modern values less than 1 to 4. This bark, which must have been used as support as well as protection, probably had 38% to 58% lignin. Lignin is insoluble, too large to pass through cell walls, too heterogeneous for specific enzymes, and toxic, so that few organisms other than Basidiomycetes fungi can degrade it. It can not be oxidized in an atmosphere of less than 5% oxygen. It can linger in soil for thousands of years and inhibits decay of other substances. Probably the reason for its high percentages is protection from insect herbivory in a world containing very effective insect herbivores, but nothing remotely as effective as modern insectivores and probably many fewer poisons than currently. In any case coal measures could easily have made thick deposits on well drained soils as well as swamps. The extensive burial of biologically produced carbon led to a buildup of surplus oxygen in the atmosphere; estimates place the peak oxygen content as high as 35%, compared to 21% today. This oxygen level probably increased wildfire activity, as well as resulted in insect and amphibian gigantism—creatures whose size is constrained by respiratory systems that are limited in their ability to diffuse oxygen.
In eastern North America, marine beds are more common in the older part of the period than the later part and are almost entirely absent by the late Carboniferous. More diverse geology existed elsewhere, of course. Marine life is especially rich in crinoids and other echinoderms. Brachiopods were abundant. Trilobites became quite uncommon. On land, large and diverse plant populations existed. Land vertebrates included large amphibians.
Life
Plants
Early Carboniferous land plants, some of which were preserved in coal balls, were very similar to those of the preceding Late Devonian, but new groups also appeared at this time.
The main Early Carboniferous plants were the Equisetales (horse-tails), Sphenophyllales (vine-like plants), Lycopodiales (club mosses), Lepidodendrales (scale trees), Filicales (ferns), Medullosales (informally included in the “seed ferns”, an artificial assemblage of a number of early gymnosperm groups) and the Cordaitales. These continued to dominate throughout the period, but during late Carboniferous, several other groups, Cycadophyta (cycads), the Callistophytales (another group of “seed ferns”), and the Voltziales (related to and sometimes included under the conifers), appeared.
The Carboniferous lycophytes of the order Lepidodendrales, which are cousins (but not ancestors) of the tiny club-moss of today, were huge trees with trunks 30 meters high and up to 1.5 meters in diameter. These included Lepidodendron (with its fruit cone called Lepidostrobus), Halonia, Lepidophloios and Sigillaria. The roots of several of these forms are known as Stigmaria. Unlike present day trees, their secondary growth took place in the cortex, which also provided stability, instead of the xylem. The Cladoxylopsids were large trees, that were ancestors of ferns, first arising in the Carboniferous.
The fronds of some Carboniferous ferns are almost identical with those of living species. Probably many species were epiphytic. Fossil ferns and “seed ferns” include Pecopteris, Cyclopteris, Neuropteris, Alethopteris, and Sphenopteris; Megaphyton and Caulopteris were tree ferns.
The Equisetales included the common giant form Calamites, with a trunk diameter of 30 to 60 cm (24 in) and a height of up to 20 m (66 ft). Sphenophyllum was a slender climbing plant with whorls of leaves, which was probably related both to the calamites and the lycopods.
Cordaites, a tall plant (6 to over 30 meters) with strap-like leaves, was related to the cycads and conifers; the catkin-like inflorescence, which bore yew-like berries, is called Cardiocarpus. These plants were thought to live in swamps and mangroves. True coniferous trees (Walchia, of the order Voltziales) appear later in the Carboniferous, and preferred higher drier ground.
Marine invertebrates
Aviculopecten subcardiformis from the Logan Formation, Mississippian, Ohio. Photograph taken by Mark A. Wilson (Department of Geology, The College of Wooster)
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Syringothyris sp.; a spiriferid brachiopod from the Logan Formation (Lower Carboniferous) of Wooster, Ohio (internal molds). Photograph taken by Mark A. Wilson (Department of Geology, The College of Wooster).
In the oceans the most important marine invertebrate groups are the Foraminifera, corals, Bryozoa, Ostracoda, brachiopods, ammonoids, hederelloids, microconchids and echinoderms (especially crinoids). For the first time foraminifera take a prominent part in the marine faunas. The large spindle-shaped genus Fusulina and its relatives were abundant in what is now Russia, China, Japan, North America; other important genera include Valvulina, Endothyra, Archaediscus, and Saccammina (the latter common in Britain and Belgium). Some Carboniferous genera are still extant.
The microscopic shells of radiolarians are found in cherts of this age in the Culm of Devon and Cornwall, and in Russia, Germany and elsewhere. Sponges are known from spicules and anchor ropes, and include various forms such as the Calcispongea Cotyliscus and Girtycoelia, the demosponge Chaetetes, and the genus of unusual colonial glass sponges Titusvillia.
Both reef-building and solitary corals diversify and flourish; these include both rugose (for example, Caninia, Corwenia, Neozaphrentis), heterocorals, and tabulate (for example, Chladochonus, Michelinia) forms. Conularids were well represented by Conularia
Bryozoa are abundant in some regions; the fenestellids including Fenestella, Polypora, and Archimedes, so named because it is in the shape of an Archimedean screw. Brachiopods are also abundant; they include productids, some of which (for example, Gigantoproductus) reached very large (for brachiopods) size and had very thick shells, while others like Chonetes were more conservative in form. Athyridids, spiriferids, rhynchonellids, and terebratulids are also very common. Inarticulate forms include Discina and Crania. Some species and genera had a very wide distribution with only minor variations.
Annelids such as Serpulites are common fossils in some horizons. Among the mollusca, the bivalves continue to increase in numbers and importance. Typical genera include Aviculopecten, Posidonomya, Nucula, Carbonicola, Edmondia, and Modiola Gastropods are also numerous, including the genera Murchisonia, Euomphalus, Naticopsis. Nautiloid cephalopods are represented by tightly coiled nautilids, with straight-shelled and curved-shelled forms becoming increasingly rare. Goniatite ammonoids are common.
Trilobites are rarer than in previous periods, on a steady trend towards extinction, represented only by the proetid group. Ostracoda, a class of crustaceans, were abundant as representatives of the meiobenthos; genera included Amphissites, Bairdia, Beyrichiopsis, Cavellina, Coryellina, Cribroconcha, Hollinella, Kirkbya, Knoxiella, and Libumella.
Amongst the echinoderms, the crinoids were the most numerous. Dense submarine thickets of long-stemmed crinoids appear to have flourished in shallow seas, and their remains were consolidated into thick beds of rock. Prominent genera include Cyathocrinus, Woodocrinus, and Actinocrinus. Echinoids such as Archaeocidaris and Palaeechinus were also present. The blastoids, which included the Pentreinitidae and Codasteridae and superficially resembled crinoids in the possession of long stalks attached to the seabed, attain their maximum development at this time.
Freshwater and lagoonal invertebrates
Freshwater Carboniferous invertebrates include various bivalve molluscs that lived in brackish or fresh water, such as Anthraconaia, Naiadites, and Carbonicola; diverse crustaceans such as Candona, Carbonita, Darwinula, Estheria, Acanthocaris, Dithyrocaris, and Anthrapalaemon.
The Eurypterids were also diverse, and are represented by such genera as Eurypterus, Glyptoscorpius, Anthraconectes, Megarachne (originally misinterpreted as a giant spider) and the specialised very large Hibbertopterus. Many of these were amphibious.
Frequently a temporary return of marine conditions resulted in marine or brackish water genera such as Lingula, Orbiculoidea, and Productus being found in the thin beds known as marine bands.
Terrestrial invertebrates
Fossil remains of air-breathing insects, myriapods and arachnids are known from the late Carboniferous, but so far not from the early Carboniferous. The first true priapulids appeared during this period. Their diversity when they do appear, however, shows that these arthropods were both well developed and numerous. Their large size can be attributed to the moistness of the environment (mostly swampy fern forests) and the fact that the oxygen concentration in the Earth’s atmosphere in the Carboniferous was much higher than today (35% then compared with 21% today). This required less effort for respiration and allowed arthropods to grow larger with the up to 2.6 metres long millipede-like Arthropleura being the largest known land invertebrate of all time. Among the insect groups are the huge predatory Protodonata (griffinflies), among which was Meganeura, a giant dragonfly-like insect and with a wingspan of ca. 75 cm (30 in) — the largest flying insect ever to roam the planet. Further groups are the Syntonopterodea (relatives of present-day mayflies), the abundant and often large sap-sucking Palaeodictyopteroidea, the diverse herbivorous Protorthoptera, and numerous basal Dictyoptera (ancestors of cockroaches). Many insects have been obtained from the coalfields of Saarbrücken and Commentry, and from the hollow trunks of fossil trees in Nova Scotia. Some British coalfields have yielded good specimens: Archaeoptitus, from the Derbyshire coalfield, had a spread of wing extending to more than 35 cm; some specimens (Brodia) still exhibit traces of brilliant wing colors. In the Nova Scotian tree trunks land snails (Archaeozonites, Dendropupa) have been found.
Fish
Many fish inhabited the Carboniferous seas; predominantly Elasmobranchs (sharks and their relatives). These included some, like Psammodus, with crushing pavement-like teeth adapted for grinding the shells of brachiopods, crustaceans, and other marine organisms. Other sharks had piercing teeth, such as the Symmoriida; some, the petalodonts, had peculiar cycloid cutting teeth. Most of the sharks were marine, but the Xenacanthida invaded fresh waters of the coal swamps. Among the bony fish, the Palaeonisciformes found in coastal waters also appear to have migrated to rivers. Sarcopterygian fish were also prominent, and one group, the Rhizodonts, reached very large size.
Most species of Carboniferous marine fish have been described largely from teeth, fin spines and dermal ossicles, with smaller freshwater fish preserved whole.
Freshwater fish were abundant, and include the genera Ctenodus, Uronemus, Acanthodes, Cheirodus, and Gyracanthus.
Sharks (especially the Stethacanthids) underwent a major evolutionary radiation during the Carboniferous. It is believed that this evolutionary radiation occurred because the decline of the placoderms at the end of the Devonian period caused many environmental niches to become unoccupied and allowed new organisms to evolve and fill these niches. As a result of the evolutionary radiation carboniferous sharks assumed a wide variety of bizarre shapes including Stethacanthus which possessed a flat brush-like dorsal fin with a patch of denticles on its top. Stethacanthus’ unusual fin may have been used in mating rituals.
Tetrapods
Carboniferous amphibians were diverse and common by the middle of the period, more so than they are today; some were as long as 6 meters, and those fully terrestrial as adults had scaly skin. They included a number of basal tetrapod groups classified in early books under the Labyrinthodontia. These had long bodies, a head covered with bony plates and generally weak or undeveloped limbs. The largest were over 2 meters long. They were accompanied by an assemblage of smaller amphibians included under the Lepospondyli, often only about 15 cm (6 in) long. Some Carboniferous amphibians were aquatic and lived in rivers (Loxomma, Eogyrinus, Proterogyrinus); others may have been semi-aquatic (Ophiderpeton, Amphibamus, Hyloplesion) or terrestrial (Dendrerpeton, Tuditanus, Anthracosaurus).
The Carboniferous Rainforest Collapse slowed the evolution of amphibians who could not survive as well in the cooler, drier conditions. Reptiles, however prospered due to specific key adaptations. One of the greatest evolutionary innovations of the Carboniferous was the amniote egg, which allowed for the further exploitation of the land by certain tetrapods. These included the earliest sauropsid reptiles (Hylonomus), and the earliest known synapsid (Archaeothyris). These small lizard-like animals quickly gave rise to many descendants. The amniote egg allowed these ancestors of all later birds, mammals, and reptiles to reproduce on land by preventing the desiccation, or drying-out, of the embryo inside.
Reptiles underwent a major evolutionary radiation in response to the drier climate that proceeded the rainforest collapse. By the end of the Carboniferous period, amniotes had already diversified into a number of groups, including protorothyridids, captorhinids, aeroscelids, and several families of pelycosaurs.
Fungi
Because plants and animals were growing in size and abundance in this time (for example, Lepidodendron), land fungi diversified further. Marine fungi still occupied the oceans. All modern classes of fungi were present in the Late Carboniferous (Pennsylvanian Epoch).
Extinction events
Romer’s gap
The first 15 million years of the Carboniferous had very limited terrestrial fossils. This gap in the fossil record is called Romer’s gap after the American palaentologist Alfred Romer. While it has long been debated whether the gap is a result of fossilisation or relates to an actual event, recent work indicates the gap period saw a drop in atmospheric oxygen levels, indicating some sort of ecological collapse. The gap saw the demise of the Devonian fish-like ichthyostegalian labyrinthodonts, and the rise of the more advanced temnospondyl and reptiliomorphan amphibians that so typify the Carboniferous terrestrial vertebrate fauna.
Carboniferous rainforest collapse
Before the end of the Carboniferous Period, an extinction event occurred. On land this event is referred to as the Carboniferous Rainforest Collapse (CRC). Vast tropical rainforests collapsed suddenly as the climate changed from hot and humid to cool and arid. This was likely caused by intense glaciation and a drop in sea levels.
The new climatic conditions were not favorable to the growth of rainforest and the animals within them. Rainforests shrank into isolated islands, surrounded by seasonally dry habitats. Towering lycopsid forests with a heterogeneous mixture of vegetation were replaced by much less diverse tree-fern dominated flora.
Amphibians, the dominant vertebrates at the time, fared poorly through this event with large losses in biodiversity; reptiles continued to diversify due to key adaptations that let them survive in the drier habitat, specifically the hard-shelled egg and scales both of which retain water better than their amphibian counterparts.
Note : The above story is based on materials provided by Wikipedia
The Serpukhovian is in the ICS geologic timescale the uppermost stage or youngest age of the Mississippian, the lower subsystem of the Carboniferous. The Serpukhovian age lasted from 330.9 ± 0.2 Ma to 323.2 ± 0.4 Ma. It is preceded by the Visean and is followed by the Bashkirian.
The Serpukhovian correlates with the lower part of the Namurian stage of European stratigraphy and the middle and upper parts of the Chesterian stage of North American stratigraphy.
Name and definition
The Serpukhovian stage was proposed in 1890 by Russian stratigrapher Sergei Nikitin and was introduced in the official stratigraphy of European Russia in 1974. It was named after the city of Serpukhov, near Moscow. The ICS later used the upper Russian subdivisions of the Carboniferous in its international geologic time scale.
The base of the Serpukhovian is at the first appearance of the conodont Lochriea crusiformis. In 2007, no GSSP had been assigned to the Serpukhovian stage yet. The top of the stage (the base of the Pennsylvanian subsystem and Bashkirian stage) is at the first appearance of the conodont Declinognathodus nodiliferus. It is also slightly above the first appearance of the foram Globivalvulina bulloides, genozone of the ammonoid genus Homoceras and the ammonoid biozone of Isohomoceras subglobosum.
Subdivision
The Serpukhovian stage includes four conodont biozones:
Gnathodus postbilineatus Zone
Gnathodus bollandensis Zone
Lochriea cruciformis Zone
Lochriea ziegleri Zone
In Russian stratigraphy, the Serpukhovian is subdivided into three substages, from bottom to top: Tarusian, Steshevian, and Protvian, named after places near Serpukhov (see Tarusa, Protva). In British stratigraphy, the Serpukhovian (lower Namurian) contains three substages. These are from bottom to top: Pendleian, Arnsbergian and Chokierian (only the lower Chokierian falls in the Serpukhovian, the top falls in the Bashkirian).
Note : The above story is based on materials provided by Wikipedia
The Visean, Viséan or Visian is an age in the ICS geologic timescale or a stage in the stratigraphic column. It is the second stage of the Mississippian, the lower subsystem of the Carboniferous. The Visean lasted from 346.7 ± 0.4 to 330.9 ± 0.2 Ma. It follows the Tournaisian age/stage and is followed by the Serpukhovian age/stage.
Name and definitions
The Visean stage was introduced by Belgian geologist André Dumont in 1832. Dumont called this stage after the city of Visé in the Belgian province of Liège. Before being used as an international stage, the Visean stage was part of the (West) European regional geologic time scale, in which it followed the Tournaisian stage and is followed by the Namurian stage. In the North American regional scale, the Visean stage correlates with the upper Osagean, the Meramecian and lower Chesterian stages. In the Chinese regional time scale, it correlates with the lower and middle Tatangian series.
The base of the Visean stage is at the first appearance of the fusulinid species Eoparastaffella simplex (morphotype 1/morphotype 2). The type locality for the stage base used to be in a road section below the castle of Dinant in Belgium, but this type locality proved to be insufficient for the purpose of stratigraphic correlation. A GSSP has been proposed in the Luzhai Formation near Penchong in the Chinese province of Guanxi. The top (the base of the Serpukhovian and Namurian) is laid at the first appearance of the conodont Lochriea ziegleri,or at the base of the biozone of goniatite Cravenoceras leion.
Tetrapods
One of the tetrapods that lived during the Visean age was westlothiana, a reptile-like amphibian.
Biostratigraphy
The Visean contains four conodont biozones:
Lochriea nodosa Zone
Lochriea mononodosa Zone
Gnathodus bilineatus Zone
Gnathodus texanus Zone
In British stratigraphy, the Visean is subdivided into five substages. These are from bottom to top: Chadian (the lower part of this substage falls in the Tournaisian), Arundian, Holkerian, Asbian and Brigantian.
Note : The above story is based on materials provided by Wikipedia
The Tournaisian is in the ICS geologic timescale the lowest stage or oldest age of the Mississippian, the oldest subsystem of the Carboniferous. The Tournaisian age lasted from 358.9 ± 0.4 Ma to 346.7 ± 0.4 Ma. It is preceded by the Famennian (the uppermost stage of the Devonian) and is followed by the Viséan.
Name and regional alternatives
The Tournaisian was named after the Belgian city of Tournai. It was introduced in scientific literature by Belgian geologist André Hubert Dumont in 1832. Like many Devonian and lower Carboniferous stages, the Tournaisian is a unit from West European regional stratigraphy that is now used in the official international time scale.
The Tournaisian correlates with the regional North American Kinderhookian and lower Osagean stages and the Chinese Tangbagouan regional stage. In British stratigraphy, the Tournaisian contains three substages: the Hastarian, Ivorian and lower part of the Chadian (the upper part falls in the Viséan).
Stratigraphy
The base of the Tournaisian (which is also the base of the Carboniferous system) is at the first appearance of the conodont Siphonodella sulcata within the evolutionary lineage from Siphonodella praesulcata to Siphonodella sulcata. The first appearance of ammonite species Gattendorfia subinvoluta is just above this and was used as a base for the Carboniferous in the past. The GSSP for the Tournaisian is near the summit of La Serre hill, in the commune of Cabrières, in the Montagne Noire (southern France).[5] The GSSP is in a section on the southern side of the hill, in an 80 cm deep trench, about 125 m south of the summit, 2.5 km southwest of the village of Cabrières and 2.5 km north of the hamlet of Fontès.
The top of the Tournaisian (the base of the Viséan) is at the first appearance of the fusulinid species Eoparastaffella simplex (morphotype 1/morphotype 2).
The Tournaisian contains eight conodont biozones:
the zone of Gnathodus pseudosemiglaber and Scaliognathus anchoralis
the zone of Gnathodus semiglaber and Polygnathus communis
the zone of Dollimae bouckaerti
the zone of Gnathodus typicus and Siphonodella isosticha
the zone of Siphonodella quadruplicata and Patrognathus andersoni (upper zone of Patrognathus andersoni)
the lower zone of Patrognathus andersoni
the zone of Patrognathus variabilis
the zone of Patrognathus crassus
The Tournaisian coincide with Romer’s gap, a period of remarkable little terrestrial fossils, thus constituting a discontinuity between the Devonian and the more modern terrestrial ecosystems of the Carboniferous.
Note : The above story is based on materials provided by Wikipedia
The Mississippian is a subperiod in the geologic timescale or a subsystem of the geologic record. It is the earliest/lowermost of two subperiods of the Carboniferous period lasting from roughly 358.9 ± 0.4 to 323.2 ± 0.4 million years ago. As with most other geochronologic units, the rock beds that define the Mississippian are well identified, but the exact start and end dates are uncertain by a few million years. The Mississippian is so named because rocks with this age are exposed in the Mississippi River valley.
The Mississippian was a period of marine ingression in the Northern Hemisphere: the ocean stood so high only the Fennoscandian Shield and the Laurentian Shield stood above sea level. The cratons were surrounded by extensive delta systems and lagoons, and carbonate sedimentation on the surrounding continental platforms, covered by shallow seas.
In North America, where the interval consists primarily of marine limestones, it is treated as a geologic period between the Devonian and the Pennsylvanian. During the Mississippian an important phase of orogeny occurred in the Appalachian Mountains. It is a major rock building period named for the exposures in the Mississippi Valley region. The USGS geologic time scale shows its relation to other periods.
In Europe, the Mississippian and Pennsylvanian are one more-or-less continuous sequence of lowland continental deposits and are grouped together as the Carboniferous system, and sometimes called the Upper Carboniferous and Lower Carboniferous instead.
Subdivisions
In the official geologic timescale, the Mississippian is subdivided into three stages:
The first two come from European stratigraphy, the last is from Russian stratigraphy. Besides Europe and Russia, there are many local subdivisions that are used as alternatives for the international timescale. In the North American system, the Mississippian is subdivided into four stages:
Chesterian (top of the Visean plus the Serpukhovian)
Meramecian (middle Visean)
Osagean (top of the Tournaisian and bottom of the Visean)
Kinderhookian (the lower two-thirds of the Tournaisian)
Note : The above story is based on materials provided by Wikipedia
This is a mounted replica skeleton of the new oviraptorosaurian dinosaur species Anzu wyliei on display in the Dinosaurs in Their Time exhibition at Carnegie Museum of Natural History, Pittsburgh, Pa., USA. Credit: Carnegie Museum of Natural History.
A team of researchers has announced the discovery of a bizarre, bird-like dinosaur, named Anzu wyliei, that provides paleontologists with their first good look at a dinosaur group that has been shrouded in mystery for almost a century. Anzu was described from three specimens that collectively preserve almost the entire skeleton, giving scientists a remarkable opportunity to study the anatomy and evolutionary relationships of Caenagnathidae (pronounced SEE-nuh-NAY-thih-DAY) — the long-mysterious group of theropod dinosaurs to which Anzu belongs.
The three described fossil skeletons of Anzu were unearthed in North and South Dakota, from roughly 66 million-year-old rocks of the Hell Creek Formation, a rock unit celebrated for its abundant fossils of famous dinosaurs such as Tyrannosaurus rex and Triceratops. The scientific paper describing the discovery appears today in the freely-accessible journal PLOS ONE.
The team of scientists who studied Anzu was led by Dr. Matthew Lamanna of Carnegie Museum of Natural History in Pittsburgh. Dr. Lamanna’s collaborators include Dr. Hans-Dieter Sues and Dr. Tyler Lyson of the Smithsonian Institution’s National Museum of Natural History in Washington, DC, and Dr. Emma Schachner of the University of Utah in Salt Lake City. According to Dr. Lamanna, “Anzu is far and away the most complete caenagnathid that has ever been discovered. After nearly a century of searching, we paleontologists finally have the fossils to show what these creatures looked like from virtually head to toe. And in almost every way, they’re even weirder than we imagined.”
This is a life reconstruction of the new oviraptorosaurian dinosaur species Anzu wyliei. Credit: Courtesy Bob Walters
Hell’s Chicken
At roughly 11 feet long and five feet tall at the hip, Anzu would have resembled a gigantic flightless bird, more than a ‘typical’ theropod dinosaur such as T. rex. Its jaws were tipped with a toothless beak, and its head sported a tall, rounded crest similar to that of a cassowary (a large ground bird native to Australia and New Guinea). The neck and hind legs were long and slender, also comparable to a cassowary or ostrich. Although the Anzu specimens preserve only bones, close relatives of this dinosaur have been found with fossilized feathers, strongly suggesting that the new creature was feathered too. The resemblance to birds ends there, however: the forelimbs of Anzu were tipped with large, sharp claws, and the tail was long and robust. Says Dr. Lamanna, “We jokingly call this thing the ‘Chicken from Hell,’ and I think that’s pretty appropriate. So we named it after Anzu, a bird-like demon in ancient mythology.”The species is named for a Carnegie Museums of Pittsburgh Trustee’s grandson, Wylie.
Not only do the fossils of Anzu wyliei paint a picture of this particular species, they shed light on an entire group of dinosaurs, the first evidence of which was discovered almost 100 years ago. In 1924, paleontologist Charles Whitney Gilmore described the species Chirostenotes pergracilis from a pair of fossil hands found a decade earlier in ~74 million-year-old rocks in Alberta, Canada. Later, in 1940, Caenagnathus collinsi was named, based on a peculiar lower jaw from the same beds. More recently, after studies of these and other fragmentary fossils, Hans Sues and other paleontologists determined that Chirostenotes and Caenagnathus belonged to the same dinosaur group, Caenagnathidae, and that these animals were close cousins of Asian oviraptorid theropods such as Oviraptor.
Asian relations
Oviraptor (‘egg thief’) is widely known because the first fossil skeleton of this animal, described in 1924, was found atop a nest of dinosaur eggs, suggesting that the creature had died in the act of raiding the nest. This thinking prevailed until the 1990s, when the same type of egg was found with a baby oviraptorid inside, demonstrating that, rather than a nest plunderer, Oviraptor was a caring parent that perished while protecting its eggs. More than a dozen oviraptorid species have been discovered, all in Mongolia and China, and many are known from beautifully-preserved, complete or nearly complete skeletons. Additionally, beginning in the 1990s, several small, primitive relatives of oviraptorids were unearthed in much older, ~125 million-year-old rocks in northeastern China. Many of these are also represented by complete skulls or skeletons, some of which preserve fossilized feathers. Researchers have established that caenagnathids, oviraptorids, and these more archaic Chinese species are closely related to one another, and have united them as the theropod group Oviraptorosauria. The occurrence of oviraptorosaurs in both Asia and North America was not a surprise to paleontologists, because these continents were frequently connected during the Mesozoic Era (the ‘Age of Dinosaurs’), allowing dinosaurs and other land animals to roam between them. However, because their fossils were so incomplete, caenagnathids remained the most poorly known members of Oviraptorosauria, and indeed, one of the least understood of all major dinosaur groups. “For many years, caenagnathids were known only from a few bits of the skeleton, and their appearance remained a big mystery,” says Dr. Sues.
More fossils, more knowledge
The nearly completely represented skeleton of Anzu opens a window into the anatomy of this and other caenagnathid species. Armed with this wealth of new information, Dr. Lamanna and his team were able to reconstruct the evolution of these extraordinary animals in more detail than ever before. Analysis of the relationships of Anzu reaffirmed that caenagnathids form a natural grouping within Oviraptorosauria: Anzu, Caenagnathus, Chirostenotes, and other North American oviraptorosaurs are more closely related to each other than they are to most of their Asian cousins — a finding that had been disputed in recent years. Furthermore, the team’s analysis confirmed the recent hypothesis that the enormous (and aptly-named) Gigantoraptor — at a weight of at least 1.5 tons, the largest oviraptorosaur known to science — is an unusual member of Caenagnathidae as well, instead of an oviraptorid as had initially been proposed. “We’re finding that caenagnathids were an amazingly diverse bunch of dinosaurs,” says Dr. Lamanna. “Whereas some were turkey-sized, others — like Anzu and Gigantoraptor — were the kind of thing you definitely wouldn’t want to meet in a dark alley. Apparently these oviraptorosaurs occupied a much wider range of body sizes and ecologies than we previously thought.”
This image shows the skeleton and selected bones of the new oviraptorosaurian dinosaur species Anzu wyliei. Credit: Carnegie Museum of Natural History.
The anatomy and ancient environment of Anzu provide insight into the diet and habitat preferences of caenagnathids as well. Although the preferred food of these oviraptorosaurs remains something of a puzzle, Dr. Lamanna and collaborators think that caenagnathids were probably omnivores — like humans, animals that could eat either meat or plants. Moreover, studies of the rocks in which several of the most complete caenagnathid skeletons have been found show that these strata were laid down in humid floodplain environments, suggesting that these dinosaurs favored such habitats. In this way, caenagnathids appear to have differed greatly from their oviraptorid cousins, all of which have been found in rocks that were deposited under arid to semi-arid conditions . “Over the years, we’ve noticed that Anzu and some other Hell Creek Formation dinosaurs, such as Triceratops, are often found in mudstone rock that was deposited on ancient floodplains. Other dinosaurs, like duckbills, are found in sandstone deposited in or next to rivers,” says Dr. Lyson, who found his first Hell Creek fossil on his family’s ranch in North Dakota when he was only six years old.
Anzu led a life that was fraught with danger. In addition to sharing its Cretaceous world with the most notorious carnivore of all time — T. rex — this oviraptorosaur seems to have gotten hurt a lot as well. Two of the three specimens show clear evidence of injuries: one has a broken and healed rib, while the other has an arthritic toe bone that may have been caused by an avulsion fracture (where a tendon ripped a piece off the bone to which it was attached). Says Dr. Schachner, “These animals were clearly able to survive quite a bit of trauma, as two of the specimens show signs of semi-healed damage. Whether these injuries were the result of combat between two individuals or an attack by a larger predator remains a mystery.”
As much insight as the Anzu skeletons provide, paleontologists still have much to learn about North American oviraptorosaurs. Ongoing studies of these and other important fossils promise to remove more of the mystery surrounding these remarkable bird-like creatures. “For nearly a hundred years, we paleontologists knew almost nothing about these dinosaurs,” concludes Dr. Lamanna. “Now, thanks to Anzu, we’re finally starting to figure them out.”
A fully-articulated cast of Anzu wyliei is on public view in Carnegie Museum of Natural History’s Dinosaurs in Their Time exhibition.
Note : The above story is based on materials provided by Carnegie Museum of Natural History.
Researchers from USC and Nanjing University in China have documented evidence suggesting that part of the reason that Earth has become neither sweltering like Venus nor frigid like Mars lies with a built-in atmospheric carbon dioxide regulator — the geologic cycles that churn up the planet’s rocky surface. Credit: NASA Goddard Space Flight Center
Researchers from USC and Nanjing University in China have documented evidence suggesting that part of the reason that Earth has become neither sweltering like Venus nor frigid like Mars lies with a built-in atmospheric carbon dioxide regulator — the geologic cycles that churn up the planet’s rocky surface.
Scientists have long known that “fresh” rock pushed to the surface via mountain formation effectively acts as a kind of sponge, soaking up the greenhouse gas CO2. Left unchecked, however, that process would simply deplete atmospheric CO2 levels to a point that would plunge Earth into an eternal winter within a few million years during the formation of large mountain ranges like the Himalayas — which has clearly not happened.
And while volcanoes have long been pointed to as a source of carbon dioxide, alone they cannot balance out the excess uptake of carbon dioxide by large mountain ranges. Instead, it turns out that “fresh” rock exposed by uplift also emits carbon through a chemical weathering process, which replenishes the atmospheric carbon dioxide at a comparable rate.
“Our presence on Earth is dependent upon this carbon cycle. This is why life is able to survive,” said Mark Torres, lead author of a study disclosing the findings that appears in Nature on March 20. Torres, a doctoral fellow at the USC Dornsife College of Letters, Arts and Sciences, and a fellow at the Center for Dark Energy Biosphere Investigations (C-DEBI), collaborated with Joshua West, professor of Earth Sciences at USC Dornsife, and Gaojun Li of Nanjing University in China.
While human-made atmospheric carbon dioxide increases are currently driving significant changes in Earth’s climate, the geologic system has kept things balanced for million of years.
“The Earth is a bit like a big, natural recycler,” West said. Torres and West studied rocks taken from the Andes mountain range in Peru and found that weathering processes affecting rocks released far more carbon than previously estimated, which motivated them to consider the global implications of CO2 release during mountain formation.
The researchers noted that rapid erosion in the Andes unearths abundant pyrite — the shiny mineral known as “fool’s gold” because of its deceptive appearance — and its chemical breakdown produces acids that release CO2 from other minerals. These observations motivated them to consider the global implications of CO2 release during mountain formation.
Like many other large mountain ranges, such as the great Himalayas, the Andes began to form during the Cenozoic period, which began about 60 million years ago and happened to coincide with a major perturbation in the cycling of atmospheric carbon dioxide. Using marine records of the long-term carbon cycle, Torres, West, and Li reconstructed the balance between CO2 release and uptake caused by the uplift of large mountain ranges and found that the release of CO2 release by rock weathering may have played a large, but thus far unrecognized, role in regulating the concentration of atmospheric carbon dioxide over the last roughly 60 million years.
Note : The above story is based on materials provided by University of Southern California.
Two giant belts of radiation surround Earth. The inner belt is dominated by electrons and the outer one by protons. Credit: Image courtesy of NASA
Scientists have discovered a new, persistent structure in one of two radiation belts surrounding Earth. NASA’s twin Van Allen Probes spacecraft have shown that high-energy electrons in the inner radiation belt display a persistent pattern that resembles slanted zebra stripes. Surprisingly, this structure is produced by the slow rotation of Earth, previously considered incapable of affecting the motion of radiation belt particles, which have velocities approaching the speed of light.
Scientists had previously believed that increased solar wind activity was the primary force behind any structures in our planet’s radiation belts. However, these zebra stripes were shown to be visible even during low solar wind activity, which prompted a new search for how they were generated. That quest led to the unexpected discovery that the stripes are caused by the rotation of Earth. The findings are reported in the March 20, 2014, issue of Nature.
“It is because of the unprecedented resolution of our energetic particle experiment, RBSPICE, that we now understand that the inner belt electrons are, in fact, always organized in zebra patterns,” said Aleksandr Ukhorskiy, lead author of the paper at The Johns Hopkins Applied Physics Laboratory, or APL, in Laurel, Md. “Furthermore, our modeling clearly identifies Earth’s rotation as the mechanism creating these patterns. It is truly humbling, as a theoretician, to see how quickly new data can change our understanding of physical properties.”
Because of the tilt in Earth’s magnetic field axis, the planet’s rotation generates an oscillating, weak electric field that permeates through the entire inner radiation belt. To understand how that field affects the electrons, Ukhorskiy suggested imagining that the electrons are like a viscous fluid. The global oscillations slowly stretch and fold the fluid, much like taffy is stretched and folded in a candy store machine. The stretching and folding process results in the striped pattern observed across the entire inner belt, extending from above Earth’s atmosphere, about 500 miles above the planet’s surface up to roughly 8,000 miles.
As material moves through Earth’s radiation belts, it can fold over on itself like taffy, creating zebra stripes of electrons with different energies.
The radiation belts are dynamic doughnut-shaped regions around our planet, extending high above the atmosphere, made up of high-energy particles, both electrons and charged particles called ions, which are trapped by Earth’s magnetic field. Radiation levels across the belts are affected by solar activity that causes energy and particles to flow into near-Earth space. During active times, radiation levels can dramatically increase, which can create hazardous space weather conditions that harm orbiting spacecraft and endanger humans in space. It is the goal of the Van Allen Probes mission to understand how and why radiation levels in the belts change with time.
“The RBSPICE instrument has remarkably fine resolution and so it was able to bring into focus a phenomena that we previously didn’t even know existed,” said David Sibeck, the mission scientist for the Van Allen Probes at NASA’s Goddard Space Flight Center in Greenbelt, Md. “Better yet, we have a great team of scientists to take advantage of these unprecedented observations: We couldn’t have interpreted this data without analysis from strong theoreticians.”
Note : The above story is based on materials provided by NASA/Goddard Space Flight Center.
Chemical Formula: Mg2SiO4 Locality: Mte. Somma, Vesuvius, Italy. Name Origin: Named for Johann Forster, German naturalist.
Forsterite (Mg2SiO4; commonly abbreviated to Fo) is the magnesium rich end-member of the olivine solid solution series. Forsterite crystallizes in the orthorhombic system (space group Pbnm) with cell parameters a 4.75 Å (0.475 nm), b 10.20 Å (1.020 nm) and c 5.98 Å (0.598 nm).
Forsterite is associated with igneous and metamorphic rocks and has also been found in meteorites. In 2005 it was also found in cometary dust returned by the Stardust probe. In 2011 it was observed as tiny crystals in the dusty clouds of gas around a forming star.
Two polymorphs of forsterite are known: wadsleyite (also orthorhombic) and ringwoodite (isometric). Both are mainly known from meteorites.
Peridot is the gemstone variety of forsterite olivine.
Physical Properties
Cleavage: {001} Good, {010} Distinct Color: Colorless, Green, Yellow, Yellow green, White. Density: 3.21 – 3.33, Average = 3.27 Diaphaneity: Transparent Fracture: Conchoidal – Fractures developed in brittle materials characterized by smoothly curving surfaces, (e.g. quartz). Hardness: 6-7 – Orthoclase-Quartz Luminescence: Non-fluorescent. Luster: Vitreous (Glassy) Magnetism: Nonmagnetic Streak: white
Fluorite (yellow and purple duo) Minerva #1 Mine, Cave-in-Rock, Hardin Co., Illinois, USA Large Cabinet, 17.5 x 12.0 x 10.0 cm “Courtesy of Rob Lavinsky, The Arkenstone, www.iRocks.com”
Chemical Formula: CaF2 Locality: Common world wide. Name Origin: Named after its composition containing fluorine (Latin, fluere = “to flow”).
Fluorite (also called fluorspar) is the mineral form of calcium fluoride, CaF2. It belongs to the halide minerals. It crystallizes in isometric cubic habit, although octahedral and more complex isometric forms are not uncommon.
Fluorite is a colorful mineral, both in visible and ultraviolet light, and the stone has ornamental and lapidary uses. Industrially, fluorite is used as a flux for smelting, and in the production of certain glasses and enamels. The purest grades of fluorite are a source of fluoride for hydrofluoric acid manufacture, which is the intermediate source of most fluorine-containing fine chemicals. Optically clear transparent fluorite lenses have low dispersion, so lenses made from it exhibit less chromatic aberration, making them valuable in microscopes and telescopes. Fluorite optics are also usable in the far-ultraviolet range where conventional glasses are too absorbent for use.
Physical Properties
Cleavage: {111} Perfect, {111} Perfect, {111} Perfect Color: White, Yellow, Green, Red, Blue. Density: 3.01 – 3.25, Average = 3.13 Diaphaneity: Transparent to subtranslucent Fracture: Uneven – Flat surfaces (not cleavage) fractured in an uneven pattern. Hardness: 4 – Fluorite Luminescence: Fluorescent, Short UV=blue, Long UV=blue. Luster: Vitreous (Glassy) Streak: white
The Devonian is a geologic period and system of the Paleozoic Era spanning from the end of the Silurian Period, about 419.2 ± 3.2 Mya (million years ago), to the beginning of the Carboniferous Period, about 358.9 ± 0.4. It is named after Devon, England, where rocks from this period were first studied.
The Devonian period experienced the first significant adaptive radiation of terrestrial life. Free-sporing vascular plants began to spread across dry land, forming extensive forests which covered the continents. By the middle of the Devonian, several groups of plants had evolved leaves and true roots, and by the end of the period the first seed-bearing plants appeared. Various terrestrial arthropods also became well-established.Fish reached substantial diversity during this time, leading the Devonian to often be dubbed the “Age of Fish”. The first ray-finned and lobe-finned bony fish appeared, while the placoderms began dominating almost every known aquatic environment.
The ancestors of all tetrapods began adapting to walking on land, their strong pectoral and pelvic fins gradually evolved into legs. In the oceans, primitive sharks became more numerous than in the Silurian and the late Ordovician. The first ammonite mollusks appeared. Trilobites, the mollusk-like brachiopods and the great coral reefs, were still common. The Late Devonian extinction severely affected marine life, killing off all placoderms, and all trilobites, save for a few species of the order Proetida.
The paleogeography was dominated by the supercontinent of Gondwana to the south, the continent of Siberia to the north, and the early formation of the small continent of Euramerica in between.
History
The period is named after Devon, a county in southwestern England, where a controversial argument in the 1830s over the age and structure of the rocks found distributed throughout the county was eventually resolved by the defining of the Devonian period in the geological timescale. The Great Devonian Controversy is a classic case of how the foundations of our present-day geological knowledge and classification of the rock record and geological timescale was socially as well as scientifically constructed. After a long period of vigorous argument and counter-argument between the main protagonists of Roderick Murchison with Adam Sedgwick against Henry de la Beche supported by George Bellas Greenough, Murchison and Sedgwick won the debate and named the period they proposed as ‘The Devonian System’.
While the rock beds that define the start and end of the Devonian period are well identified, the exact dates are uncertain. According to the International Commission on Stratigraphy (Ogg, 2004), the Devonian extends from the end of the Silurian Period 419.2 ± 3.2 Mya, to the beginning of the Carboniferous Period 358.9 ± 0.4 Mya (in North America, the beginning of the Mississippian subperiod of the Carboniferous.
In nineteenth-century texts the Devonian has been called the “Old Red Age”, after the red and brown terrestrial deposits known in the United Kingdom as the Old Red Sandstone in which early fossil discoveries were found. Another common term is “Age of the Fishes”, referring to the evolution of several major groups of fish that took place during the period. Older literature on the Anglo-Welsh basin divides it into the Downtonian, Dittonian, Breconian and Farlovian stages, the latter three of which are placed in the Devonian.
The Devonian has also erroneously been characterized as a “greenhouse age”, due to sampling bias: most of the early Devonian-age discoveries came from the strata of western Europe and eastern North America, which at the time straddled the Equator as part of the supercontinent of Euramerica where fossil signatures of widespread reefs indicate tropical climates that were warm and moderately humid but in fact the climate in the Devonian differed greatly between epochs and geographic regions. For example, during the Early Devonian, arid conditions were prevalent through much of the world including Siberia, Australia, North America, and China, but Africa and South America had a warm temperate climate. In the Late Devonian, by contrast, arid conditions were less prevalent across the world and temperate climates were more common.
Subdivisions
The Devonian Period is formally broken into Early, Middle and Late subdivisions. The rocks corresponding to these epochs are referred to as belonging to the Lower, Middle and Upper parts of the Devonian System.
The Early Devonian lasts from 419.2 ± 2.8 to 393.3 ± 2.5 and begins with the Lochkovian stage, which lasts until the Pragian. This spans from 410.8 ± 2.8 to 407.6 ± 2.5, and is followed by the Emsian, which lasts until the Middle Devonian begins, 393.3± 2.7 million years ago. The Middle Devonian comprises two subdivisions, the Eifelian giving way to the Givetian 387.7± 2.7 million years ago. During this time the armoured jawless ostracoderm fish were declining in diversity; the jawed fish were thriving and increasing in diversity in both the oceans and freshwater. The shallow, warm, oxygen-depleted waters of Devonian inland lakes, surrounded by primitive plants, provided the environment necessary for certain early fish to develop essential characteristics such as well developed lungs, and the ability to crawl out of the water and onto the land for short periods of time.
Finally, the Late Devonian starts with the Frasnian, 382.7 ± 2.8 to 372.2 ± 2.5, during which the first forests were taking shape on land. The first tetrapods appear in the fossil record in the ensuing Famennian subdivision, the beginning and end of which are marked with extinction events. This lasted until the end of the Devonian, 358.9± 2.5 million years ago.
Climate
The Devonian was a relatively warm period, and probably lacked any glaciers. The temperature gradient from the equator to the poles was not as large as it today. The weather was also very arid, mostly along the equator where it was the driest. Reconstruction of tropical sea surface temperature from conodont apatite implies an average value of 30 °C (86 °F) in the Early Devonian. CO2 levels dropped steeply throughout the Devonian period as the burial of the newly evolved forests drew carbon out of the atmosphere into sediments; this may be reflected by a Mid-Devonian cooling of around 5 °C (9 °F). The Late Devonian warmed to levels equivalent to the Early Devonian; while there is no corresponding increase in CO2 concentrations, continental weathering increases (as predicted by warmer temperatures); further, a range of evidence, such as plant distribution, points to Late Devonian warming. The climate would have affected the dominant organisms in reefs; microbes would have been the main reef-forming organisms in warm periods, with corals and stromatoporoid sponges taking the dominant role in cooler times. The warming at the end of the Devonian may even have contributed to the extinction of the stromatoporoids.
Paleogeography
The Devonian period was a time of great tectonic activity, as Euramerica and Gondwana drew closer together.
The continent Euramerica (or Laurussia) was created in the early Devonian by the collision of Laurentia and Baltica, which rotated into the natural dry zone along the Tropic of Capricorn, which is formed as much in Paleozoic times as nowadays by the convergence of two great air-masses, the Hadley cell and the Ferrel cell. In these near-deserts, the Old Red Sandstone sedimentary beds formed, made red by the oxidized iron (hematite) characteristic of drought conditions.
Near the equator, the plate of Euramerica and Gondwana were starting to meet, beginning the early stages of assembling Pangaea. This activity further raised the northern Appalachian Mountains and formed the Caledonian Mountains in Great Britain and Scandinavia.
The west coast of Devonian North America, by contrast, was a passive margin with deep silty embayments, river deltas and estuaries, in today’s Idaho and Nevada; an approaching volcanic island arc reached the steep slope of the continental shelf in Late Devonian times and began to uplift deep water deposits, a collision that was the prelude to the mountain-building episode of Mississippian times called the Antler orogeny.
Sea levels were high worldwide, and much of the land lay under shallow seas, where tropical reef organisms lived. The deep, enormous Panthalassa (the “universal ocean”) covered the rest of the planet. Other minor oceans were Paleo-Tethys, Proto-Tethys, Rheic Ocean, and Ural Ocean (which was closed during the collision with Siberia and Baltica).
Sea levels in the Devonian were generally high. Marine faunas continued to be dominated by bryozoa, diverse and abundant brachiopods, the enigmatic hederelloids, microconchids and corals. Lily-like crinoids (animals, their resemblance to flowers notwithstanding) were abundant, and trilobites were still fairly common. Among vertebrates, jaw-less armored fish (ostracoderms) declined in diversity, while the jawed fish (gnathostomes) simultaneously increased in both the sea and fresh water. Armored placoderms were numerous during the lower stages of the Devonian Period and became extinct in the Late Devonian, perhaps because of competition for food against the other fish species. Early cartilaginous (Chondrichthyes) and bony fishes (Osteichthyes) also become diverse and played a large role within the Devonian seas. The first abundant genus of shark, Cladoselache, appeared in the oceans during the Devonian Period. The great diversity of fish around at the time, have led to the Devonian being given the name “The Age of Fish” in popular culture.
The first ammonites also appeared during or slightly before the early Devonian Period around 400 Mya.
A now dry barrier reef, located in present day Kimberley Basin of northwest Australia, once extended a thousand kilometers, fringing a Devonian continent. Reefs in general are built by various carbonate-secreting organisms that have the ability to erect wave-resistant frameworks close to sea level. The main contributors of the Devonian reefs were unlike modern reefs, which are constructed mainly by corals and calcareous algae. They were composed of calcareous algae and coral-like stromatoporoids, and tabulate and rugose corals, in that order of importance.
Terrestrial biota
By the Devonian Period, life was well underway in its colonization of the land. The moss forests and bacterial and algal mats of the Silurian were joined early in the period by primitive rooted plants that created the first stable soils and harbored arthropods like mites, scorpions and myriapods (although arthropods appeared on land much earlier than in the Early Devonian and the existence of fossils such as Climactichnites suggest that land arthropods may have appeared as early as the Cambrian period). Also the first possible fossils of insects appeared around 416 Mya in the Early Devonian. The first tetrapods, evolving from lobe-finned fish, appeared in the coastal water no later than middle Devonian, and gave rise to the first Amphibians.
The greening of land
Early Devonian plants did not have roots or leaves like the plants most common today and many had no vascular tissue at all. They probably spread largely by vegetative growth, and did not grow much more than a few centimeters tall. By far the largest land organism was Prototaxites, the fruiting body of an enormous fungus that stood more than 8 meters tall, towering over the low, carpet-like vegetation. By the Middle Devonian, shrub-like forests of primitive plants existed: lycophytes, horsetails, ferns, and progymnosperms had evolved. Most of these plants had true roots and leaves, and many were quite tall. The earliest known trees, from the genus Wattieza, appeared in the Late Devonian around 385 Ma. In the Late Devonian, the tree-like ancestral Progymnosperm Archaeopteris which had conifer-like true wood and fern-like foliage and the cladoxylopsids grew. These are the oldest known trees of the world’s first forests. By the end of the Devonian, the first seed-forming plants had appeared. This rapid appearance of so many plant groups and growth forms has been called the “Devonian Explosion”.
The ‘greening’ of the continents acted as a carbon dioxide sink, and atmospheric levels of this greenhouse gas may have dropped. This may have cooled the climate and led to a massive extinction event. See Late Devonian extinction.
Animals and the first soils
Primitive arthropods co-evolved with this diversified terrestrial vegetation structure. The evolving co-dependence of insects and seed-plants that characterizes a recognizably modern world had its genesis in the Late Devonian period. The development of soils and plant root systems probably led to changes in the speed and pattern of erosion and sediment deposition. The rapid evolution of a terrestrial ecosystem containing copious animals opened the way for the first vertebrates to seek out a terrestrial living. By the end of the Devonian, arthropods were solidly established on the land.
Late Devonian extinction
A major extinction occurred at the beginning of the last phase of the Devonian period, the Famennian faunal stage, (the Frasnian-Famennian boundary), about 372.2 ± 1.6 Mya, when all the fossil agnathan fishes, save for the psammosteid heterostracans, suddenly disappeared. A second strong pulse closed the Devonian period. The Late Devonian extinction was one of five major extinction events in the history of the Earth’s biota, more drastic than the familiar extinction event that closed the Cretaceous.
The Devonian extinction crisis primarily affected the marine community, and selectively affected shallow warm-water organisms rather than cool-water organisms. The most important group to be affected by this extinction event were the reef-builders of the great Devonian reef-systems.Amongst the severely affected marine groups were the brachiopods, trilobites, ammonites, conodonts, and acritarchs, as well as jawless fish, and all placoderms. Land plants as well as freshwater species, such as our tetrapod ancestors, were relatively unaffected by the Late Devonian extinction event.The reasons for the Late Devonian extinctions are still unknown, and all explanations remain speculative.Canadian paleontologist Digby McLaren suggested in 1969 that the Devonian extinction events were caused by an asteroid impact. However, while there were Late Devonian collision events (see the Alamo bolide impact), little evidence supports the existence of a large enough Devonian crater.
Note : The above story is based on materials provided by Wikipedia
Map of the Irtysh River, (a tributary of the Ob River) which drains northern Kazakhstan, a bit of southern Russia, and a tiny bit of western China.
The Irtysh River is a river in Siberia and Kazakhstan and is the chief tributary of the Ob River.
Irtysh’s main affluents are the Tobol River and the Ishim River. The Ob-Irtysh system forms a major drainage basin in Asia, encompassing most of Western Siberia and the Altai Mountains.
Geography
From its origins as the Kara-Irtysh (Black Irtysh) in the Mongolian Altay mountains in Xinjiang, China, the Irtysh flows northwest through Lake Zaysan in Kazakhstan, meeting the Ishim and Tobol rivers before merging with the Ob near Khanty-Mansiysk in western Siberia, Russia after 4,248 kilometres (2,640 mi).
The name Black Irtysh (Kara-Irtysh in Kazakh, or Cherny Irtysh in Russian) is applied by some authors, especially in Russia and Kazakhstan, to the upper course of the river, from its source entering Lake Zaysan. The term White Irtysh, in opposition to the Black Irtysh, was occasionally used in the past to refer to the Irtysh below lake Zaysan; now this usage is largely obsolete.
History
A number of Mongol and Turkic peoples occupied the river banks for many centuries. In 657, Tang Dynasty general Su Dingfang defeated Ashina Helu, qaghan of the Western Turkic Khaganate, at the Battle of Irtysh River, ending the Tang campaign against the Western Turks. Helu’s defeat ended the Khaganate, strengthened Tang control of Xinjiang, and led to Tang suzerainty over the western Turks.
In the 15th and 16th centuries the lower and middle courses of the Irtysh lay within the Tatar Khanate of Sibir, which the Russians conquered in the 1580s. In the 17th century the Zunghar Khanate, formed by the Mongol Oirat people, became Russia’s southern neighbor, and controlled the upper Irtysh. The Russians founded the cities of Omsk in 1716, Semipalatinsk in 1718, Ust-Kamenogorsk in 1720, and Petropavlovsk in 1752.
The Chinese Qing Empire conquered the Zunghar state in the 1750s. This prompted an increase in the Russian authorities’ attention to their borderland; in 1756, the Orenburg Governor Ivan Neplyuyev even proposed the annexation of the Lake Zaysan region, but this project was forestalled by Chinese successes. Concerns were raised in Russia (1759) about the (theoretical) possibility of a Chinese fleet sailing from Lake Zaysan down the Irtysh and into Western Siberia. A Russian expedition visited Lake Zaysan in 1764, and concluded that such a riverine invasion would not be likely. Nonetheless, a chain of Russian pickets was established on the Bukhtarma River, north of Lake Zaysan. Thus the border between the two empires in the Irtysh basin became roughly delineated, with a (sparse) chain of guard posts on both sides.
The situation in the borderlands in the mid-19th century is described in a report by A.Abramof (1865). Even though the Zaysan region was recognized by both parties as part of the Qing Empire, it had been annually used, by fishing expeditions sent by the Siberian Cossack Host. The summer expeditions started in 1803, and in 1822-25 their range was expanded through the entire Lake Zaysan and to the mouth of the Black Irtysh. Through the mid-19th century, the Qing presence on the upper Irtysh was mostly limited to the annual visit of the Qing amban from Chuguchak to one of the Cossacks’ fishing stations (Batavski Piket).
The border between the Russian and the Qing empires in the Irtysh basin was established along the line fairly similar to China’s modern border with Russia and Kazakhstan by the Convention of Peking of 1860.The actual border line pursuant to the convention was drawn by the Protocol of Chuguchak (1864), leaving Lake Zaysan on the Russian side.The Qing Empire’s military presence in the Irtysh basin crumbled during the Dungan revolt (1862–77). After the fall of the rebellion and the reconquest of Xinjiang by Zuo Zongtang, the border between the Russian and the Qing empires in the Irtysh basin was further slightly readjusted, in Russia’s favor, by the Treaty of Saint Petersburg (1881).
Note : The above story is based on materials provided by Wikipedia
In the Persian Gulf, two tectonic plates-rigid pieces of the Earth’s crust-are colliding; the Arabian plate (lower left) is running up on the Eurasian plate (upper right). Credit: Banco de Imágenes Geológicas
Reasearch led by West Australian scientists into ‘subduction’ during tectonic plate collisions has provided new insights into the global sulphur cycle.
Subduction is a process that occurs at tectonic plate boundaries whereby one plate moves under the other and into the mantle as the two plates converge.
As a part of the subduction process material from the colliding tectonic plates is either ‘squeezed’ straight back out as a superheated fluid, transferred to the sub arc mantle as magma or deposited into the deeper mantle.
Curtin University researcher Dr Katy Evans says very little is known about the fundamental processes that occur in these subduction zones.
“This is one of the methods by which we cycle stuff that is on the outside of the earth onto the inside of the earth,” she says.
“The earth’s atmosphere and oceans are highly oxidised … so the process of subduction is taking stuff that’s quite oxidised and delivering it inside the earth to a place that’s quite reduced.
“We don’t really know what the potential consequences of that are.”
Dr Evans says the question of whether the area just above the subduction zone is oxidised relative to the rest of the earth’s mantle is one that is highly contested.
“Sulphur is one of the things that has the potential to cause that oxidation,” she says.
Dr Evans carried out much her of research through examination of exhumed rocks in the Zermatt-Saas zone of the Alps—rocks that were ‘spat back out’ during the formation of the Alps as the African and Eurasian tectonic plates collided.
“We looked at the sulphur in those rocks to see what sort of evidence there was to suggest whether sulphur goes all the way into the deep mantle, off into the sub-arc mantle or whether it comes out in those early fluids,” she says.
They discovered oxidised sulphur in exhumed rocks that had been up to 60km deep in the earth.
“At this point [oxidised sulphur] is still available,” she says.
“It means you probably have a method for oxidising the sub-arc mantle.”
Dr Evans says arc deposits are mineral rich, meaning her research could have significant implications for exploration into the future.
“If we know that a certain type of subduction zone is going to provide the right kind of conditions for ore deposits to form then instead of looking at all subduction zones we can really start to target effectively,” she says.
“Arc deposits provide almost 75 per cent of global copper supply, 50 per cent of molybdenum, most of the rhenium, 20 per cent of gold and a whole bunch of other elements.”
Note : The above story is based on materials provided by Science Network WA
