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43-580: Studies in the 2010s suggest that the craton can be separated into three crustal blocks since they show different accretionary history (i.e., the history of block collisions). The craton includes the western, central and eastern blocks and the three blocks are divided by several shear zones . The lithologies of the Dharwar Craton are mainly TTG (Tonalite-trondhjemite-granodiorite) gneisses , volcanic-sedimentary greenstone sequences and calc-alkaline granitoids . The western Dharwar Craton contains

86-408: A network of radiation damaged areas. Fission tracks and micro-cracks within the crystal will further extend this radiation damage network. These fission tracks act as conduits deep within the crystal, providing a method of transport to facilitate the leaching of lead isotopes from the zircon crystal. Under conditions where no lead loss or gain from the outside environment has occurred, the age of

129-401: A sample of the mineral can be used to reliably determine its age. The method relies on two separate decay chains , the uranium series from U to Pb, with a half-life of 4.47 billion years and the actinium series from U to Pb, with a half-life of 710 million years. Uranium decays to lead via a series of alpha and beta decays, in which U and its daughter nuclides undergo

172-449: A series of zircon samples has lost different amounts of lead, the samples generate a discordant line. The upper intercept of the concordia and the discordia line will reflect the original age of formation, while the lower intercept will reflect the age of the event that led to open system behavior and therefore the lead loss; although there has been some disagreement regarding the meaning of the lower intercept ages. Undamaged zircon retains

215-470: A single decay scheme (usually U to Pb) leads to the U–Pb isochron dating method, analogous to the rubidium–strontium dating method. Finally, ages can also be determined from the U–Pb system by analysis of Pb isotope ratios alone. This is termed the lead–lead dating method. Clair Cameron Patterson , an American geochemist who pioneered studies of uranium–lead radiometric dating methods, used it to obtain one of

258-422: A total of eight alpha and six beta decays, whereas U and its daughters only experience seven alpha and four beta decays. The existence of two 'parallel' uranium–lead decay routes ( U to Pb and U to Pb) leads to multiple feasible dating techniques within the overall U–Pb system. The term U–Pb dating normally implies the coupled use of both decay schemes in the 'concordia diagram' (see below). However, use of

301-443: Is a process by which material is added to a tectonic plate at a subduction zone , frequently on the edge of existing continental landmasses . The added material may be sediment, volcanic arcs , seamounts , oceanic crust or other igneous features. Accretion involves the addition of material to a tectonic plate via subduction , the process by which one plate is forced under the other when two plates collide. The plate which

344-418: Is being forced down, the subducted plate, is pushed against the upper, over-riding plate. Sediment on the ocean floor of the subducting plate is often scraped off as the plate descends. This accumulated material is called an accretionary wedge (or accretionary prism), which is pushed against and attaches to the upper plate. In addition to accumulated ocean sediments, volcanic island arcs or seamounts present on

387-839: Is made up of multiple accreted terranes that collided with the Laurentian proto-continent , such as the Proterozoic Yavapai , Mazatzal , and Grenville Province Terranes. Accreted terranes along modern subduction plate boundaries include the Nankai accretionary complex of Japan (subduction of the Philippine Plate beneath the Eurasian Plate ), the Barbados Ridge in the Caribbean (subduction of

430-535: Is no sanukitoid record in the western block. However, there are a lot of granitoid intrusions in the central block, which become less in the eastern block. Anatectic granite is a kind of rock formed by the partial melting of the pre-existing crustal rock, which is relatively younger than the TTG and greenstone in the Dharwar Craton. The granites usually cut across the older rocks. When the rocks were under subductions, they experienced high temperature and pressure leading to

473-867: The Caribbean Plate beneath the North American Plate ), and the Mediterranean Ridge (subduction of the African Plate beneath the Eurasian Plate). These examples of accreted terranes also all include accretionary wedges. Uranium%E2%80%93lead dating Uranium–lead dating , abbreviated U–Pb dating , is one of the oldest and most refined of the radiometric dating schemes. It can be used to date rocks that formed and crystallised from about 1 million years to over 4.5 billion years ago with routine precisions in

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516-430: The 0.1–1 percent range. The method is usually applied to zircon . This mineral incorporates uranium and thorium atoms into its crystal structure , but strongly rejects lead when forming. As a result, newly-formed zircon crystals will contain no lead, meaning that any lead found in the mineral is radiogenic . Since the exact rate at which uranium decays into lead is known, the current ratio of lead to uranium in

559-410: The 2 latest major accretion events occurring in 2700 Ma and 2560 Ma with massive continental growth. Crustal reworking means the old rocks ( protoliths ) are destroyed and regenerated into new rocks. The continental crust is relatively old if the crust experienced crustal reworking events. For the rocks that experienced crustal reworking, minerals like zircon, which is difficult to melt, are preserved in

602-502: The Dharwar Craton includes the western block and eastern block. The mylonite zone at the eastern boundary of the Chitradurga greenstone belt is the margin between the western block and the eastern block. The Chitradurga greenstone belt is an elongated linear supracrustal belt which is 400 km long from North to South. Cratonisation is an important process to form a craton with sufficient and stable continental masses. In terms of

645-432: The Dharwar Craton, which includes the typical TTG-type gneisses (i.e., traditional TTG with a major component of quartz and plagioclase) and the dark grey TTG banded gneisses (relatively more potassium feldspar than typical TTG gneisses): Greenstone is metamorphosed mafic to ultramafic volcanic rock that formed in volcanic eruptions in the early stage of Earth formation. The volcanic-sedimentary greenstone sequence occupies

688-428: The ages of the blocks, the western blocks is older with a cratonisation age around 3.0 Ga while the eastern block is younger with the cratonisation age around 2.5 Ga. TTG rocks are intrusive rocks with a granitic composition of quartz and feldspar but contain less potassium feldspar. In Archean craton, TTG rocks are usually present in batholiths formed by plate subduction and melting. Two kinds of gneisses can be found on

731-509: The ages of the events. According to the zircon U-Pb ages of the TTG gneisses from the Dharwar Craton, there were 5 major accretion events leading to the formation of the Archean felsic continental crust. The events occurred with the ranges of age 3450–3300, 3230–3200, 3150–3000, 2700–2600 and 2560–2520 million years ago ( Ma ). The western block records the two earliest crust accretion events, that happened in 3450 Ma and 3230 Ma. The rates of

774-412: The block, which happened in 2640–2620 Ma. The reworking event is related to the greenstone volcanism of the TTG accretion event in 2700 Ma. Before 3400 Ma, the magma upwelling from the mantle led to the intraplate hotspot setting. The upwelling magma formed the oceanic plateaus with komatiites and komatiitic basalts in the oceanic crust. After the mantle plume hotspots were formed, the tectonic setting

817-452: The chemical alteration of the mantle wedge and the melting of the wedge. The peridotitic mantle wedge was mixed with intermediate to felsic melts. This can be explained by the mixing of the previous TTG melts. The sanukitoids created by plume setting would lead to the sanukitoid intrusions with high magnesium content and low silicon dioxide. The sanukitoid magmatism is not related to the TTG accretion events during 3450–3000 Ma. The magmatism

860-491: The chemical changes and textural changes of rocks (i.e., metamorphism ). The mineral assemblages of the metamorphic rocks can tell us how high the temperature and pressure are when they are under the peak metamorphism (the progress with the highest pressure and temperature). The metamorphic rocks in the Dharwar Craton usually recorded the mineral assemblages from amphibolite facies to granulite facies: Gundlupet region B.R Hills region Krishnagiri - Dharmapuri region,

903-461: The continental growth of the two events are fast since the events led to the widespread of greenstone volcanism. The central block records 4 major accretion events, that occurred in 3375 Ma, 3150 Ma, 2700 Ma and 2560 Ma. The isotopic data suggests that the scale of the continental growth due to felsic crust accretion was large during 2700–2600 Ma and 2560–2520 Ma, leading to the large-scale greenstone volcanism at that time. The eastern block records

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946-751: The earliest estimates of the age of the Earth in 1956 to be 4.550Gy ± 70My; a figure that has remained largely unchallenged since. Although zircon (ZrSiO 4 ) is most commonly used, other minerals such as monazite (see: monazite geochronology ), titanite , and baddeleyite can also be used. Where crystals such as zircon with uranium and thorium inclusions cannot be obtained, uranium–lead dating techniques have also been applied to other minerals such as calcite / aragonite and other carbonate minerals . These types of minerals often produce lower-precision ages than igneous and metamorphic minerals traditionally used for age dating, but are more commonly available in

989-400: The emplacement of granite. The second reworking event led to the emplacement of 2640–2600 Ma of granites. For the central block, the event happened in 3140 Ma is considered as the earliest crustal reworking due to the TTG accretion event between 3230–3140 Ma in the central block of the craton. For the eastern block, the second highest-temperature reworking event was recorded in the centre of

1032-444: The geologic record. During the alpha decay steps, the zircon crystal experiences radiation damage, associated with each alpha decay. This damage is most concentrated around the parent isotope (U and Th), expelling the daughter isotope (Pb) from its original position in the zircon lattice. In areas with a high concentration of the parent isotope, damage to the crystal lattice is quite extensive, and will often interconnect to form

1075-422: The incompatible elements could be account for the high-angle subduction and the chemical interaction between the mantle wedge and the melt from the subducted crust. During the 2700 Ma, the central and eastern block of the Dharwar Craton had developed into microcontinents . The weathering and erosion of the microcontinents led to a large amount of detrital input to the ocean floor and subduction zone. Therefore,

1118-580: The lead generated by radioactive decay of uranium and thorium up to very high temperatures (about 900 °C), though accumulated radiation damage within zones of very high uranium can lower this temperature substantially. Zircon is very chemically inert and resistant to mechanical weathering – a mixed blessing for geochronologists, as zones or even whole crystals can survive melting of their parent rock with their original uranium–lead age intact. Thus, zircon crystals with prolonged and complicated histories can contain zones of dramatically different ages (usually with

1161-401: The mafic to ultramafic hydrous melt formed by the slab melting melted the base of the thickened oceanic arc crust, which formed the TTG melt, as well as magmatic protoliths of TTGs in the oceanic arc crust. During 3230–3100 Ma, the continuous collision of the oceanic island arc crust, the TTG and oceanic plateaus, that are formed in the previous stage, caused the melting of the juvenile crust in

1204-493: The magma transferred into the surrounding rock leading to the partial melting of gneisses and the formation of calc-alkaline granitoids. Sanukitoids were formed during the Neoarchean magmatic accretion events, that are originated from the mantle with low silicon dioxide and high magnesium. The sanukitoid magma could be generated by either plate subduction or plume setting. The sanukitoids created by subduction might lead to

1247-424: The majority of the Archean crustal record, which is about 30%. The western block comprises the greenstone sequences with adequate sediments, while the central block and the eastern block comprise the greenstone sequences with adequate volcanic rocks but minor sediments. Sanukitoids are granitoids with high-magnesium composition that are commonly formed by plate collision events in Archean. In the Dharwar Craton, there

1290-700: The melting of subducted oceanic crust and the melting of thickened oceanic arc crust. The continuous melting of oceanic arc crust and mantle upwelling generated the TTG and sanukitoid plutons over the Dharwar Craton. As the Dharwar Craton is located in southern India, it is geographically surrounded by the Arabian Sea , the Deccan Trap , the Eastern Ghats Mobile Belt and the Southern Granulite Belt. Traditionally,

1333-468: The notation can be ignored.) These are said to yield concordant ages ( t from each equation 1 and 2). It is these concordant ages, plotted over a series of time intervals, that result in the concordant line. Loss (leakage) of lead from the sample will result in a discrepancy in the ages determined by each decay scheme. This effect is referred to as discordance and is demonstrated in Figure ;1. If

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1376-432: The oceanic crust, and are therefore not easily subducted along with the oceanic crust that surrounds them. Instead, these less-dense bits of crust will collide with existing continental crust on the upper plate once the oceanic crust separating them is completely subducted. Most continents are composed of multiple accreted " terranes ", pieces of low-density continental crust with different origins. For example, North America

1419-518: The oceanic island arc, which generated trondhjemite plutons in 3200 Ma. The trondhjemite emplacement generated heat and fluid that led to the melting that made the low-density TTG crust rose while the high-density greenstone volcanics sank, which developed the dome-keel structures between the TTG and greenstone. The transitional TTGs, which were recorded in the central and eastern blocks, was formed during 2700–2600 Ma. The transitional TTGs are relatively enriched in incompatible elements . The enrichment of

1462-418: The oldest basement rocks, with greenstone sequences between 3.0-3.4 Ga, whereas the central block of the craton mainly contains migmatitic TTG gneisses, and the eastern block contains 2.7 Ga greenstone belts and calc-alkaline plutons . The formation of the basement rock of the Dharwar Craton was created by intraplate hotspots (i.e., volcanic activities caused by mantle plumes from the core-mantle boundary),

1505-464: The reworked rocks. Some new zircons with a younger age would be formed in the reworking events. The crustal reworking events happened in the time range of 3100–3000 Ma. All 3 crustal blocks record the crustal reworking events in 2520 Ma due to the final assembly of the Superia supercontinent. For the western block, there are two reworking events. The first event happened in 3100–3000 Ma accounting to

1548-444: The southern part of the eastern block Accretions mean the collisions between plates leading to the plate subduction. Crust accretions are important in the Dharwar Craton since the continuous volcanic eruptions caused by accretions led to the formation of Archean felsic continent crust. For finding when the Archean crust accretions happened, the parent-daughter isotopes dating, like uranium-lead (U-Pb) decay could be used to find out

1591-475: The subducted slab with a large amount of sediment brought incompatible elements into the mantle due to a high-angle subduction. The mantle wedge interacted with the slab, leading to the partial enrichment of the incompatible elements in the wedge and generated mafic to intermediate magma. The mafic magma rose and accumulated under the oceanic arc crust, leading to the partial melting of the thickened, incompatible element enriched arc crust and their magma mixed to form

1634-409: The subducting plate may be amalgamated onto existing continental crust on the upper plate, increasing the continental landmass. Continental crust differs significantly from oceanic crust. Oceanic crust is primarily composed of basaltic rocks, which have a higher density than the rocks making up the majority of continental crust. Island arcs and other volcanic rocks are also lower in density than

1677-673: The three blocks joined together to form the Dharwar Craton and all the subduction zones closed, followed by the regional metamorphism due to heat release from the mantle during 2535–2500 Ma. The final cratonisation finished in 2400 Ma through slow cooling. [REDACTED] Africa [REDACTED] Antarctica [REDACTED] Asia [REDACTED] Australia [REDACTED] Europe [REDACTED] North America [REDACTED] South America [REDACTED] Afro-Eurasia [REDACTED] Americas [REDACTED] Eurasia [REDACTED] Oceania Accretion (geology) In geology , accretion

1720-467: The transitional TTGs during 2700–2600 Ma. After the transitional TTG accretion, the inflexible subducted oceanic crust broke and fell into the asthenosphere , leading to the mantle upwelling under the pre-existing crust. The upwelling mantle rock rose to the shallow depth and melted the upper mantle to generate intermediate to mafic magma. Then, the magma intruded into the middle part of the crust. It underwent differentiation in magma chambers. The heat from

1763-451: The zircon can be calculated by assuming exponential decay of uranium. That is where This gives which can be written as The more commonly used decay chains of Uranium and Lead gives the following equations: (The notation Pb ∗ {\displaystyle {\text{Pb}}^{*}} , sometimes used in this context, refers to radiogenic lead. For zircon, the original lead content can be assumed to be zero, and

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1806-463: Was followed by the transitional TTG accretion event in 2600 Ma and only occurred in the central and eastern blocks. Since the sanukitoids are enriched in both incompatible and compatible elements, while the TTGs are not, it indicates the appearance of the sanukitoid magmatism shows the tectonic change from melting of oceanic crust to melting of mantle during the period of 2600–2500 Ma. During 2560–2500 Ma,

1849-456: Was followed by the two-stage melting, which include the melting of the subducted oceanic crust and the melting of the thickened oceanic arc crust. In 3350 Ma, due to the ridge push from the oceanic spreading centres ( mid-oceanic ridges ), some oceanic crust subducted under the mantle. The subduction led to the melting of the subducted crust and formed magma that rose to the oceanic crust and formed oceanic island arc crust. During 3350–3270 Ma,

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