Infiltration Of Aqueous Fluids Research Articles

The redox budget of the Mariana subduction zone

Assessing the efficiency of material recycling at convergent margins is critical to constraining the impact of plate tectonic processes on the composition of surface and deep mantle reservoirs on geologic timescales. In particular, oceanic lithosphere bearing oxidized phases such as Fe-oxy-hydroxides, Fe-oxides, serpentine, carbonate, and sulfate minerals, subduct at convergent margins and the infiltration of aqueous fluids and sediment melts from the subducting slab into the mantle beneath arc volcanoes may thus carry oxidized forms of multi-valent elements (e.g., S, Fe, C) and lead to the generation of primitive arc melts that record elevated oxygen fugacities relative to mid-ocean ridge primitive melts. It is unclear, however, how efficiently aqueous fluids and silicate melts transport the oxidized signatures of any given subducting slab into the mantle wedge in a single subduction zone, and how much, if any, of these oxidized phases may be recycled into the deeper mantle. We present a mass balance of Fe3+, S2−, S6+, and C4+, as well as the O2 associated with these species, through the Mariana subduction zone to assess the efficiency of recycling oxidized materials in an end-member type subduction zone, where old oceanic lithosphere and a thick sediment package is subducted. To do this, we report Fe3+/ΣFe ratios of bulk sediments and altered oceanic crust recovered from ODP Site 801 in the western Pacific in order to constrain the bulk Fe3+/ΣFe ratio of the Pacific plate prior to subduction in the Mariana convergent margin. Site 801 sediments have Fe3+/ΣFe ratios >0.69 and the altered oceanic crust (801 Super Composite) has Fe3+/ΣFe of 0.51. Bulk Fe3+/ΣFe ratios of altered oceanic crust at Site 801 increase from 0.14 (pristine Jurassic-aged MORB glass) to 0.78 with increasing extent of alteration. We find that 68–95% of the O2 added to the subducting crust by sedimentation, in situ alteration of basaltic crust on the seafloor, and serpentinization of the mantle lithosphere is not output by Mariana arc or back-arc magmas. This result demonstrates that significant amounts of oxidized materials from Earth's surface are transported into the deeper mantle beyond subduction zones, despite the production of oxidized arc and back-arc basalts, and may contribute to elevated oxygen fugacities recorded by ocean island lavas such as Iceland and Hawaii. This oxygen cycle is likely to have been operating at least for the past 400–800 million years, and potentially for the duration of plate tectonics.

Granitoids of the Pozdnestanovoy Complex of the Dzhugdzhur–Stanovoy Superterrane, Central Asia Fold Belt: Age, Tectonic Setting, and Sources

The geochemistry, geochronology, and isotope geochemical systematics (Nd, Sr, Hf, and Pb) of the granitoids of the Pozdnestanovoy complex of the Dzhugdzhur–Stanovoy superterrane of the Central Asia fold belt were investigated. It was shown that their age is Mesozoic (142–138 Ma) rather than Early Precambrian, as was previously supposed. The main sources of parental melts for these granitoids were the Neoarchean and Paleoproterozoic rocks of the lower continental crust of the Dzhugdzhur–Stanovoy superterrane and the rocks of the Late Paleozoic–Early Mesozoic continental crust of the Amur microplate. They were formed at depths of >40 km and temperatures of 700–800°C, most likely through the melting of mafic feldspar granulites under the conditions of aqueous fluid infiltration without any significant contribution from a juvenile heat source. The granitoids of the Pozdnestanovoy complex were emplaced during the closure of the eastern segment of the Mongolia–Okhotsk Ocean owing to the collision of the Siberian and Sino-Korean continents.

電気石を用いた含ホウ素H2O流体活動と部分溶融過程制約の試み―ネパールヒマラヤ東部・ダンクッタ地域の例

電気石を用いた含ホウ素H2O流体活動と部分溶融過程制約の試み―ネパールヒマラヤ東部・ダンクッタ地域の例

Porosity generated during the fluid-mediated replacement of calcite by fluorite

Mineral replacement reactions are common phenomena in natural and laboratory environments where solids have re-equilibrated with aqueous solutions and are characterized by the generation or destruction of porosity in the product phase(s). Here, the evolution of porosity during the replacement of calcite by fluorite is used as a model system to characterize the kinetics of volume variations. Non-porous single crystals of calcite were reacted with sodium fluoride solutions for different reaction times. The crystals were pseudomorphically replaced by highly porous fluorite. Complementary use of porosimetry techniques, high resolution imaging, and mass-balance calculations revealed the total, open, and closed porosity in the samples. The infiltration of aqueous fluids in the Earth depends on the evolution of porosity and hence porosity variations are important in various geological processes such as, rock weathering and soil formation, fluid-controlled metamorphism, mineral ore emplacement, or oil and gas reservoir compaction. Such mechanisms can also be used to develop geo-inspired materials designed for industrial and medical applications.

Talc–carbonate alteration of ultramafic rocks within the Leka Ophiolite Complex, Central Norway

Petrographic and geochemical analyses of partly and completely serpentinized and carbonated peridotites within the ultramafic section of the Leka Ophiolite Complex have been used to elucidate the evolution of alterations and identify possible fluid sources. The alterations show no evidence for any major deformation and are located along low-angle structures that were formed in a late stage of the structural evolution of the ophiolite complex. Modeling of mineral equilibria in the SiO2–MgO–FeO–Fe2O3–CaO–H2O±CO2 system has been utilized to constrain the conditions during serpentinization and carbonation.The partly altered peridotites consist of the mineral assemblage olivine–clinopyroxene–serpentine–magnetite–brucite and formed at temperatures <410°C by infiltration of aqueous fluids. Completely serpentinized rocks with the mineral assemblage serpentine–magnesite–magnetite–dolomite formed at temperatures <500°C and low XCO2 (≤0.05) by the breakdown of the minerals in the partly altered peridotites. Talc–carbonate rocks formed by the breakdown of the serpentine in the previously formed serpentinite rock at temperatures <550°C and elevated XCO2, which resulted in the stabilization of the assemblage talc–magnesite–magnetite–dolomite. Carbon isotope values determined for dolomite from crosscutting carbonate lenses within the talc–carbonate rock yield δ13C values of ~−5 indicative of a mantle source for the carbon required for the carbonation. Oxygen isotope values δSMOW18O of ~10.8–11.3‰ together with initial 87Sr/86Sri=400Ma values of 0.7029 and 0.7063, suggest dehydration of rocks with mantle affinity as a source for the fluids. Based on analytical results and field observations we propose that the formation of the talc- and carbonate-bearing alteration zones is caused by the focused infiltration of fluids that originated at the bottom of already partly serpentinized ophiolite complex during extension-driven burial at the late stage of the Caledonian orogeny.

Syn-metamorphic aqueous fluid infiltration and petrogenesis of tourmaline leucogranites in the MCT zone, Dhankuta area, Eastern Nepal

Syn-metamorphic aqueous fluid infiltration and petrogenesis of tourmaline leucogranites in the MCT zone, Dhankuta area, Eastern Nepal

Fluid–rock interactions during UHP metamorphism: A review of the Dabie–Sulu orogen, east-central China

Comprehensive review on the characteristics of petrology, oxygen isotope, fluid inclusion and nominally anhydrous minerals (NAMs) for many Dabie–Sulu ultrahigh-pressure (UHP) metamorphic rocks including drill-hole core samples reveals that fluid has played important and multiple roles during complicated fluid–rock interactions attending the subduction and exhumation of supracrustal rocks. We have identified several distinct stages of fluid–rock interactions as follows: (1) The Neoproterozoic supercrustal protoliths of UHP rocks experienced variable degrees of hydration through interactions with cold meteoric water with extremely low oxygen isotope compositions during Neoproterozoic Snow-ball Earth time. (2) A series of dehydration reactions took place during Triassic subduction of the Yangtze plate beneath the Sino-Korean plate; the released fluid entered mainly into volatile-bearing high-pressure (HP) and UHP minerals, such as phengite, zoisite-epidote, talc, lawsonite and magnesite, as well as into UHP NAMs, such as garnet, omphacite and rutile. (3) Silicate-rich supercritical fluid (hydrous melt) existed during the UHP metamorphism at mantle depths >100 km which mobilized many normally fluid-immobile elements and caused unusual element fractionation. (4) The fluid exsolved from the NAMs during the early exhumation of the Dabie–Sulu terrane was the main source for HP hydrate retrogression and generation of HP veins. (5) Local amphibolite-facies retrogression at crustal depths took place by infiltration of aqueous fluid of various salinities possibly derived from an external source. (6) The greenschist-facies overprinting and low-pressure (LP) quartz veins were generated by fluid flow along ductile shear zones and brittle faults during late-stage uplift of the UHP terrane.

Metasomatic tourmaline in hybrid contact-bands between gneiss and peridotite in the Ulten zone of the Eastern Italian Alps: chemistry and boron isotopic composition

Ultramafic rocks in the Ulten Zone (UZ) high-pressure melange, in the Eastern Italian Alps, embedded in crustal gneisses, preserve a series of metasomatic hybrid bands generated by infiltration of aqueous fluids. These hybrid bands at the peridotite–gneiss contact comprise phlogopite and anthophyllite with accessory zircon, apatite and allanite. Here, we report the rare occurrence of centimeter-sized crystals of metasomatic tourmaline in two different UZ outcrops, at Mt. Hochwart and Malga Preghena. Tourmaline has a dravite–uvite-rich composition and shows optical and chemical zoning, with slightly variable Ti, Ca and Fe contents. Secondary-ion mass spectrometry (SIMS) analyses provide information on the intragrain B-isotopic zonation of the grains, which is correlated with optical and chemical zoning. The range in δ 11 B is from −7.4 to +0.3‰ for the Mt. Hochwart tourmaline, generally with an isotopically lighter core and heavier rim. The δ 11 B range for Malga Preghena tourmaline is from +1.2‰ in the core to −3.9‰ in the rim. Variable proportions of fluids derived from both the local crustal gneisses and a subducting slab control the B-isotope composition in the metasomatic tourmaline from the UZ. Fluid mixing in hybrid crustal–ultramafic bands can be monitored by metasomatic tourmaline, which may also have a significant impact on the B isotope budget of the subducted slab and the slab–mantle interface.

Lithium isotopes as a tracer of fluids in a subduction zone mélange: Franciscan Complex, CA

Abstract High-grade blocks of eclogite, blueschist, and garnet amphibolite found in melange terrains in the Franciscan Complex, CA display petrologic and geochemical evidence for a complicated history of interactions with aqueous fluids. These blocks have features (actinolitic rinds, a blueschist layer) that have petrologic and geochemical indicators of interaction with retrograde aqueous fluids. Lithium concentrations and isotopic compositions of different portions of three high-grade blocks are different from those of MORB (their presumed protolith) and show systematic variations associated with fluid-related features. Block cores and an eclogite layer have high whole-rock Li concentrations relative to MORB (17 to 39 ppm) and low to moderate δ7Li (0.4 to 2.1‰). This range of values is inconsistent with dehydration of MORB and is interpreted as the product of infiltration of aqueous fluids with an elevated Li concentration and low δ7Li. Rinds and a blueschist layer exhibit lower Li concentrations (7 to 24 ppm) and higher δ7Li (2.7 to 4.4‰). The differences between cores and rinds, and the eclogite and blueschist layers are interpreted as the product of retrograde infiltration of an aqueous fluid with low Li concentrations and high δ7Li. Results of a small-scale traverse across the boundary between the blueschist and eclogite layers show that the boundary is gradational over ∼ 0.5 cm, suggesting small-scale cross-layer diffusion/dispersion associated with the fluid infiltration. The high Li concentrations and low δ7Li of block cores suggests that the source of early fluids was likely subducted sedimentary rocks. The lower Li concentrations and higher δ7Li values of the rinds and blueschist layers do not fully constrain the source of retrograde fluids, but indicate that the fluid source likely had a lower Li concentration and higher δ7Li.

Genesis of wollastonite- and grandite-rich skarns in a suite of marble-calc-silicate rocks from Sittampundi, Tamil Nadu: constraints on the P–T–fluid regime in parts of the Pan-African mobile belt of South India

The Pan-African tectonothermal activities in areas near Sittampundi, south India, are characterized by metamorphic changes in an interlayered sequence of migmatitic metapelites, marble and calc-silicate rocks. This rock sequence underwent multiple episodes of folding, and was intruded by granite batholiths during and subsequent to these folding events. The marble and the calc-silicate rocks develop a variety of skarns, which on the basis of mineralogy; can be divided into the following types: Type I: wollastonite + clinopyroxene (mg# = 71–73) + grandite (16–21 mol% Adr) + quartz ± calcite, Type II: grandite (25–29 mol% Adr ) + clinopyroxene (mg# = 70) + calcite + quartz, and Type III: grandite (36–38 mol% Adr) + clinopyroxene (mg# = 55–65) + epidote + scapolite + calcite + quartz. Type I skarn is 2–10 cm thick, and is dominated by wollastonite (>70 vol%) and commonly occurs as boudinaged layers parallel to the regional foliation Sn1 related to the Fn1 folds. Locally, thin discontinuous lenses and stringers of this skarn develop along the axial planes of Fn2 folds. The Type II skarn, on the other hand, is devoid of wollastonite, rich in grandite garnet (40–70 vol%) and developed preferentially at the interface of clinopyroxene-rich calc-silicates layers and host marble during the later folding event. Reaction textures and the phase compositional data suggest the following reactions in the skarns: 1. calcite + SiO2 → wollastonite + V, 2. calcite + clinopyroxene + O2 → grandite + SiO2 + V, 3. scapolite + calcite + quartz + clinopyroxene + O2 → grandite + V and 4. epidote + calcite + quartz + clinopyroxene + O2 → grandite + V Textural relations and composition of phases demonstrate that (a) silica metasomatism of the host marble by infiltration of aqueous fluids (XCO2 11 kbar and >950°C) inferred for the Pan-African tectonothermal events from the neighboring areas. Field and petrological attributes of these skarn rocks are consistent with the infiltration of aqueous fluid predominantly during the Fn1 folding event at or close to the ‘peak’ metamorphic conditions. Petrological features indicate that the buffering capacity of the rocks was lost during the formation of type I and II skarns. However, the host rock could buffer the composition of the permeated fluids during the formation of type III skarn. Aqueous fluids derived from prograde metamorphism of the metapelites seem to be the likely source for the metasomatic fluids that led to the formation of the skarn rocks.

The Role of Fluid for Diamond-Free UHP Dolomitic Marble from the Kokchetav Massif

A diamond-free, dolomite-bearing UHP marble showing a banded structure occurs at Kumdy-kol in the Kokchetav Massif, northern Kazakhstan. Three centimeter-scale zones occur in this marble (sample no. Y665): zone A = Ti-clinohumite-bearing dolomitic marble; zone B = dolomite marble; and zone C = dolomitic marble lacking Ti-clinohumite and forsterite. The occurrence of phlogopite and garnet lamellae in diopside in zone C suggests UHP metamorphism. Large-area chemical mapping covering about two-thirds of the sample surface was conducted. Ti-K∝ X-ray images clearly indicate that TiO2 is concentrated in zone A. Ca-K∝ and Mg-K∝ images showed that zones A and C have similar modal compositions of carbonates, but they have strong contrasts in TiO2 contents and mineral paragenesis. Mineral assemblages in each zone were analyzed in terms of the CaO-(MgO, FeO)-TiO2-SiO2 compositional tetrahedron. In zone A, the aragonite-Ti-clinohumite tieline was stable under UHP conditions, whereas it was unstable in zones B and C. This indicates that XCO2 in zone A was lower than that in zones B and C. Infiltration of TiO2-bearing aqueous fluid is implied on the basis of paragenetic relations, distribution of Ti-bearing phases and chemical zonation in Ti-clinohumite in zone A. The lack of microdiamond in this dolomite-bearing carbonate rock suggests extremely low-XCO2 conditions, and implies the infiltration of an aqueous fluid during UHP metamorphism.

Reaction localization and softening of texturally hardened mylonites in a reactivated fault zone, central Argentina

AbstractThe Tres Arboles ductile fault zone in the Eastern Sierras Pampeanas, central Argentina, experienced multiple ductile deformation and faulting events that involved a variety of textural and reaction hardening and softening processes. Much of the fault zone is characterized by a (D2) ultramylonite, composed of fine‐grained biotite + plagioclase, that lacks a well‐defined preferred orientation. The D2 fabric consists of a strong network of intergrown and interlocking grains that show little textural evidence for dislocation or dissolution creep. These ultramylonites contain gneissic rock fragments and porphyroclasts of plagioclase, sillimanite and garnet inherited from the gneissic and migmatitic protolith (D1) of the hangingwall. The assemblage of garnet + sillimanite + biotite suggests that D1‐related fabrics developed under upper amphibolite facies conditions, and the persistence of biotite + garnet + sillimanite + plagioclase suggests that the ultramylonite of D2 developed under middle amphibolite facies conditions. Greenschist facies, mylonitic shear bands (D3) locally overprint D2 ultramylonites. Fine‐grained folia of muscovite + chlorite ± biotite truncate earlier biotite + plagioclase textures, and coarser‐grained muscovite partially replaces relic sillimanite grains. Anorthite content of shear band (D3) plagioclase is c. An30, distinct from D1 and D2 plagioclase (c. An35). The anorthite content of D3 plagioclase is consistent with a pervasive grain boundary fluid that facilitated partial replacement of plagioclase by muscovite. Biotite is partially replaced by muscovite and/or chlorite, particularly in areas of inferred high strain. Quartz precipitated in porphyroclast pressure shadows and ribbons that help define the mylonitic fabric. All D3 reactions require the introduction of H+ and/or H2O, indicating an open system, and typically result in a volume decrease. Syntectonic D3 muscovite + quartz + chlorite preferentially grew in an orientation favourable for strain localization, which produced a strong textural softening. Strain localization occurred only where reactions progressed with the infiltration of aqueous fluids, on a scale of hundreds of micrometre. Local fracturing and microseismicity may have induced reactivation of the fault zone and the initial introduction of fluids. However, the predominant greenschist facies deformation (D3) along discrete shear bands was primarily a consequence of the localization of replacement reactions in a partially open system.

Rochas metaultramáficas de Lamim, sul do Quadrilátero Ferrífero, MG: contribuição ao conhecimento do protólito da pedra-sabão

A região de Lamim, sudeste do Quadrilátero Ferrífero (QF), é constituída de gnaisses e rochas metamáficas e metaultramáficas, estas do Grupo Nova Lima, base do greenstone belt Rio das Velhas. As principais rochas metaultramáficas são pedra-sabão, amplamente explotada no QF, e serpentinito. A região distingue-se por rochas com olivina preservada, interpretadas como o protólito magmático das metaultramáficas. São olivina-anfibólio fels com textura semelhante a cumulus, com inclusão de vários grãos de olivina em anfibólio de porte maior. O teor relativamente alto de ferro da olivina (Fo75Fa25) indica a sua origem magmática. Há dois tipos de anfibólio, cristais centimétricos de tremolita, envolvendo vários grãos de olivina, interpretados como pseudomorfoses, substituindo o piroxênio intercumulus original, e antofilita acicular. Os teores de serpentina, clorita, dolomita e talco variam. A composição química e as texturas sugerem que o provável protólito das rochas metaultramáficas são komatiitos peridotíticos plutônicos e não komatiitos vulcânicos encontrados em outras regiões do QF. O peridotito foi variavelmente metamorfizado em condições de fácies xisto verde alto a anfibolito baixo durante a infiltração de fluidos aquosos que acompanharam o processo metamórfico-metassomático.

Melt Generation and Fluid Flow in the Thermal Aureole of the Bushveld Complex

Granite sheets emplaced into the migmatite zone of the eastern contact aureole of the Bushveld Complex resulted from fluid-enhanced, incongruent biotite melting of the underlying Silverton Formation shales during prograde metamorphism. Ba concentrations are extreme in both the sheets (>1000 ppm) and the hornfels (>800 ppm) into which they have been emplaced. We conclude that a Ba-rich, hydrothermal fluid induced melting in the aureole, and that fluid transport of Ba2+, and to a lesser extent, Sr2+ and Eu2+, persisted in the melt zones under subsolidus conditions. Sr-isotope systematics from high-Ba localities define an errorchron of 2161 ± 106 Ma with an initial (87Sr/86Sr) ratio of 0·705 ± 0·001. Metasedimentary rocks unaffected by fluid infiltration were homogenized at the same time but with an increased initial ratio, suggesting that whereas isotope homogenization was achieved between outcrops permeated by fluids, there is no evidence of regional homogenization. Oxygen-isotope compositions of psammitic metasediments in the aureole are uncorrelated with distance from the contact, suggesting the infiltrating fluid equilibrated isotopically with the metasediments. Their elevated δ18O values (11·3–12·1‰) are consistent with a fluid source from devolatilization of the sedimentary lithologies. Textural analysis at both outcrop and thin-section scale of arkose and psammites in the aureole (Lakenvalei and Magaliesberg Formations) shows that the extent of melting was highly heterogeneous, even on the grain scale, and resulted from heterogeneously distributed infiltration of aqueous fluid on dilatant cracks and grain boundaries. Cathodoluminescence imaging of quartz shows a marked difference in the amount of fine structure, with that in the melted rocks having uniform luminescence in contrast to that in rocks containing little or no melt, which preserve textures inherited from the regionally metamorphosed protolith. Simple finite-difference thermal modelling of the aureole suggests that the width of the melt zone (>500 m) is inconsistent with conductive heat transfer, and hence that the thermal structure has been modified by fluid advection.

U–Pb geochronology from Tonagh Island, East Antarctica: implications for the timing of ultra-high temperature metamorphism of the Napier Complex

Ion microprobe U–Pb zircon geochronology of an orthopyroxene-bearing felsic orthogneiss from central Tonagh Island, Enderby Land, East Antarctica provides insight into the chronological-metamorphic evolution of the Archaean Napier Complex, the details of which have been the source of debate for over two decades. The orthogneiss crystallised at 2626±28 Ma, predating peak, ultra-high temperature (UHT) metamorphism and development of an intense regional S 1 gneissosity. Two subsequent episodes of zircon growth/resetting can be identified. A minor period of zircon growth occurred at 2546±13 Ma, the regional significance and geological nature of which is unclear. This was followed by an episode of abundant zircon growth, as mantles on ∼2626 Ma cores and as anhedral grains, partly characterised by high Th/U (>1.2), at ∼2450–2480 Ma. This age coincides with both lower and upper concordia intercept ages from other U–Pb zircon studies, and several Rb–Sr and Sm–Nd whole-rock isochron ages from the Napier Complex. We conclude that UHT metamorphism occurred at ∼2450–2480 Ma, and find no compelling evidence that UHT occurred much earlier as has been postulated. The zircon U–Pb data from this study also indicates a lower intercept age of ∼500 Ma, which coincides with the emplacement of Early Palaeozoic pegmatite swarms and synchronous infiltration of aqueous fluids into the southwestern regions of the Napier Complex.

Fluid‐rock history of granulite facies humite‐marbles from Ambasamudram, southern India.

AbstractAn extensive humite‐bearing marble horizon within a supracrustal sequence at Ambasamudram, southern India, was studied using petrological and stable isotopic techniques to define its metamorphic history and fluid characteristics. At peak metamorphic temperatures of 775±73°C, based on calcite‐graphite carbon isotope thermometry, the mineral assemblages suggest layer‐by‐layer control of fluid compositions. Clinohumite + calcite‐bearing assemblages suggest XCO2 &lt; 0.4 (at 700°C and 5 kbar), calcite + forsterite + K‐feldspar‐bearing assemblages suggest XCO2&gt;0.9 (at 790°C); and local wollastonite + scapolite + grossular‐bearing zones formed at XCO2 of c. 0.3. Retrograde reaction textures such as scapolite + quartz symplectites after feldspar and calcite and replacement of dolomite + diopside or tremolite+dolomite after calcite+forsterite or calcite+clinohumite are indicative of retrogression under high XCO2 conditions. Calcite preserves late Proterozoic carbon and oxygen isotopic signatures and the marble lacks evidence for extensive retrograde fluid infiltration, while during prograde metamorphism the possible infiltration of aqueous fluids did not produce significant isotopic resetting. Isotopic zonation of calcite and graphite grains was likely produced by localized CO2 fluid infiltration during retrogression. Contrary to the widespread occurrence of humite‐marbles related to retrograde aqueous fluid infiltration, the Ambasamudram humite‐marbles record a prograde‐to‐peak metamorphic humite formation and retrogression under conditions of low XH2O.

Metamorphic devolatilization of subducted oceanic metabasalts: implications for seismicity, arc magmatism and volatile recycling

Subducted oceanic metabasalts are believed to be a primary source of volatiles for arc magmatism and fluid-induced seismicity. From phase equilibria computed for an average oceanic metabasalt we present a model for subduction zone devolatilization for pressures up to 6 GPa (∼180 km). Along high temperature geotherms complete dehydration occurs under forearcs, whereas dehydration does not occur along low temperature geotherms. For intermediate geotherms, major dehydration occurs under subarcs and provides a subjacent H 2O source for arc volcanism. Decarbonation is negligible along cold and intermediate geotherms and limited along high temperature geotherms. Because decarbonation is limited for all subducted carbonate-bearing lithologies, transfer of CO 2 from subducted slabs to arc magmas may be triggered by aqueous fluid infiltration. Metabasalt devolatilization could induce seismicity in forearcs (high temperature geotherms) and subarcs (intermediate geotherms); however, because of the lack of devolatilization, metabasalts would not be a fluid source for seismicity with low temperature geotherms. Along low temperature geotherms, limited devolatilization of subducted oceanic metabasalts and marine sediments in forearcs and subarcs provides a mechanism for return of volatiles to the deeper mantle.

Experimental study of aqueous fluid infiltration into quartzite: implications for the kinetics of fluid redistribution and grain growth driven by interfacial energy reduction

AbstractTo investigate the kinetics of interfacial energy‐driven fluid infiltration, experiments were carried out in a quartzite–water system at 621–925°C and 0.8 GPa. Infiltration couples were made by juxtaposing presynthesized dry quartzite cylinders and fluid reservoirs. The infiltration process was confirmed by the presence of pores at the quartzite grain edges. As predicted from theoretical considerations and previous experiments, wetting fluids such as pure water and NaCl aqueous solution infiltrated into quartzite, whereas nonwetting CO2‐rich fluids did not. Newly precipitated quartz layers at the surfaces of the infiltrated sample proved that infiltration took place by a dissolution–precipitation mechanism.The enhancement of grain growth by fluid infiltration was observed over the entire range of experimental temperatures. The fluid fraction, gauged by the porosity of the run products, increases at the infiltration front and then decreases towards the fluid reservoir to form a high‐porosity zone with a maximum porosity of 2.3–2.9%. As infiltration proceeds, the high‐porosity zone advances like a travelling wave. This porosity wave is probably caused by a grain curvature gradient resulting from preferential grain growth in the infiltrated part of the quartzite, perhaps combined with other factors. The infiltration kinetics were modelled with a steady‐state diffusion model over the high‐porosity zone. The solubility difference between dissolving and precipitating grains was deduced to be 2 × 10−2−3 × 10−1 wt %. The experimentally obtained infiltration rate of aqueous fluid in the steady‐state diffusion regime (2 ± 0.5 × 10−8 m sec−1 at 823°C) is much faster than the estimated metamorphic fluid flux rates, so that interfacial energy‐driven fluid redistribution in quartz‐rich layers could significantly contribute to the fluid flux in high‐grade metamorphism, at least over a short distance.Cathodoluminescence observations of the run products revealed that the grain growth of quartzite in the presence of fluid proceeds extensively, which would promote the chemical equilibration between fluid and rock more effectively than would volume diffusion in quartz crystals.

Clay mineral transformations and weakening mechanisms along the Alpine Fault, New Zealand

AbstractThe formation of clay minerals within active fault zones, which results from the infiltration of aqueous fluids, often leads to important changes in mechanical behaviour. These hydrous phyllosilicates can (1) enhance anisotropy and reduce shear strength, (2) modify porosity and permeability, (3) store or release significant volumes of water, and (4) increase fluid pressures during shearing. The varying interplay between faulting, fluid migration, and hydrous clay mineral transformations along the central Alpine Fault of New Zealand is suggested to constitute an important weakening mechanism within the upper section of this crustal discontinuity. Well-developed zones of cataclasite and compacted clay gouge show successive stages of hydrothermal alteration, driven by the cyclic, coseismic influx of meteoric fluids into exhumed amphibolite-facies rocks that are relatively Mg rich. Three modes of deformation and alteration are recognized within the mylonite-derived clay gouge, which occurred during various stages of the fault’s exhumation history. Following initial strain-hardening and frictional melting during anhydrous cataclastic breakdown of the mylonite fabric, reaction weakening began with formation of Mg-chlorite at sub-greenschist conditions (&lt;320 °C) and continued at lower temperatures (&lt;120 °C) by growth of swelling clays in the matrix. The low permeability and low strength of clay-rich shears are suitable for generating high pore-fluid pressures during faulting. Despite the apparent weakening of the c. 6 km upper segment of the Alpine Fault, the upper crust beneath the Southern Alps is known to be actively releasing elastic strain, with small (&lt;M 5) earthquakes occurring to 12 km depth. We predict that larger events will nucleate at c. 6–12 km along an anhydrous, strain-hardened portion of the fault.

浸透的な流体移動の素過程

A review of the pervasive fluid-migration mechanism is presented with newexperimental results in a quartzite-water system. Microgeometry and connectivity of geological fluids in rocks are governed by the balance of interfacial energy between fluid-crystal and crystalcrystal interfaces; i. e., dihedral angle. Fluid with dihedral angle <-60° can migrate through grain edges as pervasive flow. In rocks having a fluid network, the fluid flow velocity under a fluid pressure gradient is determined by Darcy's law. The minimization of the total interfacial energy drives fluid infiltration and segregation (expulsion). Several experimental and theoretical studies on the interfacial energy-driven fluid migration have been reported, where in the systems considered have been extended from a simple triple junction to polycrystalline rocks with or without two lithologies, bimodal grain size and grain growth. The concepts of MEMF (minimum energy melt fraction), lithological partitioning, grain size effect on fluid fraction, and fluid localization in coarsening rocks, all of whichare required to minimize the total interfacial energy of the system, have been developed. The kinetics of fluid infiltration, segregation and grain growth is derived from the difference in pressure over the interfaces with different curvatures that results in different mineral solubility into the fluids.The interfacial tension, which may be easily overwhelmed with fluid pressure gradient as a direct driving force of Darcy flow, significantly affects Darcy flow by controlling porosity and permeability of the rock. Because the rate of aqueous fluid infiltration into quartzite obtained by the infiltration experiments is much higher than that of Darcy flow velocity under geologically plausible permeability and pressure gradient during metamorphism, interfacial energy-driven fluid infiltration might play a major role in some large-scale fluid/rock systems, although long-term assessment of infiltration rate in natural rocks involves large uncertainty arising from phenomena such as grain faceting, choking of the pore network by accessory minerals and precipitated crystals. More experimental studies to clarify the fluid behavior in geologically realistic systems, as well as direct observation of natural rocks, are needed for better understanding of fluid migration in the Earth's interior.