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Development of the Kawai-type Multi-anvil Apparatus (KMA) and Its Application to High
Pressure Earth Science
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2012 J. Phys.: Conf. Ser. 377 012001
(http://iopscience.iop.org/1742-6596/377/1/012001)
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Development of the Kawai-type Multi-anvil Apparatus (KMA) and Its Application to High Pressure Earth Science
E Ito
Institute for Study of the Earth’s Interior Okayama University Misasa Tottori-ken 682-0193 Japan
E-mail: eiito645@gmail. com
Abstract. Since Birch’s prediction on the structure of the Earth’s interior high pressure Earth science has rapidly been grown by the Kawai-type multi-anvil apparatus (KMA) and the diamond anvil cell (DAC). An important advantage of the KMA is its large specimen volume which makes it possible to conduct experiments under precisely controlled P-T conditions. A typical application of the KMA to the Earth science might be determination of the post-spinel phase equilibria in the system Mg2SiO4-Fe2SiO4. By adopting sintered diamond (SD) as the anvil material accessible pressure of the KMA has substantially increased. Melting experiments of mantle materials up to 35 GPa opened a new paradigm on the mantle fractionation in early Earth. Combining the KMA equipped with SD anvils with the synchrotron radiation phase equilibria of Fe GaN and Fe2O3 were determined by means of in situ X-ray diffraction. Special attention was paid to define the phase boundaries between perovskite and post-perovskite in MgGeO3 and MnGeO3 as analogues of MgSiO3. We also observed the spin transition of Fe2+ in (Mg0.87Fe0.17)O at 300 and 700 K. Recently the maximum attainable pressure is reaching 100 GPa and high P-T experiments up to 90 GPa are our ordinary jobs. In order to produce still higher pressure however innovation of SD such as NPD is indispensable.
1. Beginning of the high pressure Earth science In the early 20th century the Earth’s interior became an object of scientific research due to the information provided by seismology [1] which made it possible to determine the density and thereby pressure as functions of depth from the surface to the center [2]. Following these pioneering works Birch [3] analyzed homogeneity of the subdivided layers of the Earth’s interior [2] using the equation of state based on finite strain theory and Bridgman’s compression data and concluded that minerals constituting the uppermost mantle such as olivine pyroxenes and garnet successively transform into closed-packed oxides similar to corundum rutile spinel or perovskite in structure. As his analyses were so concrete and convincing that the prediction had been the guiding principle for exploration of the Earth’s interior for long time and strongly stimulated the high pressure experiments.
Figure 1 shows a standard Earth’s model PREM [4]. The mantle is characterized by two sharp increases in seismic velocities at depths of 410 and 660 km which divides the mantle into three parts the upper mantle (B) the transition zone (C) and the lower mantle (D). Following Birch [3] high pressure phase equilibria of the system Mg2SiO4-Fe2SiO4 were extensively studied by many workers represented by Ringwood and Major [5] and Akimoto and Fujisawa [6] because olivine (Mg0.9Fe0.1)2SiO4 is the most dominant (> 60%) constituent of the upper mantle. And the 410 km discontinuity was reasonably assigned to the transformation of the olivine (α) into the modified spinel
23rd International Conference on High Pressure Science and Technology (AIRAPT-23) IOP PublishingJournal of Physics: Conference Series 377 (2012) 012001 doi:10.1088/1742-6596/377/1/012001
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(β) structure up to the early 1970s. As capability of the apparatuses employed in these studies were limited to ca. 15 GPa neither synthesis of the end member Mg2SiO4 spinel (γ) nor acquisition of insight into the post-spinel transformation were successful at that time.
Figure 1. A standard Earth’s model (PREM) by Dziewonski and Anderson (1981). Layers A-G are correspond to division by Bullen [2].
2. Devices employed in the high pressure Earth sciences Beginning of the high pressure Earth science Soon after however γ–Mg2SiO4 was synthesized by Suito [7] in the Kawai-type multi-anvil apparatus (KMA) and the decomposition of γ-Fe2SiO4 into an assemblage of FeO (wüstite) and SiO2 (stishovite) was found by Mao and Bell [8] by adopting the diamond anvil cell (DAC). Hereafter the high pressure Earth science has been extensively developed by adopting both the devices. In the DAC it is possible to compress a small amount of sample to multi Mbar heat it to thousands of Kelvin and observe the state of the sample under these extreme conditions by means of X-ray optical and other measurements. A marked advantage of the KMA over the DAC on the other hand is the much larger sample volume which makes it possible to conduct experiments under precisely controlled P-T conditions. Therefore the KMA has been adopted in various researches determination of phase equilibria synthesis of high pressure phases and measurements of physical properties. Development of the KMA was carried out mainly during 1965-1973 at Osaka University under the direction of the late N. Kawai [9]. Photos of the KMA are shown in Figure 2. The cubic assemblage of eight cubes of tungsten carbide (WC) an octahedral pressure medium and gaskets so-called the Kawai-cell (left) is squeezed along the [111] direction in the split sphere guide blocks with the aid of a uniaxial press (right).
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FK
presqu
igure 2.The KKawai-cell cossure medium
ueezed in the
Kawai-type momposed of cum pyrophyllitsplit sphere g
press (l
multi anvil appubic WC anvite pre-gasketsguide block wlower photo).
paratus (KMAils MgO octas etc. (upper
with the aid of
A). The ahedral photo) is
f uniaxial
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The egrown sinthan 23 Gmantle ma
3. The poto phase eSynthesis assemblagwith the lasystem Mand 1600 the mant(Mg0.97Fe0
pressures density anIt is realizthe high p
The pquite narrby makingtemperatuthrough th
Seconrevealed t
easiest way tongle crystals oGPa and coulaterial thus sy
per
ost-spinel traequilibrium sof MgSiO3
ge of MgSiOaser heating s
Mg2SiO4-Fe2Si℃ determinetle spinel w0.03)SiO3 peroof 23.1-24.5
nd seismic vezed that the sipressure transfpost-spinel diow pressure ig the dissocia
ure fixed poinhe transition zndly the phasthat some of
o convince theof MgSiO3 perld be the mosynthesized hav
Figure 3. “Hrovskite which
ansformationstudy perovskite (P3Pv and MgOsystem. Later O4 by Ito and
ed by quenchiwith compo
ovskite (Pv) anGPa and at locities [13] ilicate Pv’s anformations inissociation pointerval less tation boundarnt of 1600 ±zone [14]. se boundary hdescending s
e performancrovskite [10] st abundant mve been used
Huge” (over 1mh is stable onl
Af
n in the syste
Pv) and confOpericlase we the post-spin
d Takahashi ing method a
osition (Mg0nd (Mg0.83Fe0
1100-1600 ℃the dissociat
nd Fp are by n pyroxenes anossesses two than 0.15 GPry correspond± 100 ℃ at
has a negativeslabs stagnate
ce of the KMA(see Figure 3
material in outo measure v
mm) single crly at pressurefter [10].
m Mg2SiO4-F
firmation of ere first carrinel transform[12] using th
are reproduced0.9Fe0.1)2SiO4
0.17)O magnes℃. As the disstion must be rfar dominant
nd garnet intoimportant ch
Pa (or 4 km ind to the depththe depth an
e slope dP/dTe around the
A may be to s3) which is staur planet. Thevarious kinds o
rystals of Mges higher than
Fe2SiO4: An
the dissociatied out by Li
mation was exe KMA. Pseud in Figure 4
dissociates siowüstite (Msociation brinresponsible fot constituents o consideratioharacteristics.n depth) for th of the 660 knd can constr
T~ -3 MPa/de660 km disc
show “huge (oable only at pe single crystof physical pr
gSiO3 n 23 GPa.
application o
ion of γ–Mgiu [11] usingamined in deudobinary dia. The diagram
into an aMw) (or ferrop
ngs about 10 or the 660 kmof the lower
on as well. First it comthe mantle spkm discontinuruct the temp
eg. Seismic tocontinuity be
over 1 mm)” pressures hightals of the deeroperties.
of the KMA
g2SiO4 into ag DAC coupletail all over thagrams at 110ms indicate thassemblage periclase Fp)
% increases m discontinuitr mantle takin
mpletes withinpinel. Therefouity we haveperature profi
omography hfore collapsin
as her ep
an ed he 00 hat of at in
ty. ng
n a ore e a ile
has ng
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down into the lower mantle [15]. On the other hand it is known that a phase boundary with a negative slope in the mantle suppresses material transport through the boundary [16]. Therefore it is highly likely that the spinel dissociation substantially contributes to the stagnation of slabs.
Figure 4. Pseudobinary diagrams of the post-spinel transformation in the
system Mg2SiO4-Fe2SiO4 at 1200 and 1600 . After [12].
4. Adoption of sintered diamond (SD) for anvils of the KMA Decisive disadvantage of the KMA in comparison with the DAC was that the maximum attainable pressure was limited to 28 GPa so far as WC was used as the anvil material. Fortunately sintered diamond (SD) which was twice harder than WC [17] became available for anvils of the KMA in the late 1980s. Figure 5 shows SD cubes of Co-binder. We have employed cubes of an edge length 14 mm with truncated corners of 2 to 0.75 mm. We first adopted the split-sphere system [9] to squeeze the Kawai-cell of SD cubes and compared the performances with those of WC cubes. Generated pressure was calibrated using several fixed points and plotted versus oil pressure for both the SD and WC cubes as Figure 6. Superiority of SD to WC is overwhelming suggesting high potential of SD in pressure generation. Following these
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calibration runs we carried out high P-T quenching experiments. The followings are summaries of studies which had never been achieved by using WC anvils.
Figure 5.Sintered diamond cubes with Co binder.
Figure 6.Comparison of pressure generation using SD with WC anvils.
Superiority of SD to WC anvils is overwhelming.
4.1.Synthesis of perovskite with pyrope (Mg3Al2Si3O12) As the system MgSiO3-Al2O3 represents the compositions of pyroxene and garnet in the mantle high pressure phase equilibria of the system are also indispensable to understand mineralogy of the lower
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mantle. Sysolid solutthat the bi
We eorthorhomloop and ttiny amou
4.2MeltingIn order tomelting phare indispmaterial (fractionati
We e
liquidus p
ystematic studtions of the Minary loop betexamined the mbic perovskithe silicate pe
unt of SiO2 sti
g experimentso simulate pohase relations
pensable. TheCMM) [21] hion had been
extended melphase changed
dy by Irifune MgSiO3-rich ptween the twostability of pyte phase at 37
erovskite can ishovite sugg
s of the primoossible materis of the Earth erefore meltinhad been carrpostponed.
lting experimd from ferrop
et al. [18] haperovskite ano phases woulyrope compo7 GPa and 16accommodat
gested slight n
ordial mantle ial fractionatimaterial and
ng experimenried out up to
ment on both periclase (Fp)
ad shown thatnd Al2O3-richld persist to hsition using S600 ℃ [19]. Tte certain amononstoichiome
materials ion in a deep d element portnts of fertile po 25 GPa. Ne
the materialsto Mg-perov
t pyrope (Mg3h corundum sthigher pressurSD anvils andThe result indount of Al2O3etry of Al2O3-
magma oceationing betweperidotite [20evertheless a
Figureimagesperidot
s to 35 GPa vskite (Mg-Pv
3Al2Si3O12) brtructures at cres. d confirmed fodicates closin3. Ubiquitous-bearing pero
an formed on een liquidus p0] and CI choa clear model
e 7. Back scatts of quenchedtite at 29 31
[22]. In periv) at 31 GPa
roke-down ina. 27 GPa an
formation of thng of the bina coexistence
ovskite.
the early Earphases and meondritic mant for the mant
tered electrond charges of
and 33 GPa.
ditite the firand at 33 GP
nto nd
he ary of
rth elt tle tle
n
rst Pa
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liquidus Mg-Pv was successively followed down temperature by Fp and Ca-perivskite (Ca-Pv) within a small temperature range. The change of liquidus phase with pressure is clearly demonstrated in a series of pictures shown in Figure 7. In the CMM Mg-Pv was the liquidus phase which was followed down temperature by Ca-Pv at pressures higher than 28 GPa and Fp was absent in super solidus conditions. Differentiation in a deep magma ocean was examined by crystal fractionation of Mg-Pv Fp and Ca-Pv for CMM and peridotitic bulk silicate Earth models. Mass balance calculation indicated that subtraction of about 40% Mg-Pv and 2% Ca-Pv from CMM yielded a residual melt with characteristics of fertile upper mantle composition. The fractionated Mg-Pv and Ca-Pv would pile up to a depth ca. 1400 km from bottom of the mantle and might be characterized as an enriched and possibly heat producing reservoir by the higher capability of Ca-Pv to accommodate large cations such as rare earth elements and alkaline elements than melt. The observed effect of pressure on element partitioning suggested that better mass balance solutions might be obtained for higher pressure liquidus composition.
5. In situ X-ray observation using the KMA In situ X-ray observation using synchrotron radiation has rapidly pushed the high pressure Earth science towards the exact sciences because the pressure value is determined continuously and uniquely from volume of a pressure marker via its equation of state. The pressure marker is usually mixed with the sample or put next to the sample. By being interfaced with synchrotron radiation versatility of the KMA has been expanded in various research fields such as phase equilibria reaction kinetics equation of state radiographic measurements etc. At the synchrotron facility SPring-8 two DIA-type presses [23] were installed on beam line BL04B1 to squeeze the Kawai-cell. One of them SPEED mkII [24] has exclusively been used to squeeze the Kawai-cell of SD cubes. Experimental methodology of in situ X-ray observation using the Kawai-cell were described to some extent elsewhere [25].
5.1.In situ X-ray diffraction studies on Fe GaN and Fe2O3 We have first studied high pressure polymorphism of iron by means of in situ X-ray diffraction. Our aim of the study was to clarify the stability of β-phase the 5th polymorph of iron which was claimed to be stable under the conditions higher than 35 GPa/1500 K by several groups from the experiments using the DAC [26]. Our experiments up to 44 GPa and 2100 K confirmed progression of the ε→γand the reverse transitions on increasing and decreasing temperature respectively and the presence of β-phase was thus excluded [27].
We successively examined phase relations in GaN [28] and Fe2O3 [29]. In GaN onset of the wurtzite→rocksalt transformation was observed at conditions of 54 GPa/300 K and 51.5 GPa/ 750 K.suggesting a negative dP/dT slope. However it was observed that the rocksalt phase persisted for 90 min at 48.9 GPa/850 K. Therefore the reverse transformation is rather sluggish and more examination is needed to decide the equilibrium phase boundary. Electrical resistance of GaN was tens of mega ohms up to ca. 62 GPa at 300 K and no remarkable change in resistance was observed on the wurtzite – rocksalt transformation.
Phase equilibria of Fe2O3 were examined up to 58 GPa and 1400 K. Hematite (phase I) transformed successively into the Rh2O3 II type structure (II) and an orthorhombic phase (III) with increasing pressure. The phase boundaries for the I - II and II - III were defined to be P(GPa) = -0.015 T(K) + 44.2 and P(GPa) = -0.005 T(K) + 48.7 respectively by observing both the forward and backward reactions in situ. It should be noted that the transformations were observed only at temperatures higher than 500 K and hematite persisted metastably at least up to 58 GPa at 300 K. The electrical resistanceof hematite on the other hand decreased monotonically from tens of mega ohms at 10 GPa to a few ohms with increasing pressure and then plateaus at ca. 60 GPa as shown in Figure 8. The isostructural electrical resistance reduction strongly suggests the occurrence of a Mott transition. The plateau point of electric resistance 60 GPa is usable as a pressure fixed point at room temperature.
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5.2. Post-pThe loweraseismic avelocity VThese enimantle anclarify dyn
In 20MgSiO3 pGPa and important transformainsight to
As thpresent was the best
Crossmixture othe center thermocousee througfrom the v
The tdiffractionpressure bnot recogn10 (B). Wover the crelevant towas defineby T(K) =
Figure 8.
perovskite trarmost 200-30anomalies s
VS and bulk sgmatic featur
nd the core. Tnamics and ev004 Murakaperovskite (Pv
2200 K usinrole in form
ation is of urgthe thermal s
he P-T conditwe examined tt analogs of Ms section of af MgGeO3ilmof octahedro
uple whose jugh the samplvolume of goltransformation profiles in Fby reducing thnized until pr
We carried outconditions upo define the ped by passing
= 177P(GPa) –
Change in el
ansformation 00 km regionsuch as velocound velocityres would be Therefore unvolution of thami et al. [3v) into the Cang the laser-hmation and sgent need. Estructure throuions for the Pthe PPv trans
MgSiO3. a sample assemenite + 0.1Aon of MgO + 5unction was ale and the theld based on thn from Pv to
Figure 10(A).he applied loaressure went dt more few ru
p to 74 GPa aphase boundag through the – 9677 with d
300
ectrical resist3
in meta-germn of the mantcity jumps [3y VC [32] an
refection of nderstanding he Earth. 4] and OganIrO3 structureheated DAC.structure of tspecially theugh the D” layPPv transformsformation in
embly adoptedAu (in weight5% Cr2O3. Teat the center ermocouple bhe Anderson e
PPv was firs Then we triead and keepindown to 60.5uns to recognand 2200 K. Fary between P
Pv-growth PdP/dT = 5.6 M
0 K
tance of Fe2O300 K.
manates tle called th30] anisotropnd presence of
active exchaof the D” lay
nov and Onoe (the post-pe The post-pethe D” layer slope of the yer and to est
mation in MgSMgGeO3 [37
d in MgGeO3t) was put in emperature wof the sampleby the CCD et al.’s [39] Ast confirmed aed to observe ng temperatur5 GPa as clarinize growth eFigure 11 sho
Pv and PPv. TPPv-growth a
MPa/K.
O3 (hematite) w
he D” layer py [31] antf ultra-low ve
ange of energyer should be
o [35] discoverovskite (PPverovskite tranr. Therefore phase bound
timate of therSiO3 are out o7] and MnGe
3 experimentsa cylindrical as measured be. By adoptincamera. Pres
Au scale. at 63.2 GPa athe reverse tr
re constant atified by the s
either PPv or ows P-T plot
The phase bouand the coexi
with pressure
is characterizti-correlation elocity zone agy and materie of essential
vered the tranv) transformansformation sdetailed know
dary dP/dT wormal flux fromof the ability
eO3 [38] whic
s is shown inTiB2 heater
by a thin W3ng the TiB2 hssure value w
and 1325 K aransformationt 1323 K. Grosuccessive proPv from the
ts of the X-raundary betweistence points
at
zed by variobetween she
at the base [33ial between thl importance
nsformation ation) at ca. 12should play awledge on thould give som
m the core [36of the KMA
ch are regarde
n Figure 9. Finwhich is set %Re/W25%R
heater we couwas determine
as shown by thn by decreasinowth of Pv wofiles in Figucounter phas
ay observatioeen Pv and PPs and expresse
us ear 3]. he to
of 20 an he
me 6]. at ed
ne at
Re uld ed
he ng
was ure ses ns Pv ed
23rd International Conference on High Pressure Science and Technology (AIRAPT-23) IOP PublishingJournal of Physics: Conference Series 377 (2012) 012001 doi:10.1088/1742-6596/377/1/012001
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Fexp
Figure 9. A speriments for
chematic drawthe post-pero
wing of the saovskite transfo
ample assembformation in M
Figure 10M511. Prthe growtfrom the p1325 K athe bottomreverse trand 1323
bly for MgGeO3.
0.Diffraction rofiles in (A) th of post-perperovskite at and a series om to top in (Bransformation
K.
profiles of rudemonstrate
rovskite phase63.2 GPa andf profiles from
B) do the n at 60.5 GPa
un
e d m
23rd International Conference on High Pressure Science and Technology (AIRAPT-23) IOP PublishingJournal of Physics: Conference Series 377 (2012) 012001 doi:10.1088/1742-6596/377/1/012001
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The dthe D” diboundary mantle doassuming such as Tpressure bpressure s
The P
method ason Tsuchiwith a lag 5.3.High sHigh spinbeen attraand geochcompressitransition counter paspinel [12
We asample as(Mg0.83Fe0
dP/dT value iiscontinuity dand the geo
wnwellings. Tthermal cond
Tsuchiya [42]by 3.5 GPa cale is fatally
Figure 1boundar
denote th
Pv-PPv phases in MgGeO3ya’s Au scaleer dP/dT valu
spin-low spin n-low spin tracted special ahemical procion curve due[44]. We se
art of magnes].
acquired presssembly show0.17)OFp powd
is slightly smdeeper and
otherm [40] wThe slope of
ductivity of 10 instead of Aand the dP/d
y important.
11. P-T plots ory between Pvhe different ru
by the
e equilibria i. The phase be [42] which ue [38].
transition in ansition of Feattention beccesses [43]. Te to a drastic elected Fp wisian perovskit
sure (P)-voluwn Figure 9.der based on
maller than thoso called PP
would be pre5.6 MPa/K su0 Wm-1K-1 [Anderson et adT increases
of the X-ray ov and PPv (seuns. Growingarrows and c
in MnGeO3 [boundary wasis located aro
ferropericlase2+ in (Mg1-xFause the transThe transitionreduction of
ith a composte in the asse
ume (V) data . Pressure wAnderson et
ose estimated Pv lens formeesent only inuggests a larg[41]. Nevertheal.’s [38] outo 8.7 MPa
observations ree text). Circl
g phases and pcolor markers
[38] were alss determined ound ca. 10 G
se (Mg0.83Fe0.Fex)OFp occusition is consn can be det
f effective ionsition (Mg0.83
emblage produ
at 300 and 7as determine al.’s scale [3
for MgSiO3ed by the do
n relatively coge heat flux oeless if we adur phase bouna/K. Therefor
relevant to deles squares aphases presen. After [37].
o examined bto be P(GPa)
GPa lower pre
17)O urring under lidered to subtected by obnic radius of F3Fe0.17)O beuced by disso
700 K and uped from volu39]. The acqu
[36]. The smouble-crossingold region suf 16 TW acrodopt other Aundary shifts tre establishm
efine the phasand diamondsnt are indicate
by in situ X-) = 39.2 + 0.
essures than th
lower mantle stantially affe
bserving an aFe2+ accompcause the coociation of (M
p to 90 GPa ume of Au muired P-V dat
maller value seg of the phauch as beneaoss the D” layu pressure scatowards high
ment of reliab
se s d
-ray diffractio013T(K) basehat of MgGeO
conditions hect geophysicanomaly in thpanied with thomposition is Mg0.9Fe0.1)2SiO
employing thmixed with thta are shown
ets ase ath yer ale her ble
on ed O3
has cal he he a O4
he he in
23rd International Conference on High Pressure Science and Technology (AIRAPT-23) IOP PublishingJournal of Physics: Conference Series 377 (2012) 012001 doi:10.1088/1742-6596/377/1/012001
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Figure 12were with
We trdata up tozero pressvalues [45higher tha
Figure Fitting u300 and
occurrencwe fit
deviation AssumingM EoS withe insertiThe V0 anrespectivehigher preNeverthelLS state in
6. RecentBy adoptinFigure 13 observatioreaching 1ordinary j
One ospinel tran
. Errors in prhin ± 0.4 GPa ried to fit the 40 GPa whi
sure values o5] which arean 50 GPa a
12.Compressup to 40 GPa 700 K data. T
ce of the spinEoS’s with p
from the sog that the tranith K0’ = 4 foions as LS vand K0 at 300 ely in the saessure and exess it is evidn more detail.
t pressure geng SD anvils shows our re
on at SPring-100 GPa anobs. of our urgentnsformation.
ressure determand those in
e 3rd order Bich were succf volume V0 e noted as Hat 300 K and
sion data of (Massuming K0The data for h
n transition. Foparameters no
olid curves wsition comple
or the data higalues in the fK for the low
ame composixpands with ident that acqu.
eneration and the attainabl
ecent perform-8 using anvid high pressu
t objects is toIn order to ac
mination cauvolume deter
Birch-Murnagcessfully perfo
and bulk moHS values in td those highe
Mg0.83Fe0.17)O0’ = 4.0 (solidhigher pressuror low spin reted as LS in t
with increasinetes at 70 GPagher than thefigures and thw spin regimition. Our daincreasing temuisition of LS
d future persle pressure of
mance of presils with 1.0 mure and temp
o clarify the Pccomplish the
used those of rmination werhan equationormed as shoodulus K0 wethe insertionser than 55 G
OFp and fittind curves) yieldres clearly deegime of 70-9the insertions
ng pressure a at 300 K an
ese pressures. he correspond
me are larger aata suggest thmperature in
S data up to h
spectives f the KMA hassure generatimm truncatioperature expe
PPv transforme object we h
Au volume re typically w
n of state (B-Mwn by the sol
ere in good ags of the figur
GPa at 700 K
ng the 3rd ordeds reasonableeviate toward 90 GPa at 300
which are sh
indicating ond 80 GPa at
The resultanding EoS’s arand smaller that the mixed
accord with higher pressu
as increased yion carried ouon. The maxiriments up to
mation in detahave to exten
and temperatwithin ± 0.05 %M EoS) with lid curves. Angreement witres. HoweverK show grad
er Birch-Mune V0 and K0 va
lower directi0 K and 80-90hown by the b
nset of the s700 K we tri
nt V0’s and K0re shown by than those of d spin regiontheoretical p
ure is required
year by year sut by means oimum attainao 90 GPa hav
ail just like dond the accessi
ture fluctuatio%.
K0’ = 4 to thnd the resultath the literatur volume da
dual downwa
naghanEoS’s.alues for bothon indicating
0 GPa at 700 Kbroken lines.
spin transitioied to fit the B0’s are noted broken curve
f Lin et al. [4n shifts towaprediction [47d to specify th
ince 1998 [19of in situ X-raable pressure ve become o
one in the posible pressure
on
he ant ure ata ard
h g K
on. B-in
es. 46] ard 7]. he
9]. ay is
our
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23rd International Conference on High Pressure Science and Technology (AIRAPT-23) IOP PublishingJournal of Physics: Conference Series 377 (2012) 012001 doi:10.1088/1742-6596/377/1/012001
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least by 20pressures possibilityimportanc(NPD) rereaches 14
Acknowle I am verytheir guidKawai S.
Reference[1] Jeffrey[2] Bullen[3] Birch F[4] Dziew[5] Ringw[6] Akimo[7] Suito K[8] Mao H[9] KawaiKawai N [10] Shats[11] Liu L[12] Ito E [13] SawaA Weidne
0 GPa. The syfor WC SD
y to producece to produce cently develo40 GPa
Figure1.0 m
edgements y grateful to
dance help aAkimoto an
es ys H 1939 Mon E 1940 Bull.F P 195) J. G
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.
e 224 749; Y
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