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These reconstructions rely on benthic foraminifera incorporating and retaining unaltered the ambient isotopic compositions of pore fluids and bottom waters. Comparisons are made here of isotopic compositions of abundant live and fossil foraminifera (\u003Cjats:italic>Uvigerina peregrina, Epistominella pacifica, Bulimina mexicana\u003C\u002Fjats:italic>, and \u003Cjats:italic>Globobulimina pacifica\u003C\u002Fjats:italic>) collected in Monterey Bay, CA from two cold seeps (Clam Flats and Extrovert Cliffs) and from sediments ∼5 m outside of the Clam Flats seep. Clam Flats has steep δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C\u003Cjats:sub>DIC\u003C\u002Fjats:sub> gradients (to <−45‰), but DIC at Extrovert Cliffs is less enriched in \u003Cjats:sup>12\u003C\u002Fjats:sup>C (to approximately −22‰). Oxygen isotope values of fossil foraminifera at Clam Flats are ∼1.5‰ enriched in \u003Cjats:sup>18\u003C\u002Fjats:sup>O over the living foraminifera, as well as those of both live and fossil foraminifera at Extrovert Cliffs, suggesting they may have lived during the last glacial maximum. Statistical comparisons (Student's t and Kolmogorov‐Smirnov tests) of δ\u003Cjats:sup>13\u003C\u002Fjats:sup>C and δ\u003Cjats:sup>18\u003C\u002Fjats:sup>O values indicate that live and fossil foraminifera come from different populations at both Clam Flats and Extrovert Cliffs. At Clam Flats, the difference appears to result from alteration enriching some fossil foraminifera in \u003Cjats:sup>12\u003C\u002Fjats:sup>C over live foraminifera. At Extrovert Cliffs, the fossil foraminifera are enriched in \u003Cjats:sup>13\u003C\u002Fjats:sup>C over the live foraminifera, suggesting they lived prior to the onset of venting and thus that venting began recently. The short time of venting at Extrovert Cliffs may be responsible for the less alteration there compared with Clam Flats. 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However, values for key parameters that characterize gas and water flows during hydrate dissociation have not been identified due to experimental challenges. This study utilizes the combined techniques of micro‐focus X‐ray computed tomography (CT) and pore‐network model simulation to identify proper values for those key parameters, such as gas entry pressure, residual water saturation, and curve fitting values. Hydrates with various saturation and morphology are realized in the pore‐network that was extracted from micron‐resolution CT images of sediments recovered from the hydrate deposit at the Mallik site, and then the processes of gas invasion, hydrate dissociation, gas expansion, and gas and water permeability are simulated. Results show that greater hydrate saturation in sediments lead to higher gas entry pressure, higher residual water saturation, and steeper water retention curve. An increase in hydrate saturation decreases gas permeability but has marginal effects on water permeability in sediments with uniformly distributed hydrate. Hydrate morphology has more significant impacts than hydrate saturation on relative permeability. Sediments with heterogeneously distributed hydrate tend to result in lower residual water saturation and higher gas and water permeability. In this sense, the Brooks‐Corey model that uses two fitting parameters individually for gas and water permeability properly capture the effect of hydrate saturation and morphology on gas and water flows in hydrate‐bearing sediments.\u003C\u002Fjats:p>",{"EN":478},"The water retention curve and relative permeability for gas production from hydrate‐bearing sediments: pore‐network model 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This form is legitimate for homogenous materials, but it is impossible to formulate a general equation of state for a polyphase aggregate, e.g., a rock, as a function of pressure and temperature because these variables cannot distinguish all possible states of the aggregate. In consequence, the governing equations of a geodynamic model based on a pressure‐temperature equation of state are singular at the conditions of low‐order phase transformations. An equation of state as a function of specific entropy, specific volume, and chemical composition eliminates this difficulty and, additionally, leads to a robust formulation of the energy and mass conservation equations. In this formulation, energy and mass conservation furnish evolution equations for entropy and volume and the equation of state serves as an update rule for temperature and pressure. Although this formulation is straightforward, the computation of phase equilibria as a function of entropy and volume is challenging because the equations of state for individual phases are usually expressed as a function of temperature and pressure. This challenge can be met by an algorithm in which continuous equations of state are approximated by a series of discrete states: a representation that reduces the phase equilibrium problem to a linear optimization problem that is independent of the functional form used for the equations of state of individual phases. Because the efficiency of the optimization decays as an exponential function of the dimension of the function to be optimized, direct solution of the linearized optimization problem is impractical. Successive linear programming alleviates this difficulty. A pragmatic alternative to optimization as an explicit function of entropy and volume is to calculate phase relations over the range of pressure‐temperature conditions of interest. Numerical interpolation can then be used to generate tables for any thermodynamic property as a function of any choice of independent variables. 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The experiments are designed to mimic low degrees of anhydrous melting beneath mid‐ocean ridges. The available data indicate that the partition coefficients are pressure, temperature, and composition dependent. Therefore partitioning behavior over the appropriate range of pressure, temperature, and composition must be quantified, in order to model continuous extraction of melt during the adiabatic rise of mantle material. For this purpose, we have parameterized the partitioning behavior of the REE, Hf, Zr, U, and Th based on a simple thermodynamic model. Although these parameterizations cannot be used for retrieving thermodynamic constants yet, they do yield accurate descriptions of the partitioning behavior that are useful for modeling decompression melting. Our parameterizations show that the partitioning of trace elements is strongly dependent on the Ca and Al‐content of the clinopyroxene (cpx) and REE are always incompatible in cpx on the peridotite solidus at pressures up to 3.4 GPa. For garnet the data indicate that the heavy REE partition coefficients decrease with increasing pressure. Our data also indicates that Pb is more incompatible than Ce in clinopyroxene; Ce and Pb have similar partition coefficients in garnet. Therefore the presence of a residual phase with high Pb partition coefficients is required to produce the near‐constant Ce\u002FPb ratios in MORB and OIB. Sulfides are the most likely phase to buffer the Pb content in the melt. Except at small porosities (<0.3%), clinopyroxene on the peridotite solidus is unable to fractionate U from Th significantly (15% \u003Cjats:sup>230\u003C\u002Fjats:sup>Th‐excess), whereas garnet can fractionate U from Th effectively at porosities up to 1%. Therefore if the \u003Cjats:sup>230\u003C\u002Fjats:sup>Th‐excesses in mid‐ocean ridge basalts are melting phenomena, then melting with garnet residual is required in order to be compatible with physical observations on porosities and upwelling rate at mid‐ocean ridges. New model calculations that include the compositional dependent partitioning of the trace elements show that the predicted physical characteristics (depth and extent of melting, upwelling rate, porosity) of the MORB melting regime are similar for the Lu\u002FHf, Sm\u002FNd, and U‐Th systems.\u003C\u002Fjats:p>",{"EN":1802},"Near mantle solidus trace element partitioning at pressures up to 3.4 GPa",{"VOID":1804},"10.1029\u002F2001gc000148","2025-02-08T08:29:49.160+00:00",[154],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2001GC000148",[1809,1828,1845],{"id":1810,"sortIndex":20,"researcher":19,"roles":1811,"affiliations":1812,"properties":1821},"3c73667d-cbdf-4bd4-84a6-16b0a223251b",[],[1813],{"id":1814,"sortIndex":20,"affiliation":1815,"properties":19},"6ba7830a-7b93-424e-a398-b552e2414363",{"id":1814,"createTime":19,"updateTime":19,"relativeEntities":1816,"slug":19,"properties":1817,"entityType":19,"verifyStatus":19,"verifyTime":19,"verifyNote":19,"languages":19,"translateLanguages":19,"viewCount":19,"url":19,"parentIds":1820,"statistic":19},[],{"title":1818},{"EN":1819},"National High Magnetic Field Laboratory and Department of Geological Sciences 1800 E. 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The most mafic shoshonitic lavas (absarokites) range from 8.4 to 15.2 wt % MgO and are variably clinopyroxene + olivine‐phyric. Fijian shoshonitic suites display a range of enrichment in large ion lithophile elements, Th, U, and P relative to rare earth elements and high field strength elements (HFSE), reflecting variable contributions by the subarc mantle source and subduction‐related components. The subarc mantle source component controls HFSE, heavy rare earth elements, to a lesser degree light rare earth elements (LREE), and most importantly the sensitivity of the mantle source with respect to subduction‐related enrichment processes, whereas Pb, K, Sr, Ba, Rb, Th, U, P\u003Cjats:sub>2\u003C\u002Fjats:sub>O\u003Cjats:sub>5\u003C\u002Fjats:sub>, and LREE are contributed by hydrous or supercritical fluid(s) and sediment melts that are added to the subarc mantle. Fijian shoshonitic suites situated ∼150 km apart display a wide range of Nb\u002FYb (0.3–4.3), implying that there is significant spatial heterogeneity in the sub‐Fijian mantle with respect to the ambient fertility of mantle sources independent of subduction‐related enrichment. The range in incompatible element ratios (e.g., Th\u002FNb, U\u002FNb, Ba\u002FTh, Ba\u002FLa, P\u002FNd, and Ce\u002FPb) displayed by Fijian shoshonitic suites cannot reflect addition of the same subduction‐derived component to variably enriched subarc mantle sources. Differences in the relative amount of fluid versus sediment melt and potentially the composition of the subducted sediment are required to explain the data. The greater overall subduction‐related enrichment in Fijian shoshonites relative to calk‐alkaline and tholeiitic arc magmas is attributed to a melt generation process involving low‐degree partial melting of metsomatized subarc lithosphere in contrast to magmas associated with active or steady state arcs, where higher degrees of melting occur in response to volatile fluxing of the mantle wedge. Shoshonitic magma generation occurs in linear zones during extension of the arc lithosphere preceding arc fragmentation and establishment of back‐arc spreading centers.\u003C\u002Fjats:p>",{"EN":2157},"Primitive shoshonites from Fiji: Geochemistry and source components",{"VOID":2159},"10.1029\u002F2008gc002326",[154],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2008GC002326",[2163,2180,2197,2212],{"id":2164,"sortIndex":20,"researcher":19,"roles":2165,"affiliations":2166,"properties":2175},"388153cf-d267-483a-9e69-a9465d9dc20c",[],[2167],{"id":2168,"sortIndex":20,"affiliation":2169,"properties":19},"ef4e09f6-157f-4463-89cf-7ccacc65f4e9",{"id":2168,"createTime":19,"updateTime":19,"relativeEntities":2170,"slug":19,"properties":2171,"entityType":19,"verifyStatus":19,"verifyTime":19,"verifyNote":19,"languages":19,"translateLanguages":19,"viewCount":19,"url":19,"parentIds":2174,"statistic":19},[],{"title":2172},{"EN":2173},"ARC Centre of Excellence in Ore Deposits, School of Earth Sciences, University of Tasmania, Private Bag 79, Hobart, Tasmania, 7001, Australia",[],{"title":2176,"openalex":2178},{"EN":2177},"Roman A. 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Samples recovered in situ record deformation restricted to the cold (shallow) lithosphere (greenschist facies), with no evidence for significant high‐temperature deformation either at the fault zone or in the footwall near it. High‐temperature deformation (∼720–750°C) is observed only at two sites, and cannot be directly linked to the detachment. Detachment faulting was coeval with dyke intrusions that cross cut it, as demonstrated by the presence of undeformed and highly deformed diabase found in shear zones, and by the presence of chill margins in diabase against fault rock. Basalts are very scarce and restricted to clasts in breccias, with no evidence of pillows or extrusive structures. Gabbros crop out along mass‐wasted and fault scarps structurally below the detachment. Footwall rocks show little or no deformation, due to strain localization along a narrow shear zone (<200 m) with fluid flow, as required to form talc‐ and amphibole schists after an ultramafic protolith. We speculate that the alteration front in a heterogeneous lithosphere may be a rheological boundary that may localize deformation during long periods of time. Our observations and other geological evidence elsewhere suggest that this detachment model limited to the cold (shallow) lithosphere is applicable to other corrugated surfaces along slow‐ and intermediate‐spreading ridges. These observations preclude detachment models rooting in melt‐rich zones (i.e., Atlantis Bank, Southwest Indian Ridge) or recording high‐temperature deformation. We infer that oceanic detachment faults (1) localize strain at T < 500–300°C, (2) persist during active magmatism, and (3) root at shallow rheological boundaries, such as a melt‐rich zone or magma chamber (“hot” detachments) or an alteration front (“cold” detachments).\u003C\u002Fjats:p>",{"EN":2647},"Constraints on deformation conditions and the origin of oceanic detachments: The Mid‐Atlantic Ridge core complex at 15°45′N",{"VOID":2649},"10.1029\u002F2002gc000472","2025-02-07T12:40:37.064+00:00",[154],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2002GC000472",[2654,2673,2690,2709],{"id":2655,"sortIndex":20,"researcher":19,"roles":2656,"affiliations":2657,"properties":2666},"fcf40537-7896-40d4-ae2e-830014421377",[],[2658],{"id":2659,"sortIndex":20,"affiliation":2660,"properties":19},"61e36c3e-0029-4a4e-bb41-e2d9ba2da14c",{"id":2659,"createTime":19,"updateTime":19,"relativeEntities":2661,"slug":19,"properties":2662,"entityType":19,"verifyStatus":19,"verifyTime":19,"verifyNote":19,"languages":19,"translateLanguages":19,"viewCount":19,"url":19,"parentIds":2665,"statistic":19},[],{"title":2663},{"EN":2664},"Laboratoire de Geosciences Marines (CNRS UMR7097), Institut de Physique du Globe, 75252 Paris, France",[],{"orcid":2667,"title":2669,"openalex":2671},{"VOID":2668},"https:\u002F\u002Forcid.org\u002F0000-0002-3416-6856",{"EN":2670},"J. 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A., 1974, Guidebook, Death Valley Region, California and Nevada, 27",{},{"id":3043,"createTime":3044,"updateTime":3044,"relativeEntities":3045,"slug":3046,"properties":3047,"entityType":150,"verifyStatus":151,"verifyTime":3058,"verifyNote":152,"languages":3059,"translateLanguages":19,"viewCount":20,"primaryUrl":3060,"fullTextUrl":19,"authors":3061,"publicationType":262,"publisherRelationship":3100,"citationCount":3150,"citationInfo":3151,"publishDate":3154,"publishYear":3152,"citationAnalyzeStatus":18,"lastCitationAnalyze":19,"indexDatabases":3155,"openAccess":19,"references":3156,"isForceReanalyzing":463},"b104ae48-835c-449f-9092-8aefcfb5a423","2025-02-06T14:43:35.178+00:00",[],"Rheologic-controls-on-slab-dynamics",{"openalex":3048,"mag":3050,"abstract":3052,"title":3054,"doi":3056},{"VOID":3049},"W1488619614",{"VOID":3051},"1488619614",{"EN":3053},"\u003Cjats:p>Several models have been proposed to relate slab geometry to parameters such as plate velocity or plate age. However, studies on the observed relationships between slab geometry and a wide range of subduction parameters show that there is not a simple global relationship between slab geometry and any one of these other subduction parameters for all subduction zones. Numerical and laboratory models of subduction provide a method to explore the relative importance of different physical processes in determining subduction dynamics. Employing 2‐D numerical models with a viscosity structure constrained by laboratory experiments for the deformation of olivine, we show that the observed range in slab dip and the observed trends between slab dip and convergence velocity, subducting plate age, and subduction duration can be reproduced without trench motion (i.e., slab roll‐back) for locations away from slab edges. Successful models include a stiff slab that is 100–1000 times more viscous than previous estimates from models of plate bending, the geoid, and global plate motions. We find that slab dip in the upper mantle depends primarily on slab strength and plate boundary coupling, with a small dependence on subducting plate age. Once the slab sinks into the lower mantle the primary processes controlling slab evolution are (1) the ability of the stiff slab to transmit stresses up dip, (2) resistance to slab descent into the higher‐viscosity lower mantle, and (3) subduction‐induced flow in the mantle‐wedge corner.\u003C\u002Fjats:p>",{"EN":3055},"Rheologic controls on slab dynamics",{"VOID":3057},"10.1029\u002F2007gc001597","2025-02-06T14:43:35.177+00:00",[154],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2007GC001597",[3062,3081],{"id":3063,"sortIndex":20,"researcher":19,"roles":3064,"affiliations":3065,"properties":3074},"4e3b7b1d-e980-4649-a2b0-7b8897419aae",[],[3066],{"id":3067,"sortIndex":20,"affiliation":3068,"properties":19},"da671019-4244-4190-8129-ea80b105b92d",{"id":3067,"createTime":19,"updateTime":19,"relativeEntities":3069,"slug":19,"properties":3070,"entityType":19,"verifyStatus":19,"verifyTime":19,"verifyNote":19,"languages":19,"translateLanguages":19,"viewCount":19,"url":19,"parentIds":3073,"statistic":19},[],{"title":3071},{"EN":3072},"Department of Geology, University of California, Davis, One Shields Avenue,, Davis, California, 95616 USA",[],{"orcid":3075,"title":3077,"openalex":3079},{"VOID":3076},"https:\u002F\u002Forcid.org\u002F0000-0002-7316-1791",{"EN":3078},"M. 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When analyzed separately, underside \u003Cjats:italic>P\u003C\u002Fjats:italic> and \u003Cjats:italic>S\u003C\u002Fjats:italic> reflections (\u003Cjats:italic>PdP\u003C\u002Fjats:italic> and \u003Cjats:italic>SdS\u003C\u002Fjats:italic>) are suggestive of very different structures despite similar raypaths and data coverage. By stacking the radial component of \u003Cjats:italic>PdP\u003C\u002Fjats:italic> rather than the vertical \u003Cjats:italic>PdP\u003C\u002Fjats:italic>, we show that this difference does not result from interference from other more steeply inclined phases such as \u003Cjats:italic>PKP\u003C\u002Fjats:italic> and \u003Cjats:italic>Ppdp\u003C\u002Fjats:italic>\u003Cjats:sub>\u003Cjats:italic>diff\u003C\u002Fjats:italic>\u003C\u002Fjats:sub>. In general, stacks of \u003Cjats:italic>P\u003C\u002Fjats:italic>‐to‐\u003Cjats:italic>S\u003C\u002Fjats:italic> converted phases (\u003Cjats:italic>Pds\u003C\u002Fjats:italic>) appear to lack evidence of a 520‐km discontinuity when examined without other phases. When these phases and stacked topside \u003Cjats:italic>P\u003C\u002Fjats:italic> reflections (\u003Cjats:italic>Ppdp\u003C\u002Fjats:italic>) are analyzed jointly using a nonlinear inversion method, consistent but nonunique, seismological models emerge. These models show that a discontinuity at ∼653 km depth has smaller contrasts in density and velocity than found in most previous studies. A sub‐660 gradient can account for the majority of this difference. A 1.6 ± 0.5% \u003Cjats:italic>P\u003C\u002Fjats:italic>‐velocity contrast and a 2.2 ± 0.3% density contrast at ∼518 km depth without a \u003Cjats:italic>S\u003C\u002Fjats:italic>‐velocity contrast can explain the lack of a \u003Cjats:italic>P\u003C\u002Fjats:italic>520\u003Cjats:italic>s\u003C\u002Fjats:italic>, together with robust \u003Cjats:italic>Pp\u003C\u002Fjats:italic>520\u003Cjats:italic>p\u003C\u002Fjats:italic> and \u003Cjats:italic>S\u003C\u002Fjats:italic>520\u003Cjats:italic>S \u003C\u002Fjats:italic>phases. For models parameterized with a finite thickness for each discontinuity, the 410‐km discontinuity is consistently ∼3 times thicker than the 660‐km discontinuity.\u003C\u002Fjats:p>",{"EN":3368},"Constraining seismic velocity and density for the mantle transition zone with reflected and transmitted waveforms",{"VOID":3370},"10.1029\u002F2006gc001339","2025-02-06T14:43:33.170+00:00",[154],"https:\u002F\u002Fagupubs.onlinelibrary.wiley.com\u002Fdoi\u002F10.1029\u002F2006GC001339",[3375,3392],{"id":3376,"sortIndex":20,"researcher":19,"roles":3377,"affiliations":3378,"properties":3387},"908db9c5-15cd-4be0-b0b4-cb98be999c4b",[],[3379],{"id":3380,"sortIndex":20,"affiliation":3381,"properties":19},"cf60eeb6-813c-4a2d-9917-57889c363ca5",{"id":3380,"createTime":19,"updateTime":19,"relativeEntities":3382,"slug":19,"properties":3383,"entityType":19,"verifyStatus":19,"verifyTime":19,"verifyNote":19,"languages":19,"translateLanguages":19,"viewCount":19,"url":19,"parentIds":3386,"statistic":19},[],{"title":3384},{"EN":3385},"IGPP Scripps Institution of Oceanography 9500 Gilman Drive, IGPP 0225 La Jolla California USA",[],{"title":3388,"openalex":3390},{"EN":3389},"J. 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