Solidus Liquidous Graph How to Read Geology

H2o Solution Mechanisms and Construction

Bjorn Mysen , Pascal Richet , in Silicate Glasses and Melts (Second Edition), 2019

15.four.three Crystallization, Melting, and Construction

The solidus temperature decrease of silicates caused past dissolved h2o is in office because of the dilution of the silicate solution past dissolved water, and in part because of the nature of the interaction between dissolved water and the silicate structure. Notably, h2o causes a larger depression of the solidus temperature of highly polymerized melt systems compared with depolymerized silicate systems (encounter Chapter 14, Fig. fourteen.1). This difference probably results from the fact that depolymerized melts are less prone to further fragmentation than highly polymerized melts in the absence of H_iiO (run into likewise Fig. fourteen.16). Moreover, in highly depolymerized melts, free M single bond OH complexes become important and increasingly so with increasing Grand/Si-affluence ratio of the melt (Xue and Kanzaki, 2004; Cody et al., 2005). This mechanism has an overall effect of reducing the degreee of polymerization of the melt, which also explains why the enstatite + forsterite eutectic in the MgO-SiO₂-H_iiO system shifts to more silica-rich compositions at very high force per unit area (Luth, 1993; Xue and Kanzaki, 2008; Yamada et al., 2007).

Depolymerization of a melt via solution of water also leads to a subtract of the action of SiO₂ considering the interconnected silicate network of an anhydrous melt is cleaved upwards to class less polymerized entities and OH groups (Eq. xv.1). As a issue of the decreased silicate activity, liquidus volumes of polymerized silicate minerals shrink relative to less polymerized minerals. A classic instance of this result is the observation that at high force per unit area, enstatite (MgSiO_three) melts congruently at least to 3 GPa pressure (Boyd et al., 1964), whereas in the presence of excess H₂O, enstatite melts incongruently to form olivine + melt (Kushiro et al., 1968).

An implication of these features is that the effect of dissolved water on the activity of SiO₂ in a silicate melt is positively correlated with the OH/H₂O abundance ratio. This, in plough, implies not merely more reduction of a _SiO2 with increasing water content of a given melt composition (Fig. xv.i), it besides implies that any other melt compositional variable affecting the OH/H₂O will bear on the extent to which water affects the a _SiO2. One might expect, for case, that with decreasing ionization potential of a network-modifying cation, the influence of H₂O on a _SiO2 would decrease considering of the positive correlation between OH/H_twoO and the ionization potential.

Related to the behavior of OH groups in aluminosilicate melts is the shift in the "granite minimum" (Tuttle and Bowen, 1958; Luth et al., 1964) away from the SiO₂ noon toward more feldspar-rich compositions with increasing water pressure, P _H2O. This shift, in turn, is related to interaction between dissolved h2o and the alkali aluminate components in the melt. For compositions as aluminous every bit those respective to the granite minimum, structural data summarized previously (Mysen and Virgo, 1986b; Schmidt et al., 2000; Malfait and Xue, 2014) point that dissolved h2o interacts increasingly with Al^{iii +}. As a consequence, the activity of feldspar components in the system decreases relative to that of SiO₂, thus leading to the expansion of the liquidus book of quartz relative to feldspar.

Read full chapter

URL:

https://www.sciencedirect.com/scientific discipline/commodity/pii/B9780444637086000156

Including Actinides

Volodymyr Babizhetskyy , ... Herwig Michor , in Handbook on the Physics and Chemistry of Rare Earths, 2017

3.2.2 Sc–V–C

The previous overview on the Sc–Five–C system has been done past Kotur and Gratz [5]. Additional details and updates are provided here.

The offset solidus surface projection of the Sc–V–C system was evaluated theoretically by Velikanova et al. [90]. Taking into business relationship the difference betwixt the unit cell parameters of cubic grouping 4–VI d-transition element carbides (Δa/a × 100% = 13, which is greater than the established limiting value of 11%), no csss betwixt isomorphous ScC_x and VC_{1 − x} was predicted. Preliminary experimental results concerning phase equilibria in the Sc–V–C system at subsolidus temperatures were reported in Ref. [92]. The solidus surface project of the Sc–Five–C stage diagram based on the data of Ref. [92] is shown in Fig. xix. Predicted earlier [90] limited mutual solubility of ScC_ten and VC_{one − 10} carbides has been confirmed in Ref. [92]. However, the solubilities were considerably larger than those projected in Ref. [90]. Maximum crystallization temperatures observed are those for the formation of VC_{1 − 10} (2800°C) and ScC_x (2770°C). No ternary compounds have been constitute.

Read full chapter

URL:

https://www.sciencedirect.com/scientific discipline/article/pii/S0168127317300181

Crustal and Lithosphere Dynamics

B.D. Marsh , in Treatise on Geophysics (Second Edition), 2015

vi.07.2.3 Solidification Fronts

Between the liquidus and solidus, the magma is a physical and chemical mixture of liquid (cook) and crystals (and perhaps bubbles). The properties of this mixture are complex and exceedingly important at every stage in a magma's life in determining the set of dominant physical and chemical processes involved in shaping the magma's beliefs and chemical evolution. Figure 4 shows the buildup of crystals with decreasing temperature between the liquidus and solidus for typical basalts. Nucleation and growth of crystals begins at the liquidus, by definition, and with decreasing temperature crystallinity (ϕ, or crystal fraction) at first builds upward slowly and and so more rapidly as crystallinity reaches 50 vol.% afterward which it again builds increasingly slowly with approach to the solidus. Near the liquidus, where crystallinity is low and crystals are pocket-sized, the magma is a suspension. Hither, the crystals can settle relative to ane another without much hindrance from one another, but since they are small, settling is slow. This state holds to a crystallinity of virtually 25 vol.% where the viscosity of the mass (see the succeeding text) has increased by a factor of ten over that at the liquidus and the crystals now 'feel' the presence of 1 another as they movement. Motion of a unmarried crystal causes a shear menstruation extending out ~ 10 radii, which entrains neighboring crystals. There is besides some observational (Marsh, 1998) and experimental (Philpotts and Carroll, 1996) evidence that, especially in plagioclase-begetting basaltic magmas, a 'craven-wire' network of crystals may develop that gives a sure structure and force to the magma. Across the suspension zone where crystals are (ideally) still separated from one some other is the mush zone, which persists until the crystallinity reaches the land of maximum packing where the crystals are all touching. This occurs when crystallinity reaches about 55 vol.% (ϕ ~ 0.55). At this point, the crystals are tacked or welded together to course a solid framework of some strength (e.g., Marsh, 2002). In essence, the magma is at present a partially molten rock and tin can no longer flow every bit a viscous fluid. The remaining melt, which is interstitial to the crystals, can withal move as a porous or the Darcy menses (e.g., Hersum et al., 2005). Because of this overall strength, which is found in Hawaiian lava lakes to exist drillable, this cooler region is called the rigid crust. These three zones, then, pause, mush, and rigid crust, make upward all magmatic solidification fronts. A solidification forepart (meet Figure 5 ) is the active zone of crystallization that forms the perimeter of all magmas. Solidification fronts are dynamic in the sense that they continually move in response to the prevailing thermal government or land of heat transfer from (or sometimes to) the magma. All crystallization, past definition, takes place within solidification fronts. And information technology is inside these fronts that all concrete and chemical processes accept place to modify the magma composition and texture. Beyond the solidification fronts, in the magma interior, in that location are no new crystals and hence no processes operate there to separate crystals and melt (more in the succeeding text).

As magma approaches the indicate of maximum crystal packing, where ϕ ~ 0.55, it undergoes a dramatic rheological transition. Information technology becomes a dilatant solid, which means that the mass of crystals and melt upon being sheared expands as neighboring solids try to motility outward and around one another to accommodate the shear. When this condition is reached for magma in the throat of a volcano, the volcano becomes plugged and tin can no longer emit lava. With continued cooling and crystallization in the magma below, gases exsolve that tin build pressure to the point of catastrophic failure of the entire edifice. This condition volition exist discussed again soon. The dynamics of solidification fronts measure the dynamics, especially the rate of cooling, of every magma from deep chambers to lava flows.

Read full affiliate

URL:

https://www.sciencedirect.com/science/article/pii/B9780444538024001160

Volume 2

Gautam Sen , Robert J. Stern , in Encyclopedia of Geology (Second Edition), 2021

Melting and Melt Limerick

Melting tin can but occur when the solidus temperature is exceeded; therefore, information technology is important to determine the solidi of both hydrous drape wedge and subducted sediments and altered oceanic crust, preferably at about three–v GPa, the pressure of the slab that lies deeper than where drape wedge melting occurs.

Fig. 19 shows that there is a large discrepancy betwixt different experimental studies about the location of H₂O-saturated lherzolite solidus. For cooler to boilerplate temperature gradients (dT/dP) of the slab/wedge interface, the top of the chlorite-bearing slab will brainstorm to cook if Till et al.'southward (2012) solidus is correct; and on the other paw, excluding very warm slabs, "normal" slabs will non more often than not cook if the higher solidi are correct. In this diagram a possible fluid path is shown: fluids will motion into the hotter region and thus eventually cross the hydrous wedge peridotite solidus, and thus produce fluid-fluxed magma.

What kinds of melts are generated by fluid-fluxed melting at 3–4 GPa? Conducting loftier-pressure, high-temperature experiments is very hard. The studies by Kawamoto and Holloway (1997) and Tenner et al. (2012) propose that in the presence of H_twoO, magmas are alkalic (i.e., nepheline-normative) when forming from a garnet peridotite, which is stable at > two.eight GPa (> 100 km deep in the Globe). On the other hand, the magmas are more than high-Mg andesitic when they are generated from low to moderate degrees of partial melting of spinel peridotite, shallower in the mantle (due east.1000., Tenner et al., 2012). Grove et al. (2012) tried to explain the composition of hydrous magmas produced in the mantle wedge (Fig. 20). They suggested that a multifariousness of magmas are generated within the wedge with a fairly constant FeO*/MgO ratio of 0.5–0.viii; and the higher-silica versus lower-silica melts are extracted from harzburgite vs. lherzolite residues, respectively. Hydrous fractional crystallization produces the calc-alkaline trends. On the other hand, "dry out" fractionation of basalt magma generates Fe-enrichment fractionation trends with but a modest increase in silica content.

Johnson and Plank (1999a,b) performed experiments on a pelagic red dirt (similar to subducted sediment) at two–4 GPa in the presence of H₂O. The melts were peraluminous to peralkaline granites, quite different from the lavas erupted at arcs. It is possible that hydrous sediment-derived melts rising from the subducted plate up to the hottest function of the wedge and induce large-scale melting; and this latter (second stage simply volumetrically more arable) melt may be high-Mg andesite.

Read full chapter

URL:

https://www.sciencedirect.com/scientific discipline/article/pii/B9780081029084000862

Primary Cook Compositions in the Earth's Drapery

Stephen F. Foley , Zsanett Pintér , in Magmas Under Pressure level, 2018

5.1 Oceanic Lithosphere

Geothermal gradients do not intersect the dry solidus for peridotite except in a minor window beneath the midocean ridges. In three dimensions, this results in a toblerone-shaped melting region in which decompression melting of peridotite dominates. This is in the major melting regime to depths of around 50 km (Fig. 1.x), and incipient melting triggered by volatiles occurs at deeper levels and in lateral extremities. The high-temperature weather condition are such that melts migrate in a three-dimensional network forth grain boundaries and do not need channeled period (McKenzie, 1985). Melt compositions ranging from quartz tholeiite to alkali basalt can grade under "dry" weather condition (Figs. 1.1 and i.2).

Fifty-fifty though midocean ridge basalts are used to define the "depleted MORB pall," which is oftentimes viewed as an endmember among basalts (Zindler and Hart, 1986), the endmembers themselves are probably mixtures containing notwithstanding more than depleted mantle (Salters and Dick, 2002), indicating the interest of NPMR even in the depleted MORB curtain source. Despite the major melting region being almost exclusively in the spinel peridotite field, a trace-element and isotopic "garnet signature" is interpreted to prove the involvement of pyroxenites that originate from recycled ocean crust during melting (Hirschmann and Stolper, 1996). These include gabbros that impart a "ghost plagioclase" signature to the basalts (Sobolev et al., 2000). Sediments probably play only a minor part, as most will be melted or dehydrated during subduction. Melts produced from recycled eclogites generate garnet pyroxenites by reaction with peridotite (Yaxley and Green, 1998) and result in nepheline-normative to andesitic liquids that mix with peridotite-derived basalt during progressive melting (Pertermann and Hirschmann, 2003).

Volatiles crusade more alkaline cook compositions at greater depths, which is the probable cause of the highly conductive seismic low-velocity zone beneath the lithosphere (Sifré et al., 2014). These initial melts volition also exist more mutual in the lower extremities lateral to the midocean ridge. Although mobile, many of the melts will not be successfully drawn into the primary melt puddle and will solidify as pyroxenites in the lower oceanic lithosphere (Langmuir et al., 1993; Foley et al., 2001). Ultramafic cumulates were probably more important early in Earth history, and currently in oceanic plateau where oceanic chaff is unusually thick (Kerr et al., 1997; Neal et al., 1997). Their importance every bit cook sources after recycling of the oceanic lithosphere has probably waned with time.

Intraplate volcanism, either oceanic or continental, volition comprise like components, but results from a deeper melting interval because of the thicker lid of lithosphere relative to midocean ridges (Fig. one.10). This ways that the amount of pyroxenite-derived melt is likely to be college (Sobolev et al., 2007). Ocean island basalts also have slightly higher volatile contents (Danyushevsky et al., 2000; Rosenthal et al., 2015), merely do not approach those in collisional or continental environments.

Read total chapter

URL:

https://www.sciencedirect.com/science/article/pii/B9780128113011000010

Advanced Fuels/Fuel Cladding/Nuclear Fuel Performance Modeling and Simulation

A.K. Sengupta , ... H.S. Kamath , in Comprehensive Nuclear Materials, 2012

3.03.2.one Thermophysical Properties of Carbide Fuel

The thermophysical properties that are of importance and bear upon the fuel operation are solidus/liquidus temperature, thermal conductivity, coefficient of thermal expansion, elastic/fracture properties, creep, and hardness at ambient and at high temperatures.

The solidus/liquidus temperatures along with thermal electrical conductivity limit the fuel operating temperature in terms of linear rut rating (W cm⁻¹), and the fuel center which 'sees' the highest temperature does not exceed the solidus temperature. The liquidus temperature gives some indication of the physical state of the fuel in case of core meltdown nether accidental atmospheric condition. Thermal conductivity is an important factor that determines the rate of estrus transfer from the fuel to the clad. As mentioned above, these properties also put a limit on the fuel surface temperature. Thermal conductivity, though an intrinsic property, varies with a number of parameters which are feature to the sample. Some of these parameters are density or porosity (shape, size, and distribution), composition, presence of a 2d phase, grain size, etc. Coefficient of thermal expansion is an important design parameter for the fuel pivot (both for fuel and cladding fabric). Information technology depends on the composition as well as the extent of second phase nowadays. The stresses generated past the fuel over the cladding material are partly due to the departure in the coefficient of thermal expansion between the fuel and the cladding material. The elastic holding and the fracture property of the fuel are primarily responsible for the extent of FCMI. Hardness of the fuel determines the extent of FCMI: a softer fuel will exert lower stresses on the cladding, thus have lower FCMI. Both thermal-induced and irradiation-induced pitter-patter of the fuel also determine the extent of pellet–clad mechanical interaction. Creep backdrop also depend on a number of variables such as composition, presence of a 2nd phase as precipitates, grain size, etc. Thermophysical properties of actinide carbide have been extensively described and discussed in Chapter 2.04, Thermodynamic and Thermophysical Backdrop of the Actinide Carbidesof this Comprehensive. A summary of the data for high (70%) and low (20%) plutonium-containing fuel ¹² is given in Table 4 .

Table iv. Thermophysical properties of loftier- and low-plutonium-containing carbide fuels

Backdrop	(U_0.threePu_0.7)C	(U_0.8Pu_0.2)C
Solidus temperature (K)	2148	3023
Thermal conductivity (West m⁻¹ K) at 1273 K	12.0	xix.0
Coefficient of thermal expansion (300–1800 K)	13.8 × 10⁻⁶	10.9 × 10^−vi
Hardness (MPa) at 1250 Yard	1200	1400

Read full chapter

URL:

https://www.sciencedirect.com/science/article/pii/B9780080560335000513

The Chaff

M.L. Farmer , in Treatise on Geochemistry (Second Edition), 2014

4.three.ii.2 Trigger Mechanisms for Mantle Melting

Mantle melting simply requires that the mantle temperature, at a given pressure, exceeds its solidus temperature. Such conditions can be induced in the drape past heating, decompression, or a change in chemical limerick, particularly the improver of volatiles, which profoundly reduces mantle solidus temperatures ( Figure 2 ; come across also Chapter 3.9). Each of these processes can be relevant in the formation of continental magmatism. For case, consider melting in the sublithospheric drapery. Decompression melting of this drape can be induced past lithospheric thinning associated with continental extension, peculiarly during the formation of continental rifts ( Figure ane ). Melting occurs when deeper mantle flows upward to recoup for the decreased lithospheric thickness. In a seminal paper, McKenzie and Bickle (1988) numerically modeled this process and demonstrated that the college the sublithospheric mantle potential temperature (T _p, the temperature that the mantle would have should information technology be allowed to rising adiabatically to the Earth'south surface), and the greater the degree of lithospheric extension, the larger the depth interval in the drape over which melting occurs (the polybaric 'melt column,' Figure 1 ) and, consequently, the larger the volume of cook produced. For example, decompression melting of 'normal' potential temperature (1290 ᵒC) sublithospheric drapery induced past lithospheric extension may occur through only a short pressure interval considering the melt column is effectively capped past the base of the CLM ( Figure 1 ). As a result, only small cook volumes are generated, as observed in alkali basalt volcanic fields ( Figure ane ) and melting may be restricted to the garnet peridotite stability field. Conversely, the hotter the sublithospheric pall, the greater the depth of initiation of melting and the volume of magma produced in upwelling mantle, fifty-fifty in the absence of thinning lithospheric mantle; hence, the likely importance of high potential temperature mantle plumes in the generation of large-book CFB ( Figure 1 ). Decompression melting in the sublithospheric mantle tin can too be induced by convective instabilities in the upper pall resulting from original variations in lithospheric thickness (King and Anderson, 1998) or lithospheric 'delamination' (Elkins-Tanton, 2005, 2007).

Decompression melting in the continental drapery lithosphere, by contrast, is difficult to induce, fifty-fifty in fertile drapery. Harry and Leeman (1995), for example, demonstrated that lithospheric extension does non typically bring either dry out or water-saturated peridotite into supersolidus conditions ( Figure 3 ). Instead, melting of the lithospheric mantle seems to require the addition of fluids and/or heat from the underlying mantle (Harry and Leeman, 1995). Turner et al. (1996b) demonstrated that conductive heating of hydrated lithospheric mantle past an upwelling mantle plume can produce significant volumes of melt, depending, in role, on the original thickness of the hydrated drape.

Clearly, then, the concrete and chemical characteristics of the continental lithosphere play an important role in determining the sources and volumes of continental mafic magmatism. Therefore, if the sources of a given continental igneous stone tin be determined, and so inferences can be made regarding what sort of dynamic processes were taking place in the subcontinental pall during magma generation. The difficulty is in unambiguously determining the sources of continental basalts. For this purpose, the geochemist must rely on indirect information on magma source regions provided past the rock'southward major trace element and isotopic compositions.

Read total affiliate

URL:

https://world wide web.sciencedirect.com/science/article/pii/B978008095975700303X

The Crust

G.Fifty. Farmer , in Treatise on Geochemistry, 2007

3.03.2.two Trigger Mechanisms for Mantle Melting

Mantle melting simply requires that the mantle temperature, at a given pressure, exceeds its solidus temperature. This can be induced in the drapery either by heating, decompression, or a alter in chemical composition, especially the addition of volatiles, which greatly reduces the mantle solidus temperature (meet also Chapter 2.07; Effigy 2). Each of these processes can be relevant in the germination of continental magmatism. For example, consider melting in the sublithospheric curtain. Decompression melting of this pall can be induced by lithospheric thinning associated with continental extension, particularly during the formation of continental rifts (Effigy 1). Melting occurs when the deeper drapery flows upwards to compensate for the decreased lithospheric thickness. In a seminal paper, McKenzie and Bickle (1988) numerically modeled this process and demonstrated that the higher the sublithospheric mantle-potential temperature (T _p, the temperature that the mantle would have should information technology exist allowed to rise adiabatically to the Earth'south surface) and the greater the degree of lithospheric extension, the larger the depth interval in the drape over which melting occurs (the polybaric "melt column," Figure i) and, consequently, the larger the volume of melt produced. In general, the thicker the continental lithosphere and the colder the sublithospheric mantle, the smaller the volume of magma produced by sublithospheric mantle melting. For instance, decompression melting of "normal" potential temperature (i,290°C) sublithospheric drapery induced by lithospheric extension may occur through only a brusque pressure level interval because the cook column is effectively capped past the base of the CLM (Figure one). As a result, only small cook volumes are generated, equally observed in brine basalt volcanic fields (Figure ane) and melting may be restricted to the garnet peridotite stability field. Conversely, the hotter the sublithospheric mantle, the greater the depth of initiation of melting and the volume of magma produced in upwelling mantle, fifty-fifty in the absence of thinning lithosphere; hence, the probable importance of high-potential temperature mantle plumes in the generation of big-volume CFBs (Figure 1). Decompression melting in the sublithospheric mantle can too exist induced inside convective instabilities in the upper curtain resulting from original variations in lithospheric thickness (King and Anderson, 1998) or lithospheric "delamination" (Elkins and Hager, 2000).

Decompression melting in the continental pall lithosphere, in contrast, is difficult to induce, even in fertile mantle (Arndt and Christensen, 1992). Harry and Leeman (1995), for instance, demonstrated that lithospheric extension does not typically bring either dry or h2o-saturated peridotite into supersolidus conditions (Figure 3). Instead, melting of the lithospheric drapery seems to crave the add-on of fluids and/or heat from the underlying mantle (Harry and Leeman, 1995). Turner et al. (1996b) demonstrated that conductive heating of hydrated lithospheric mantle past an upwelling mantle plume can produce significant volumes of melt depending, in part, on the original thickness of hydrated mantle.

Conspicuously, and so, the physical and chemic characteristics of the continental lithosphere play an important role in determining the sources and volumes of continental mafic magmatism. Therefore, if the sources of a given continental igneous rock tin can be determined, and then inferences can be fabricated regarding the dynamic processes in the subcontinental drapery during magma generation. The difficulty is to make up one's mind unambiguously the source of a given continental basalt. For this purpose, the geochemist must rely on indirect data regarding magma source regions provided by a basalt's major-, trace-chemical element, and isotopic composition.

Read full chapter

URL:

https://www.sciencedirect.com/science/article/pii/B008043751603019X

The origin of magma on planetary bodies

Eric H. Christiansen , ... Jani Radebaugh , in Planetary Volcanism beyond the Solar System, 2022

Advection of hot material

Oestrus transfer associated with advective movement of magma is an important means of raising stone temperatures higher up the relevant solidus temperatures, especially in the chaff of a planet ( Figs. 1 and iii). Already hot, deep crust tin exist heated above its solidus if bodies of hotter, curtain-derived magma intrude it. Density constraints bespeak that ascending basaltic magma tin can be arrested at the base of operations of the (usually feldspathic) crust by underplating, or by stagnating in the eye crust, depending on the density profile. One time intruded, the hot mafic magma may cause melting of surrounding wall rock. The thermal upkeep for melting terrestrial basaltic chaff can exist approximated by considering rock at a depth of 30 km with a thermal gradient of 20 °C/km (and therefore T = 600 °C). To raise the rock T to its solidus of, say, 900 °C (Fig. half dozen) and assuming a rock specific heat of 1.4 kJ/kg deg, requires (1.four kJ/kg deg) × (900° – 600°) deg = 420 kJ/kg. To melt i kilogram of this hot (but still solid rock), then, requires an additional 300 kJ/kg—its approximate latent heat of melting. Thus, the thermal energy to accomplish this subsolidus heating and subsequent melting is well-nigh 720 kJ/kg, and can exist supplied past less than 1 kg of basalt magma initially at 1300 °C. This calculation assumes that the latent heat of crystallization of the magma supplies about 420 kJ/kg and cooling to 900 °C supplies nigh (1.4 kJ/kg deg) × (1300° – 900°) deg = 560 kJ/kg for a total of 980 kJ/kg. An estimate dominion of thumb is that the mass of crustal rock melted is well-nigh the same every bit the mass of basaltic magma heating it. Melting consumes relatively large amounts of thermal energy, moderating T variations inside magma source rocks.

High crustal temperatures and thus thermal gradients are required for much crust to melt in this way, so this mechanism was probably limited to the early stages of planetary cooling. These constraints on crustal melting are similar for other terrestrial planets, and maybe even Io and Europa. Crustal melting on Vesta would be limited by its minor size. Crustal melting or reprocessing is a key to the generation of tertiary crust (eastward.1000., Chapter 8).

Read full affiliate

URL:

https://www.sciencedirect.com/scientific discipline/commodity/pii/B9780128139875000067

Thermal models of the oceanic lithosphere and upper mantle

Anne Thou. Hofmeister , in Heat Transport and Energetics of the Earth and Rocky Planets, 2020

7.three.2.ane Buffering of temperatures below the thermal boundary layer

Given the speed of h2o ascent, the base of the lithosphere is not water saturated. The "moist" solidus of Takahashi (1986) reasonably matches the temperature at the continental base, and therefore is used down to 320 km. Below 320 km, the temperature should be higher since water was removed from this region and shear heating is present.

It is possible that material below 320 km is more than refractory, since calcium silicate inclusions in diamond samples formed at this depth (see Affiliate i). Ca silicates melt at loftier T and P (Huang et al., 1980). However, diamonds were brought to the surface in CO₂ gas-backed explosions, and do non necessarily stand for typical mantle. Since calcium silicates are non found in xenoliths, we infer that peridotite represents the upper drapery. Hence, the dry peridotite solidus of Zhang and Herzberg (1994) sets the upper limit from 320 km to the 410 km seismic aperture.

Curtain composition below 410 km is poorly constrained. This seismic discontinuity is attributed to a structural transition in the major phase olivine, in which case the dry peridotite solidus sets the upper limit on temperatures downward to 660 km. Nonetheless, a chemical change could contribute to the 410 km discontinuity. This possibility is suggested past the transition zone receiving but the steepest of westward dipping slabs and by the unusual chemical science of the deepest material (Ca silicates). Thus, subduction could induce mixing of upper drape peridotite with a more refractory underlying limerick, every bit follows:

Read full chapter

URL:

https://www.sciencedirect.com/science/article/pii/B9780128184301000070

phelanfitain.blogspot.com

Source: https://www.sciencedirect.com/topics/earth-and-planetary-sciences/solidus

Phelan Fitain

Solidus Liquidous Graph How to Read Geology

H2o Solution Mechanisms and Construction

15.four.three Crystallization, Melting, and Construction

Including Actinides

3.2.2 Sc–V–C

Crustal and Lithosphere Dynamics

vi.07.2.3 Solidification Fronts

Volume 2

Melting and Melt Limerick

Primary Cook Compositions in the Earth's Drapery

5.1 Oceanic Lithosphere

Advanced Fuels/Fuel Cladding/Nuclear Fuel Performance Modeling and Simulation

3.03.2.one Thermophysical Properties of Carbide Fuel

The Chaff

4.three.ii.2 Trigger Mechanisms for Mantle Melting

The Crust

3.03.2.two Trigger Mechanisms for Mantle Melting

The origin of magma on planetary bodies

Advection of hot material

Thermal models of the oceanic lithosphere and upper mantle

7.three.2.ane Buffering of temperatures below the thermal boundary layer

Menu Halaman Statis