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1 red to about 4 per cent by volume of Earth's mantle.
2 ge low-shear-velocity provinces in the lower mantle.
3 l homogeneity of the upper and shallow lower mantle.
4 stable under the conditions of the lowermost mantle.
5 of the LLSVPs is lower than the surrounding mantle.
6 served in widespread regions of the cortical mantle.
7 can preserve carbonates in the Earth's lower mantle.
8 narrow low wave speed zone in the uppermost mantle.
9 ill also control transport properties in the mantle.
10 wered by radioactive decays in the crust and mantle.
11 , and C at conditions relevant for the whole mantle.
12 ying a cold stable state well into the upper mantle.
13 ction in peridotite at the base of the upper mantle.
14 er and a mechanism for oxidizing the Martian mantle.
15 to direct carbonate recycling into the deep mantle.
16 cortical ROIs covering most of the cortical mantle.
17 stratification of water content in the upper mantle.
18 ed on thermochemical structures in the lower mantle.
19 ests convective flow in the hydrated forearc mantle.
20 e that carbonates exist in the Earth's lower mantle.
21 te-metasomatized subcontinental lithospheric mantle.
22 ts denser polymorph, ringwoodite, in the wet mantle.
23 sin, is seismically active down to the upper mantle.
24 ed to result in the oxidation of the sub-arc mantle.
25 ected seismologically at the base of Earth's mantle.
26 the subducting oceanic crust, as well as the mantle.
27 ease in the ferric iron content of the lower mantle.
28 presence of metallic iron in an isochemical mantle.
29 ne an average carbon abundance for the upper mantle.
30 be concentrated towards the very base of the mantle.
31 le upwelling in two antipodal regions of the mantle.
32 is controlled by slow convection within the mantle.
33 atile abundances like Earth's depleted upper mantle.
34 ffect on the extent of N subduction into the mantle.
37 ion of layers could dynamically decouple the mantle above 2,000 km from the lowermost mantle, and pro
38 entinite domains are commonly present in the mantle above shallow subducting slabs and play key roles
39 livine phase transformation in the upwelling mantle across the 410-km discontinuity and investigated
41 d continents move over the weaker underlying mantle, although geophysical and geochemical constraints
43 may dominate the recycling of carbon in the mantle and contribute to chemical and isotopic heterogen
44 es resisting slab penetration into the lower mantle and deformation associated with slab buckling and
47 back-arc result in vigorous inflow of hotter mantle and subdued inflow of colder mantle beneath the a
49 mechanisms driving mass exchange between the mantle and the Earth's surface, and is central to curren
50 1,000 kilometres upward from the base of the mantle and their buoyancy remains actively debated withi
51 inally anhydrous minerals formed deep in the mantle and transported to the Earth's surface contain te
52 ific are the largest structures in the lower mantle, and hence severely affect the convective flow.
53 akest and most abundant mineral in the upper mantle, and observations of the exceptionally large (mom
54 the mantle above 2,000 km from the lowermost mantle, and provide a rheological basis for the stabiliz
57 ale geochemical differences across the upper mantle are known, but how they are preserved during conv
58 oceanic lithosphere to be subducted into the mantle as "slabs" and new rock to be generated by volcan
59 ve tracer of oceanic crust recycled into the mantle, as a diagnostic criterion by which to identify a
60 hemical evidence of a fluid pathway from the mantle, as well as with a sharp vertical offset in the l
61 e velocities in the top portion of the lower mantle, assuming a pyrolitic mantle composition and acco
62 ingly poor agreement with those of the lower mantle at depths greater than 1,200 kilometres, indicati
63 w Hf-Nd isotope data, suggest that uppermost mantle at one location (e.g. under Indian Ocean) circula
65 rth became uncoupled along the Moho, and the mantle below the Moho subducted southwards beneath the n
67 f hotter mantle and subdued inflow of colder mantle beneath the arc due to the temperature dependence
70 high-(3)He/(4)He domain resides in the deep mantle, beneath the upper mantle sampled by mid-ocean-ri
71 er Indian Ocean) circulates down to the core-mantle boundary (CMB), but returns within >/=100 Myrs vi
73 ve velocity provinces (LLSVPs) atop the core-mantle boundary beneath Africa and the Pacific are the l
74 he mantle transition zone, and atop the core-mantle boundary could efficiently sequester significant
75 uld be expected to form directly in the core-mantle boundary region and their properties would provid
76 ralow-velocity zones (ULVZs) at Earth's core-mantle boundary region have important implications for t
77 We used shear waves diffracted at the core-mantle boundary to illuminate the root of the Iceland pl
78 key role in transferring heat from the core-mantle boundary to the lithosphere, where it can signifi
80 velocity and density variations at the core-mantle boundary, is explained best when the overall dens
83 )/Fe(2+) ratio of about two in shallow-lower-mantle bridgmanite is required to match seismic data, im
84 e tidal tomography to constrain Earth's deep-mantle buoyancy derived from Global Positioning System (
85 ls the transport of H2O in the Earth's upper mantle, but is not fully understood for olivine ((Mg, Fe
86 l expansion of chromatophores present on the mantle, but not on the head and arms; furthermore, the e
87 cation of the oxidation state of the sub-arc mantle by hydrous, oxidizing sulfate and/or carbonate-be
88 The chemical composition of Earth's lower mantle can be constrained by combining seismological obs
92 lus venetoclax in murine xenograft models of mantle cell (MCL), germinal-center diffuse large B-cell
93 mide and rituximab in patients with relapsed mantle cell lymphoma (A051201) and relapsed follicular l
94 ollicular lymphoma (FL) (16.3% [43 of 263]), mantle cell lymphoma (MCL) (6.8% [18 of 263]), and diffu
95 large B-cell lymphoma (DLBCL) (10% [n = 9]), mantle cell lymphoma (MCL) (8% [n = 7]), and mycosis fun
100 interrogate signaling pathways activated in mantle cell lymphoma (MCL) in vivo, we contrasted gene e
102 t failure (TTF) and overall survival (OS) in mantle cell lymphoma (MCL) is based on the clinical fact
105 spite recent advances in lymphoma treatment, mantle cell lymphoma (MCL) remains incurable, and we are
109 mong 45 patients with relapsed or refractory mantle cell lymphoma (MCL), with manageable tolerability
111 oxidative stress-mediated drug resistance in mantle cell lymphoma (MCL); however, the biological func
113 , and Sept 30, 2014, 11 patients (three with mantle cell lymphoma and eight with follicular lymphoma)
115 rash (two [67%] of three) for patients with mantle cell lymphoma and neutropenia (five [63%] of eigh
116 s in human chronic lymphocytic leukaemia and mantle cell lymphoma cell lines, and patients treated wi
117 ased on the clinical factors included in the Mantle Cell Lymphoma International Prognostic Index (MIP
118 variable analysis, these risk groups and the Mantle Cell Lymphoma International Prognostic Index were
119 ignificantly different OS independent of the Mantle Cell Lymphoma International Prognostic Index.
121 tumor biopsies were reviewed by the European Mantle Cell Lymphoma Pathology Panel to determine Ki-67
122 small molecule inhibitor (HDACi) in CLL and mantle cell lymphoma restored the expression of the BTK-
123 mphocytic leukemia, follicular lymphoma, and mantle cell lymphoma were 5%-10% higher per 5-year incre
124 16, 124 patients with relapsed or refractory mantle cell lymphoma were enrolled and all patients rece
125 ents with histologically documented relapsed mantle cell lymphoma who had not received previous lenal
127 s efficiently lysed primary B-cell leukemia, mantle cell lymphoma, and multiple myeloma in vitro.
128 tment of chronic lymphocytic leukemia (CLL), mantle cell lymphoma, and Waldenstrom macroglobulinemia.
129 e B-cell lymphoma, Richter's transformation, mantle cell lymphoma, follicular lymphoma, and chronic l
130 iven to patients with relapsed or refractory mantle cell lymphoma, until disease progression or unacc
138 co purified DNA methylation signatures of 82 mantle cell lymphomas (MCL) in comparison with cell subp
139 dge, the clinical features of ocular adnexal mantle-cell lymphoma (OA-MCL) have not previously been e
142 al, and overall survival among patients with mantle-cell lymphoma who were younger than 66 years of a
145 /(4)He domain is denser than low-(3)He/(4)He mantle components hosted in plumes, and if high-(3)He/(4
146 on of the lower mantle, assuming a pyrolitic mantle composition and accounting for depth-dependent ch
147 ction could have influenced the evolution of mantle composition since 550 Ma and potentially since th
155 f Earth's thermal evolution and the style of mantle convection rely on robust seismological constrain
156 's mantle endure as a direct result of whole-mantle convection within largely isolated cells defined
157 ocesses in the back-arc, such as small-scale mantle convection, are likely to cause lateral variation
162 -stage terrestrial accretion of halogens and mantle degassing, which has removed less than half of Ea
163 at 120-160 km depth suggests that the slab's mantle dehydrates beneath the volcanic arc, and may be t
164 s about 0.5 per cent higher than the average mantle density across this depth range (that is, its mea
171 ns of chemical variations around the Earth's mantle endure as a direct result of whole-mantle convect
172 n the silicate Moon can instead reflect core-mantle equilibration in a largely to fully molten Moon.
173 n of Hawaiian double-track volcanism: first, mantle flow beneath the rapidly moving Pacific plate str
174 gnetic and radiometric age data suggest that mantle flow can advect plume conduits laterally, the flo
178 to Earth's surface; therefore, variations in mantle fO2 may influence the fO2 at Earth's surface.
179 occurred in the subcontinental lithospheric mantle, fused to the base of the continental crust and i
180 removed less than half of Earth's dissolved mantle gases, the efficient extraction of halogen-rich f
181 on of rising plumes in Earth's shallow lower mantle have been suggested to result from a viscosity in
183 ly utilizing seismic tomography to interpret mantle heterogeneity and its links to past tectonic and
184 ent with primary magmatic processes, such as mantle heterogeneity or change in depth of melt formatio
185 h incorporates tomography-based, present-day mantle heterogeneity to reconstruct mantle structure at
188 nts on Earth reduced the potential for upper-mantle hydration early in its geological history, leadin
190 rts the recycling of heavier N into the deep mantle in this section of the Central America margin.
191 temporary adhesive glands located within the mantle, instead of the specialised hypodermal glands in
192 romoting the deep CO2 transfer from the slab-mantle interface to the overlying mantle wedge, in parti
194 cate from the cooling core to underneath the mantle is an order of magnitude more efficient per unit
198 have juvenile epsilonHf (+7.6 to +11.5) and mantle-like delta(18)O (5.2-5.5 per thousand), whereas t
199 that multiphase deformation of the crust and mantle lithosphere leads to the formation of distinct ma
200 at plausible H2O concentrations in the upper mantle (</=250 ppm wt) can account for high electrical c
202 y affects the physico-chemical properties of mantle materials, governing planetary dynamics and evolu
203 The presence of negative S-MIF in the deep mantle may also help resolve the problem of an apparent
204 xcess of 9 per cent by volume of the Martian mantle may contain hydrous mineral species as a conseque
207 ate (230)Th and (226)Ra excesses, reflecting mantle melting in the presence of a water-rich fluid in
210 he melting temperatures of the high-pressure mantle mineral, bridgmanite (MgSiO3-perovskite), with cu
211 l clue towards understanding why these dense mantle minerals show distinctly different softening beha
214 etallic at the conditions of the deep molten mantle of early Earth and super-Earths, raising the poss
215 fueled systems in the cool, hydrated forearc mantle of subduction zones may provide an environment th
216 t humility and excitement that we assume the mantle of the leading translational science journal in t
219 s on mechanisms exposing altered products of mantle peridotite at the seafloor long time after their
220 storage in a boundary layer, upwelling as a mantle plume and partial melting to become ocean island
221 anes to reconstruct the history of pulses of mantle plume upwellings and their relation with a deep-r
224 spreading ridges or in intra-plate settings, mantle plumes may generate hotspots, large igneous provi
226 acteristic of the roots of some of the broad mantle plumes tomographically imaged within the large lo
227 ow that, among hotspots suggested to overlie mantle plumes, those with the highest maximum (3)He/(4)H
228 hat existing estimates for the oceanic upper mantle potential temperature be adjusted upward by about
229 ps delineate regions potentially affected by mantle processes, crustal heterogeneity and active tecto
230 provinces, as the surface expression of deep mantle processes, play a key role in the evolution of th
232 ation status, history of high-risk lesion or mantle radiation), tumor histopathologic results, and ti
234 reconstruction of the Andes constructed in a mantle reference frame that the Nazca slab has retreated
237 dictions that Earth has highly reducing deep mantle regions capable of precipitating a metallic iron
238 South-Central Tibet, interpreted as an upper-mantle remnant from earlier lithospheric foundering.
241 eneath the Afar triple junction, imaging the mantle response during progressive continental breakup.
245 ember models at the 1sigma level, define the mantle's radiogenic contribution to the surface heat los
247 esides in the deep mantle, beneath the upper mantle sampled by mid-ocean-ridge basalts, and that buoy
250 )He values, hotspot buoyancy flux, and upper-mantle shear wave velocity to mean that hot plumes-which
253 roterozoic surface material in the deep HIMU mantle source, a multi-stage evolution is revealed for t
254 alt (MORB) magmas, suggesting that the upper mantle sources of Hawaiian magmas have higher fO2 than M
261 ith other drivers, an overpressured sub-slab mantle supporting the weight of the slab in an advancing
262 understanding of the evolution of the plate-mantle system in which plumes rise from the edges of the
263 fies the along-arc variations in the sub-arc mantle temperature, providing a simple mechanism for vol
267 A unique structure in the Earth's lowermost mantle, the Perm Anomaly, was recently identified beneat
268 crete spatial expression patterns within the mantle tissue, hinting at modular organisation, which is
270 apes core sequestration by reacting with the mantle to form iron-rich postbridgmanite or ferropericla
271 84)W, ranging from that of the ambient upper mantle to ratios as much as 18 parts per million lower.
272 small lateral offset between the surface and mantle traces of the thrust system reveals a steep bound
274 ikely that silicate melt above and below the mantle transition zone, and atop the core-mantle boundar
275 hat buoyantly upwelling plumes from the deep mantle transport high-(3)He/(4)He material to the shallo
276 and demonstrate that flow in the deep lower mantle under the north Pacific was anomalously vigorous
277 seismic low-velocity anomalies in the upper mantle, unlike plume-fed hotspots with only low maximum
278 heavy FeO2-bearing patches in the deep lower mantle, upward migration of hydrogen, and separation of
279 e hypothesis that LLSVPs signify large-scale mantle upwelling in two antipodal regions of the mantle.
283 reduced tomographic resolution in the middle mantle, we show that it may alternatively relate to real
284 ile elements from the subducting slab to the mantle wedge and makes Mg isotopes an excellent tracer o
285 in the slab are released as fluids into the mantle wedge and this process is widely considered to re
286 mantle-wedge, which requires a cold hydrated mantle wedge beneath Mount St Helens (< approximately 70
287 gration of these fluids from the slab to the mantle wedge could therefore provide the oxidized source
289 of back-arc temperature perturbations on the mantle wedge flow pattern and sub-arc mantle temperature
291 m the slab-mantle interface to the overlying mantle wedge, in particular where fluids are stable over
295 e west are attributed to serpentinite in the mantle-wedge, which requires a cold hydrated mantle wedg
297 terial from the oxidized surface to the deep mantle, which is then returned to the surface as a compo
298 ed pressure-release melting in the uppermost mantle, which may have induced a surge in magma and CO2
299 in could remain isolated from the convecting mantle, which may help to explain the preservation of ea
300 , we create a set of vote maps for the lower mantle with 14 global P-wave or S-wave tomography models
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