Relevant bibliographies by topics / Aragonite

Academic literature on the topic 'Aragonite'

Author: Grafiati
Published: 4 June 2021
Last updated: 1 August 2024

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Journal articles on the topic "Aragonite"

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Farfan, Gabriela A., Amy Apprill, Anne Cohen, Thomas M. DeCarlo, Jeffrey E. Post, Rhian G. Waller, and Colleen M. Hansel. "Crystallographic and chemical signatures in coral skeletal aragonite." Coral Reefs 41, no. 1 (November 29, 2021): 19–34. http://dx.doi.org/10.1007/s00338-021-02198-4.

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AbstractCorals nucleate and grow aragonite crystals, organizing them into intricate skeletal structures that ultimately build the world’s coral reefs. Crystallography and chemistry have profound influence on the material properties of these skeletal building blocks, yet gaps remain in our knowledge about coral aragonite on the atomic scale. Across a broad diversity of shallow-water and deep-sea scleractinian corals from vastly different environments, coral aragonites are remarkably similar to one another, confirming that corals exert control on the carbonate chemistry of the calcifying space relative to the surrounding seawater. Nuances in coral aragonite structures relate most closely to trace element chemistry and aragonite saturation state, suggesting the primary controls on aragonite structure are ionic strength and trace element chemistry, with growth rate playing a secondary role. We also show how coral aragonites are crystallographically indistinguishable from synthetic abiogenic aragonite analogs precipitated from seawater under conditions mimicking coral calcifying fluid. In contrast, coral aragonites are distinct from geologically formed aragonites, a synthetic aragonite precipitated from a freshwater solution, and mollusk aragonites. Crystallographic signatures have future applications in understanding the material properties of coral aragonite and predicting the persistence of coral reefs in a rapidly changing ocean.
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Vinn, Olev. "The Role of Aragonite in Producing the Microstructural Diversity of Serpulid Skeletons." Minerals 11, no. 12 (December 18, 2021): 1435. http://dx.doi.org/10.3390/min11121435.

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Aragonite plays an important role in the biomineralization of serpulid polychaetes. Aragonitic structures are present in a wide range of serpulid species, but they mostly belong to one clade. Aragonitic structures are present in a wide range of marine environments, including the deep ocean. Aragonitic tube microstructures were studied using a scanning electron microscope. X-ray powder diffraction was used to identify the aragonite. Aragonite is used to build five different types of microstructures in serpulid tubes. The most common aragonitic irregularly oriented prismatic structure (AIOP) is also, evolutionarily, the most primitive. Some aragonitic microstructures, such as the spherulitic prismatic (SPHP) structure, have likely evolved from the AIOP structure. Aragonitic microstructures in serpulids are far less numerous than calcitic microstructures, and they lack the complexity of advanced calcitic microstructures. The reason why aragonitic microstructures have remained less evolvable than calcitic microstructures is currently unknown, considering their fit with the current aragonite sea conditions (Paleogene–recent).
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Rostovtseva, Yuliana. "Upper Miocene aragonite sediments of the Eastern Paratethys (Zheleznyi Rog section): Whiting events or not?" Annales g?ologiques de la Peninsule balkanique, no. 00 (2024): 6. http://dx.doi.org/10.2298/gabp240218006r.

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The upper Sarmatian and lower Maeotian unlithified aragonite sediments of the Zheleznyi Rog section (Taman Peninsula, Eastern Paratethys, Russia) were investigated by field observations and laboratory methods, including scanning electron microscopy, X-ray diffraction and isotope analyses. Aragonite sediments occur at separate intervals of the studied section, forming thin (millimeter-sized) interlayers with clays. These carbonate sediments consist almost entirely of crystals (individuals and twins) and aggregates of aragonite, ranging in size from 5 to 23 ?m. It is assumed that the isotopic composition (?13C = 5.7 and 5.3?, ?18O = -2.4 and -2.8 ? for upper Sarmatian and lower Maeotian aragonites, respectively) reflects the sedimentation conditions, chara cterized by reduced basin salinity, increased surface water bioproductivity, and periods of aridization. Abiotic precipitation of these aragonites most likely occurred due to the action of triggering mechanisms, which could include planktonic algae blooms (e.g. diatoms). The obtained results do not contradict the hypothesis that the studied aragonites may be considered as sediments of whiting phenomenon.
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Dean, Christopher D., Peter A. Allison, Gary J. Hampson, and Jon Hill. "Aragonite bias exhibits systematic spatial variation in the Late Cretaceous Western Interior Seaway, North America." Paleobiology 45, no. 4 (September 2019): 571–97. http://dx.doi.org/10.1017/pab.2019.33.

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AbstractPreferential dissolution of the biogenic carbonate polymorph aragonite promotes preservational bias in shelly marine faunas. While field studies have documented the impact of preferential aragonite dissolution on fossil molluscan diversity, its impact on regional and global biodiversity metrics is debated. Epicontinental seas are especially prone to conditions that both promote and inhibit preferential dissolution, which may result in spatially extensive zones with variable preservation. Here we present a multifaceted evaluation of aragonite dissolution within the Late Cretaceous Western Interior Seaway of North America. Occurrence data of mollusks from two time intervals (Cenomanian/Turonian boundary, early Campanian) are plotted on new high-resolution paleogeographies to assess aragonite preservation within the seaway. Fossil occurrences, diversity estimates, and sampling probabilities for calcitic and aragonitic fauna were compared in zones defined by depth and distance from the seaway margins. Apparent range sizes, which could be influenced by differential preservation potential of aragonite between separate localities, were also compared. Our results are consistent with exacerbated aragonite dissolution within specific depth zones for both time slices, with aragonitic bivalves additionally showing a statistically significant decrease in range size compared with calcitic fauna within carbonate-dominated Cenomanian–Turonian strata. However, we are unable to conclusively show that aragonite dissolution impacted diversity estimates. Therefore, while aragonite dissolution is likely to have affected the preservation of fauna in specific localities, time averaging and instantaneous preservation events preserve regional biodiversity. Our results suggest that the spatial expression of taphonomic biases should be an important consideration for paleontologists working on paleobiogeographic problems.
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Hoerl, Sebastian, Erika Griesshaber, Antonio G. Checa, and Wolfgang W. Schmahl. "The Biological Crystals in Chamid Bivalve Shells: Diversity in Morphology and Crystal Arrangement Pattern." Crystals 14, no. 7 (July 15, 2024): 649. http://dx.doi.org/10.3390/cryst14070649.

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Chamid bivalves are marine organisms that live in high-energy environments and are cemented to hard substrates. To avoid shell damage, the organisms form thick, densely ornamented shells. Shell material consists of aragonite, and the ornamentation may be either aragonitic or calcitic. The latter can be developed as scaly spines, rows of blades, or comarginal, radial arched lamellae. We investigated biological crystal morphology and mode of assembly of Chama arcana and Chama gryphoides shells. Structural characteristics were obtained from electron backscatter diffraction (EBSD) measurements, complemented with laser confocal and BSE imaging. We found a wide range of crystal morphologies and sizes, ranging from irregularly shaped calcite and/or aragonite prisms to tiny and thin aragonite laths. We observed four different modes of crystal assembly patterns: 1. strongly interlocked dendritic calcite units forming the ornamentation blades; 2. aragonite laths arranged to lamellae forming the outer shell layer, the layer adjacent to the calcite; 3. aragonite laths arranged into blocks comprising inner shell layers or aragonitic ornamentations; and 4. shell portions consisting of aragonite prisms, structured in size and crystal orientation, at muscle attachment sites. These four different types of crystal arrangements were observed for the shells of the investigated chamid species; however, they had slightly different strengths of structuring and slight variations in crystal organisation. Additionally, we observed unique microstructural features in Chama shells: We report ornamentation crystals resembling idiomorphic calcite and novel, twinned entities found at the changeover between the aragonitic layers. We highlight and discuss these differences and anomalies in this contribution.
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Nohl, Theresa, Jannick Wetterich, Nicholas Fobbe, and Axel Munnecke. "Lithological dependence of aragonite preservation in monospecific gastropod deposits of the Miocene Mainz Basin: Implications for the (dia-)genesis of limestone–marl alternations." Journal of Sedimentary Research 90, no. 11 (November 30, 2020): 1500–1509. http://dx.doi.org/10.2110/jsr.2020.057.

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ABSTRACTThe origin of limestone–marl alternations (LMA) and their diagenesis is still lively debated. The most disputed question is whether original variations in sediment input control the differentiation of the precursor sediment into limestone and marl, or if a LMA can form without compositional differences in the precursor sediment. The Miocene brackish-water deposits (Rüssingen Formation) from the Mainz–Weisenau quarry in central Germany offer the opportunity to tackle this question. They are developed as a monospecific alternation of planar beds of moderately and poorly lithified sands of aragonitic Hydrobia snails, corresponding to “limestones” and “marls” in LMA, respectively. XRD analyses and the monospecific composition reveal only minor to no changes in sedimentary input and allow comparison of the preservation of Hydrobia in both lithologies. The differential preservation of the aragonitic fossils in lithified and less lithified layers is documented in thin-sections. CaCO3 contents are high throughout the measured section. However, XRD analyses revealed high amounts of aragonite and low amounts of calcite in less lithified beds, and the opposite in lithified beds in which calcite is the main mineral phase. Mg-calcite is abundant in both lithologies. Although the less lithified beds have experienced significant loss of aragonite by dissolution, they still mainly contain aragonite since the precursor sediment contained only aragonitic shells and Mg-calcite crusts. The relative amount of aragonite is higher than in the more lithified beds because the lithified beds imported the dissolved aragonite, which precipitated as calcite cements. This shifted the aragonite–calcite ratio to higher values in the less lithified beds than in the more lithified beds, although it is counterintuitive at first sight. This is supported by thin-section analyses and point counting, revealing moderate to good preservation of Hydrobia or their replacement by calcite spar in lithified beds, but intense dissolution of aragonite in less lithified beds. The aragonite–calcite ratio and the differential preservation of Hydrobia fit the model of differential diagenesis in “classical” LMAs, which assumes early diagenetic aragonite dissolution in marls and reprecipitation as calcite cement in limestones. It is concluded that the studied succession—although an endmember of LMA—was differentiated into lithified and unlithified beds by incomplete differential diagenesis while minor primary differences are not reflected in the change in lithology. The results suggest that the differentiation of a homogeneous precursor sediment into a LMA is possible and caution should be exercised using lithological change or proxies which are potentially altered by CaCO3 redistribution for cyclostratigraphic analyses.
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Forjanes, Pablo, María Simonet Roda, Martina Greiner, Erika Griesshaber, Nelson A. Lagos, Sabino Veintemillas-Verdaguer, José Manuel Astilleros, Lurdes Fernández-Díaz, and Wolfgang W. Schmahl. "Experimental burial diagenesis of aragonitic biocarbonates: from organic matter loss to abiogenic calcite formation." Biogeosciences 19, no. 16 (August 22, 2022): 3791–823. http://dx.doi.org/10.5194/bg-19-3791-2022.

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Abstract. Carbonate biological hard tissues are valuable archives of environmental information. However, this information can be blurred or even completely lost as hard tissues undergo diagenetic alteration. This is more likely to occur in aragonitic skeletons because bioaragonite often transforms into calcite during diagenesis. For reliably using aragonitic skeletons as geochemical proxies, it is necessary to understand in depth the diagenetic alteration processes that they undergo. Several works have recently investigated the hydrothermal alteration of aragonitic hard tissues during short-term experiments at high temperatures (T > 160 ∘C). In this study, we conduct long-term (4 and 6 months) hydrothermal alteration experiments at 80 ∘C using burial-like fluids. We document and evaluate the changes undergone by the outer and inner layers of the shell of the bivalve Arctica islandica, the prismatic and nacreous layers of the hard tissue of the gastropod Haliotis ovina, and the skeleton of the coral Porites sp. combining a variety of analytical tools (X-ray diffraction, thermogravimetry analysis, laser confocal microscopy, scanning electron microscopy, electron backscatter diffraction and atomic force microscopy). We demonstrate that this approach is the most adequate to trace subtle, diagenetic-alteration-related changes in aragonitic biocarbonate structural hard materials. Furthermore, we unveil that the diagenetic alteration of aragonitic biological hard tissues is a complex multi-step process where major changes occur even at the low temperature used in this study, well before any aragonite into calcite transformation takes place. Alteration starts with biopolymer decomposition and concomitant generation of secondary porosity. These processes are followed by abiogenic aragonite precipitation that partially or totally obliterates the secondary porosity. Only subsequently does the transformation of the aragonite into calcite occur. The kinetics of the alteration process is highly dependent on primary microstructural features of the aragonitic biomineral. While the skeleton of Porites sp. remains virtually unaltered for the entire duration of the conducted experiments, Haliotis ovina nacre undergoes extensive abiogenic aragonite precipitation. The outer and inner shell layers of Arctica islandica are significantly affected by aragonite transformation into calcite. This transformation is extensive for the prismatic shell layer of Haliotis ovina. Our results suggest that the majority of aragonitic fossil archives are overprinted, even those free of clear diagenetic alteration signs. This finding may have major implications for the use of these archives as geochemical proxies.
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Vinn, Olev. "Biomineralization in Polychaete Annelids: A Review." Minerals 11, no. 10 (October 19, 2021): 1151. http://dx.doi.org/10.3390/min11101151.

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Polychaete annelids are a very important group of calcifiers in the modern oceans. They can produce calcite, aragonite, and amorphous phosphates. Serpulids possess very diverse tube ultra-structures, several unique to them. Serpulid tubes are composed of aragonite or calcite or a mixture of both polymorphs. The serpulid tubes with complex oriented microstructures, such as lamello fibrillar, are exclusively calcitic, whereas tubes with prismatic structures can be composed either of calcite or aragonite. In serpulids, the calcareous opercula also have complex microstructures. Evolutionarily, calcitic serpulid taxa belong to one clade and the aragonitic taxa belong to another clade. Modern ocean acidification affects serpulid biomineralization. Serpulids are capable of biomineralization in extreme environments, such as the deepest part (hadal zone) of the ocean. The tubes of calcareous sabellids are aragonitic and have two layers, the inner irregular spherulitic prismatic layer and the outer spherulitic layer. The tube wall of cirratulids is composed of aragonitic lamellae with a spherulitic prismatic structure. In some other polychaetes, biominerals are formed in different parts of the animal body, such as chaetae or body shields, or occur within the body as granule-shaped or rod-shaped inclusions.
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He, Jianhan, and Ulrich Bismayer. "Polarized mapping Raman spectroscopy: identification of particle orientation in biominerals." Zeitschrift für Kristallographie - Crystalline Materials 234, no. 6 (May 27, 2019): 395–400. http://dx.doi.org/10.1515/zkri-2019-0004.

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Abstract The identification of the texture of biominerals and the particle orientation in the bivalve shells of Anodonta cygnea was performed using polarized Raman spectroscopy mapping measurements. A single crystal of aragonite served as a reference to disclose orientational information on the mesoscopic scale. The relative intensities of different Raman modes combined with the determination of depolarization ratio of the Ag Raman mode at 1087 cm−1 of an aragonite single crystal was used to indicate the angular variation of aragonite crystallites in biominerals. The imaging technique shows that the a- and b-axis of aragonite crystallites in both, nacreous and prismatic layers do not only have one orientation but they are organized in a domain-type arrangement. The angular divergence in the prismatic layer of the shells is larger and hence, the crystallites in the nacreous layer have a higher degree of co-orientation. Results provide relevant textural information about aragonitic shells and indicate a sensitive technique to evaluate the crystal orientation in biominerals.
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Katti, Kalpana S., Maoxu Qian, Daniel W. Frech, and Mehmet Sarikaya. "Low-loss Electron Energy-loss Spectroscopy and Dielectric Function of Biological and Geological Polymorphs of CaCO3." Microscopy and Microanalysis 5, no. 5 (September 1999): 358–64. http://dx.doi.org/10.1017/s1431927699000197.

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Previous work on microstructural characterization has shown variations in terms of defects and organization of nanostructures in the two polymorphs of calcium carbonate, calcite, and aragonite in mollusc shells. Large variations in mechanical properties are observed between these sections which have been attributed to variations in composite microstructure as well as intrinsic properties of the inorganic phases. Here we present local low-loss electron energy-loss spectroscopic (EELS) study of calcitic and aragonitic regions of abalone shell that were compared to geological (single-crystal) counterpart polymorphs to reveal intrinsic differences that could be related to organismal effects in biomineralization. In both sets of samples, local dielectric function is computed using Kramer-Kronig analysis. The electronic structures of biogenic and geological calcitic materials are not significantly different. On the other hand, electronic structure of biogenic aragonite is remarkably different from that of geological aragonite. This difference is attributed to the increased contribution from single electron excitations in biogenic aragonite as compared to that of geological aragonite. Implications of these changes are discussed in the context of macromolecular involvement in the making of the microstructures and properties in biogenic phases.
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Dissertations / Theses on the topic "Aragonite"

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Beckett, David. "Aragonite in Jurassic ooids : distribution and significance." Thesis, University of Reading, 1991. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.306458.

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Croley, Allison L. "THE ARAGONITE TO CALCITE TRANSFORMATION: A LABORATORY STUDY." Oxford, Ohio : Miami University, 2002. http://rave.ohiolink.edu/etdc/view?acc%5Fnum=miami1038431567.

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Thesis (M.S.)--Miami University, Dept. of Geology, 2002.
Title from first page of PDF document. Document formatted into pages; contains vi, 78 p. : ill. Includes bibliographical references (p. 37-40).
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Gérard, Yves. "Étude expérimentale des interactions entre déformation et transformation de phase : exemple de la transition calcite-aragonite /." Rennes : Centre armoricain d'étude structurale des socles, 1987. http://catalogue.bnf.fr/ark:/12148/cb349781275.

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Brown, Sarah Jane. "Controls on the trace metal chemistry of foraminiferal calcite and aragonite." Thesis, University of Cambridge, 1997. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.627090.

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Gérard, Yves. "Etude experimentale des interactions entre deformation et transformation de phase : exemple de la transition calcite-aragonite." Rennes 1, 1987. http://www.theses.fr/1987REN10146.

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Zadi, Daza Louis. "Mécanismes physico-chimiques impliqués dans la formation et l’évolution à l’abandon d’un matériau sédimentaire innovant généré en milieu marin par polarisation cathodique." Electronic Thesis or Diss., La Rochelle, 2022. http://www.theses.fr/2022LAROS028.

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Ce travail de thèse porte sur un matériau (le Geocorail) formé par polarisation cathodique d’un treillis en acier disposé au sein d’un milieu sédimentaire marin. L’application de ce procédé est dédiée au renforcement des ouvrages côtiers dans la lutte contre le recul du trait de côte. L’objectif de cette étude est d’apporter des réponses relatives à l’influence des paramètres du procédé sur les propriétés physico-chimiques de ce matériau ainsi que l’évolution de celui-ci en condition d’abandon, c’est-à-dire lorsque la polarisation est arrêtée. Cette étude a été réalisée à travers une démarche expérimentale couplée avec des modèles numériques. Ces travaux ont été réalisés sur un matériau modèle formé en laboratoire et ont permis de mettre en évidence l’anisotropie de diffusion au sein de ce matériau dont l’épaisseur, la porosité et la masse volumique sont essentiellement contrôlées par la densité de courant et la durée de la polarisation. Ces deux derniers paramètres favorisent la formation de liant, constitué de brucite (Mg(OH)2) et d’aragonite (CaCO3), servant à l’agglomération du sédiment en place. La géométrie de ce sédiment est en outre un facteur primordial pour l’optimisation des propriétés du matériau. En ce qui concerne sa stabilité chimique en l’absence de polarisation, les analyses expérimentales et les modèles numériques ont révélé que l’aragonite se substitue à la brucite avec un rendement massique relativement faible, probablement lié à la forte diffusivité des matériaux analysés. La faible variation de la porosité et de la masse volumique (inférieur à 5% en 18 mois) rassure cependant de la stabilité du Geocorail dont les propriétés pourraient même s’améliorer avec le temps. Enfin, des modèles numériques de croissance et d’évolution de ce matériau à l’abandon ont été élaborés. Des voies d’amélioration ont également été proposées pour une meilleure prédiction de ces propriétés, voire la prédiction des propriétés mécaniques
This PhD work focused on the study of a material (Geocorail) formed by cathodic polarization applied in a marine sedimentary environment and used for the reinforcement of coastal structures in the fight against coastline recession. The objective of this study is to provide answers relative to the influence of the process parameters on the physico-chemical properties of this material as well as the evolution of the material under abandonment conditions, i.e. when the polarization is stopped. This was achieved through an experimental approach coupled with numerical models. This work was carried out on a laboratory material and its diffusion anisotropy within this material, the thickness, porosity and density of which are essentially controlled by the applied current density and the polarization time. These two parameters promote the formation of a binder, consisting of brucite (Mg(OH)2) and aragonite (CaCO3), which serves to agglomerate the sediments in place. The geometry of this sediment is also a key factor in optimizing the properties of this material. With regard to its chemical stability in the absence of polarization, experimental analyses and numerical models revealed that brucite substitutes for aragonite with a relatively low mass yield, probably linked to the high diffusivity of the studied materials. The small variation in porosity and density (less than 5% in 18 months) however ensures the stability of the Geocorail, whose properties could even improve with time. Finally, numerical models of the growth and evolution in abandon condition were developed. Some ways of improvement were also proposed for a better prediction of these properties, and even for the mechanical characterization using numerical methods
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Rowling, Jill. "Cave Aragonites of New South Wales." Thesis, The University of Sydney, 2004. http://hdl.handle.net/2123/694.

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Abstract Aragonite is a minor secondary mineral in many limestone caves throughout the world. It has been claimed that it is the second-most common cave mineral after calcite (Hill & Forti 1997). Aragonite occurs as a secondary mineral in the vadose zone of some caves in New South Wales. Aragonite is unstable in fresh water and usually reverts to calcite, but it is actively depositing in some NSW caves. A review of current literature on the cave aragonite problem showed that chemical inhibitors to calcite deposition assist in the precipitation of calcium carbonate as aragonite instead of calcite. Chemical inhibitors work by physically blocking the positions on the calcite crystal lattice which would have otherwise allowed calcite to develop into a larger crystal. Often an inhibitor for calcite has no effect on the aragonite crystal lattice, thus aragonite may deposit where calcite deposition is inhibited. Another association with aragonite in some NSW caves appears to be high evaporation rates allowing calcite, aragonite and vaterite to deposit. Vaterite is another unstable polymorph of calcium carbonate, which reverts to aragonite and calcite over time. Vaterite, aragonite and calcite were found together in cave sediments in areas with low humidity in Wollondilly Cave, Wombeyan. Several factors were found to be associated with the deposition of aragonite instead of calcite speleothems in NSW caves. They included the presence of ferroan dolomite, calcite-inhibitors (in particular ions of magnesium, manganese, phosphate, sulfate and heavy metals), and both air movement and humidity. Aragonite deposits in several NSW caves were examined to determine whether the material is or is not aragonite. Substrates to the aragonite were examined, as was the nature of the bedrock. The work concentrated on Contact Cave and Wiburds Lake Cave at Jenolan, Sigma Cave, Wollondilly Cave and Cow Pit at Wombeyan and Piano Cave and Deep Hole (Cave) at Walli. Comparisons are made with other caves. The study sites are all located in Palaeozoic rocks within the Lachlan Fold Belt tectonic region. Two of the sites, Jenolan and Wombeyan, are close to the western edge of the Sydney Basin. The third site, Walli, is close to a warm spring. The physical, climatic, chemical and mineralogical influences on calcium carbonate deposition in the caves were investigated. Where cave maps were unavailable, they were prepared on site as part of the study. %At Jenolan Caves, Contact Cave and Wiburds Lake Cave were examined in detail, %and other sites were compared with these. Contact Cave is located near the eastern boundary of the Late Silurian Jenolan Caves Limestone, in an area of steeply bedded and partially dolomitised limestone very close to its eastern boundary with the Jenolan volcanics. Aragonite in Contact Cave is precipitated on the ceiling as anthodites, helictites and coatings. The substrate for the aragonite is porous, altered, dolomitised limestone which is wedged apart by aragonite crystals. Aragonite deposition in Contact Cave is associated with a concentration of calcite-inhibiting ions, mainly minerals containing ions of magnesium, manganese and to a lesser extent, phosphates. Aragonite, dolomite and rhodochrosite are being actively deposited where these minerals are present. Calcite is being deposited where minerals containing magnesium ions are not present. The inhibitors appear to be mobilised by fresh water entering the cave as seepage along the steep bedding and jointing. During winter, cold dry air pooling in the lower part of the cave may concentrate minerals by evaporation and is most likely associated with the ``popcorn line'' seen in the cave. Wiburds Lake Cave is located near the western boundary of the Jenolan Caves Limestone, very close to its faulted western boundary with Ordovician cherts. Aragonite at Wiburds Lake Cave is associated with weathered pyritic dolomitised limestone, an altered, dolomitised mafic dyke in a fault shear zone, and also with bat guano minerals. Aragonite speleothems include a spathite, cavity fills, vughs, surface coatings and anthodites. Calcite occurs in small quantities at the aragonite sites. Calcite-inhibitors associated with aragonite include ions of magnesium, manganese and sulfate. Phosphate is significant in some areas. Low humidity is significant in two areas. Other sites briefly examined at Jenolan include Glass Cave, Mammoth Cave, Spider Cave and the show caves. Aragonite in Glass Cave may be associated with both weathering of dolomitised limestone (resulting in anthodites) and with bat guano (resulting in small cryptic forms). Aragonite in the show caves, and possibly in Mammoth and Spider Cave is associated with weathering of pyritic dolomitised limestone. Wombeyan Caves are developed in saccharoidal marble, metamorphosed Silurian Wombeyan Caves Limestone. Three sites were examined in detail at Wombeyan Caves: Sigma Cave, Wollondilly Cave and Cow Pit (a steep sided doline with a dark zone). Sigma Cave is close to the south east boundary of the Wombeyan marble, close to its unconformable boundary with effusive hypersthene porphyry and intrusive gabbro, and contains some unmarmorised limestone. Aragonite occurs mainly in a canyon at the southern extremity of the cave and in some other sites. In Sigma Cave, aragonite deposition is mainly associated with minerals containing calcite-inhibitors, as well as some air movement in the cave. Calcite-inhibitors at Sigma Cave include ions of magnesium, manganese, sulfate and phosphate (possibly bat origin), partly from bedrock veins and partly from breakdown of minerals in sediments sourced from mafic igneous rocks. Substrates to aragonite speleothems include corroded speleothem, bedrock, ochres, mud and clastics. There is air movement at times in the canyon, it has higher levels of CO2 than other parts of the cave and humidity is high. Air movement may assist in the rapid exchange of CO2 at speleothem surfaces. Wollondilly Cave is located in the eastern part of the Wombeyan marble. At Wollondilly Cave, anthodites and helictites were seen in an inaccessible area of the cave. Paramorphs of calcite after aragonite were found at Jacobs Ladder and the Pantheon. Aragonite at Star Chamber is associated with huntite and hydromagnesite. In The Loft, speleothem corrosion is characteristic of bat guano deposits. Aragonite, vaterite and calcite were detected in surface coatings in this area. Air movement between the two entrances of this cave has a drying effect which may serve to concentrate minerals by evaporation in some parts of the cave. The presence of vaterite and aragonite in fluffy coatings infers that vaterite may be inverting to aragonite. Calcite-inhibitors in the sediments include ions of phosphate, sulphate, magnesium and manganese. Cave sediment includes material sourced from detrital mafic rocks. Cow Pit is located near Wollondilly Cave, and cave W43 is located near the northern boundary of the Wombeyan marble. At Cow Pit, paramorphs of calcite after aragonite occur in the walls as spheroids with minor huntite. Aragonite is a minor mineral in white wall coatings and red phosphatic sediments with minor hydromagnesite and huntite. At cave W43, aragonite was detected in the base of a coralloid speleothem. Paramorphs of calcite after aragonite were observed in the same speleothem. Dolomite in the bedrock may be a source of magnesium-rich minerals at cave W43. Walli Caves are developed in the massive Belubula Limestone of the Ordovician Cliefden Caves Limestone Subgroup (Barrajin Group). At the caves, the limestone is steeply bedded and contains chert nodules with dolomite inclusions. Gypsum and barite occur in veins in the limestone. At Walli Caves, Piano Cave and Deep Hole (Deep Cave) were examined for aragonite. Gypsum occurs both as a surface coating and as fine selenite needles on chert nodules in areas with low humidity in the caves. Aragonite at Walli caves was associated with vein minerals and coatings containing calcite-inhibitors and, in some areas, low humidity. Calcite-inhibitors include sulfate (mostly as gypsum), magnesium, manganese and barium. Other caves which contain aragonite are mentioned. Although these were not major study sites, sufficient information is available on them to make a preliminary assessment as to why they may contain aragonite. These other caves include Flying Fortress Cave and the B4-5 Extension at Bungonia near Goulburn, and Wyanbene Cave south of Braidwood. Aragonite deposition at Bungonia has some similarities with that at Jenolan in that dolomitisation of the bedrock has occurred, and the bedding or jointing is steep allowing seepage of water into the cave, with possible oxidation of pyrite. Aragonite is also associated with a mafic dyke. Wyanbene cave features some bedrock dolomitisation, and also features low grade ore bodies which include several known calcite-inhibitors. Aragonite appears to be associated with both features. Finally, brief notes are made of aragonite-like speleothems at Colong Caves (between Jenolan and Wombeyan), a cave at Jaunter (west of Jenolan) and Wellington (240\,km NW of Sydney).
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Rowling, Jill. "Cave Aragonites of New South Wales." University of Sydney. Geosciences, 2004. http://hdl.handle.net/2123/694.

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Abstract Aragonite is a minor secondary mineral in many limestone caves throughout the world. It has been claimed that it is the second-most common cave mineral after calcite (Hill & Forti 1997). Aragonite occurs as a secondary mineral in the vadose zone of some caves in New South Wales. Aragonite is unstable in fresh water and usually reverts to calcite, but it is actively depositing in some NSW caves. A review of current literature on the cave aragonite problem showed that chemical inhibitors to calcite deposition assist in the precipitation of calcium carbonate as aragonite instead of calcite. Chemical inhibitors work by physically blocking the positions on the calcite crystal lattice which would have otherwise allowed calcite to develop into a larger crystal. Often an inhibitor for calcite has no effect on the aragonite crystal lattice, thus aragonite may deposit where calcite deposition is inhibited. Another association with aragonite in some NSW caves appears to be high evaporation rates allowing calcite, aragonite and vaterite to deposit. Vaterite is another unstable polymorph of calcium carbonate, which reverts to aragonite and calcite over time. Vaterite, aragonite and calcite were found together in cave sediments in areas with low humidity in Wollondilly Cave, Wombeyan. Several factors were found to be associated with the deposition of aragonite instead of calcite speleothems in NSW caves. They included the presence of ferroan dolomite, calcite-inhibitors (in particular ions of magnesium, manganese, phosphate, sulfate and heavy metals), and both air movement and humidity. Aragonite deposits in several NSW caves were examined to determine whether the material is or is not aragonite. Substrates to the aragonite were examined, as was the nature of the bedrock. The work concentrated on Contact Cave and Wiburds Lake Cave at Jenolan, Sigma Cave, Wollondilly Cave and Cow Pit at Wombeyan and Piano Cave and Deep Hole (Cave) at Walli. Comparisons are made with other caves. The study sites are all located in Palaeozoic rocks within the Lachlan Fold Belt tectonic region. Two of the sites, Jenolan and Wombeyan, are close to the western edge of the Sydney Basin. The third site, Walli, is close to a warm spring. The physical, climatic, chemical and mineralogical influences on calcium carbonate deposition in the caves were investigated. Where cave maps were unavailable, they were prepared on site as part of the study. %At Jenolan Caves, Contact Cave and Wiburds Lake Cave were examined in detail, %and other sites were compared with these. Contact Cave is located near the eastern boundary of the Late Silurian Jenolan Caves Limestone, in an area of steeply bedded and partially dolomitised limestone very close to its eastern boundary with the Jenolan volcanics. Aragonite in Contact Cave is precipitated on the ceiling as anthodites, helictites and coatings. The substrate for the aragonite is porous, altered, dolomitised limestone which is wedged apart by aragonite crystals. Aragonite deposition in Contact Cave is associated with a concentration of calcite-inhibiting ions, mainly minerals containing ions of magnesium, manganese and to a lesser extent, phosphates. Aragonite, dolomite and rhodochrosite are being actively deposited where these minerals are present. Calcite is being deposited where minerals containing magnesium ions are not present. The inhibitors appear to be mobilised by fresh water entering the cave as seepage along the steep bedding and jointing. During winter, cold dry air pooling in the lower part of the cave may concentrate minerals by evaporation and is most likely associated with the ``popcorn line'' seen in the cave. Wiburds Lake Cave is located near the western boundary of the Jenolan Caves Limestone, very close to its faulted western boundary with Ordovician cherts. Aragonite at Wiburds Lake Cave is associated with weathered pyritic dolomitised limestone, an altered, dolomitised mafic dyke in a fault shear zone, and also with bat guano minerals. Aragonite speleothems include a spathite, cavity fills, vughs, surface coatings and anthodites. Calcite occurs in small quantities at the aragonite sites. Calcite-inhibitors associated with aragonite include ions of magnesium, manganese and sulfate. Phosphate is significant in some areas. Low humidity is significant in two areas. Other sites briefly examined at Jenolan include Glass Cave, Mammoth Cave, Spider Cave and the show caves. Aragonite in Glass Cave may be associated with both weathering of dolomitised limestone (resulting in anthodites) and with bat guano (resulting in small cryptic forms). Aragonite in the show caves, and possibly in Mammoth and Spider Cave is associated with weathering of pyritic dolomitised limestone. Wombeyan Caves are developed in saccharoidal marble, metamorphosed Silurian Wombeyan Caves Limestone. Three sites were examined in detail at Wombeyan Caves: Sigma Cave, Wollondilly Cave and Cow Pit (a steep sided doline with a dark zone). Sigma Cave is close to the south east boundary of the Wombeyan marble, close to its unconformable boundary with effusive hypersthene porphyry and intrusive gabbro, and contains some unmarmorised limestone. Aragonite occurs mainly in a canyon at the southern extremity of the cave and in some other sites. In Sigma Cave, aragonite deposition is mainly associated with minerals containing calcite-inhibitors, as well as some air movement in the cave. Calcite-inhibitors at Sigma Cave include ions of magnesium, manganese, sulfate and phosphate (possibly bat origin), partly from bedrock veins and partly from breakdown of minerals in sediments sourced from mafic igneous rocks. Substrates to aragonite speleothems include corroded speleothem, bedrock, ochres, mud and clastics. There is air movement at times in the canyon, it has higher levels of CO2 than other parts of the cave and humidity is high. Air movement may assist in the rapid exchange of CO2 at speleothem surfaces. Wollondilly Cave is located in the eastern part of the Wombeyan marble. At Wollondilly Cave, anthodites and helictites were seen in an inaccessible area of the cave. Paramorphs of calcite after aragonite were found at Jacobs Ladder and the Pantheon. Aragonite at Star Chamber is associated with huntite and hydromagnesite. In The Loft, speleothem corrosion is characteristic of bat guano deposits. Aragonite, vaterite and calcite were detected in surface coatings in this area. Air movement between the two entrances of this cave has a drying effect which may serve to concentrate minerals by evaporation in some parts of the cave. The presence of vaterite and aragonite in fluffy coatings infers that vaterite may be inverting to aragonite. Calcite-inhibitors in the sediments include ions of phosphate, sulphate, magnesium and manganese. Cave sediment includes material sourced from detrital mafic rocks. Cow Pit is located near Wollondilly Cave, and cave W43 is located near the northern boundary of the Wombeyan marble. At Cow Pit, paramorphs of calcite after aragonite occur in the walls as spheroids with minor huntite. Aragonite is a minor mineral in white wall coatings and red phosphatic sediments with minor hydromagnesite and huntite. At cave W43, aragonite was detected in the base of a coralloid speleothem. Paramorphs of calcite after aragonite were observed in the same speleothem. Dolomite in the bedrock may be a source of magnesium-rich minerals at cave W43. Walli Caves are developed in the massive Belubula Limestone of the Ordovician Cliefden Caves Limestone Subgroup (Barrajin Group). At the caves, the limestone is steeply bedded and contains chert nodules with dolomite inclusions. Gypsum and barite occur in veins in the limestone. At Walli Caves, Piano Cave and Deep Hole (Deep Cave) were examined for aragonite. Gypsum occurs both as a surface coating and as fine selenite needles on chert nodules in areas with low humidity in the caves. Aragonite at Walli caves was associated with vein minerals and coatings containing calcite-inhibitors and, in some areas, low humidity. Calcite-inhibitors include sulfate (mostly as gypsum), magnesium, manganese and barium. Other caves which contain aragonite are mentioned. Although these were not major study sites, sufficient information is available on them to make a preliminary assessment as to why they may contain aragonite. These other caves include Flying Fortress Cave and the B4-5 Extension at Bungonia near Goulburn, and Wyanbene Cave south of Braidwood. Aragonite deposition at Bungonia has some similarities with that at Jenolan in that dolomitisation of the bedrock has occurred, and the bedding or jointing is steep allowing seepage of water into the cave, with possible oxidation of pyrite. Aragonite is also associated with a mafic dyke. Wyanbene cave features some bedrock dolomitisation, and also features low grade ore bodies which include several known calcite-inhibitors. Aragonite appears to be associated with both features. Finally, brief notes are made of aragonite-like speleothems at Colong Caves (between Jenolan and Wombeyan), a cave at Jaunter (west of Jenolan) and Wellington (240\,km NW of Sydney).
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Miller, Caroline E. "Environmental influences on synthetic and biogenic calcium carbonate in aragonite-calcite sea conditions." Thesis, University of Glasgow, 2018. http://theses.gla.ac.uk/8665/.

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Ocean chemistry has oscillated throughout Earth history to favour the dominant non-biogenic polymorph of calcium carbonate (CaCO3) to be either calcite or aragonite (Sandberg, 1983). Throughout the Phanerozoic these oscillations have occurred to facilitate aragonite-dominant conditions three times and calcite-dominant conditions twice. These aragonite-calcite seas conditions have previously been viewed as a global phenomenon where conditions fluctuate over time, but not in space, and represent the main environmental context in which the evolution of CaCO3 biomineralisation has occurred (Stanley and Hardie, 1998). CaCO3 is one of the most widely distributed minerals in the marine environment, occurring throughout geological history, both biogenically and non-biogenically (Lowenstam and Weiner, 1989). Marine non-biogenic precipitates are commonly found as carbonate ooids, sedimentary cements and muds (Nichols, 2009). Biogenic CaCO3 is formed via biomineralisation in calcifying organisms (Lowenstam and Weiner, 1989; Allemand et al., 2004), and is much more abundant than the non-biogenic forms. Although CaCO3 is abundant, it only accounts for a small proportion of the global carbon budget. Biogenic CaCO3 is representative of a larger proportion of the global carbon budget than non-biogenically formed CaCO3 (Berelson et al., 2007). The main driving force controlling the precipitation of CaCO3 polymorphs is the Mg:Ca molar ratio of seawater (Morse et al., 2007). However, other parameters such as temperature (Burton and Walter, 1984; Morse et al, 1997; Balthasar and Cusack, 2015), pCO2 (Lee and Morse, 2010), and SO4 (Morse et al., 2007) are also known to influence CaCO3 polymorph formation but are often overlooked in the context of aragonite-calcite seas. Fluctuations in these parameters of Mg:Ca ratio, SO42+ and pCO2 of seawater have been suggested to cause shifts in original composition of non-biogenic marine carbonates, and in turn viewed as the main driving mechanisms facilitating the switch between aragonite and calcite dominance (Morse et al., 1997; Lee and Morse, 2010; Bots et al., 2011). Specifically the influence of temperature is important because it is likely to result in aragonite-calcite sea conditions to vary spatially (Balthasar and Cusack, 2015). Today marine temperatures are changing across the latitudes due to environmental factors. Global CO2 levels have increased significantly since industrialisation (Doney et al., 2009), with 33% entering the oceans and reducing pH (Raven et al., 2005) accelerating climate change (IPCC, 2013) and influencing marine calcification (Fitzer et al., 2014a; 2015b; Bach, 2015; Zhao et al., 2017). Strong links between the carbon cycle and climate change observed in the rock record give evidence that environmental changes such as pCO2 and global warming have impacts on calcification and marine biota (Hönish et al., 2012). The first objective was to determine the influence of Mg:Ca ratio, temperature and water movement on the first-formed precipitates of non-biogenic CaCO3 precipitation yielded via a continuous addition technique experiments (Chapter 3). CaCO3 precipitation was induced by continuously adding bicarbonate to a bulk solution of known Mg:Ca ratio (1,2 or 3), and fixed salinity of 35 (practical salinity scale), at 20°C and 30ºC in still conditions, and then repeated with the solution being shaken at 80rpm mimicking more natural marine conditions. The mineralogy and crystal morphology of precipitates was determined using Raman Spectroscopy and Scanning Electron Microscopy. Results in Chapter 3 indicated that polymorphs co-precipitate, with the ratio of aragonite to calcite increasing with increased Mg:Ca ratio and elevated temperature. The main difference between still and shaken conditions was that overall, more crystals of aragonite compared to calcite precipitate in shaking conditions. The crystal size is less influenced in aragonite, but calcite crystals were smaller. These results contradict current views on aragonite-calcite seas as spatially homogenous ocean states need to be re-examined to include the effect of temperature on the spatial distribution of CaCO3 polymorphs. Examining polymorph growth under these experimental constraints allows us to gain a better understanding of how temperature and Mg:Ca together control non-biogenic aragonite and calcite precipitation providing a more realistic environmental framework in which to evaluate the evolution of biomineralisation. To further this work, the same continuous addition technique was used with the presence of sulphate in the mother solution (Chapter 4). Sulphate being the 4th most common marine ion (Halvey et al., 2012) and known to have an influence on mineralogy (Kontrec et al., 2004). The presence of sulphate increase the aragonite to calcite proportion formed compared to sulphate-free conditions (Chapter 4). Elevated temperature with sulphate further increased the proportion of aragonite to calcite facilitated (Chapter 4). In the presence of sulphate the main difference between sulphate-free environments and those with sulphate environments was: in still conditions the presence of sulphate increased the crystal number more than the crystal size at 20°C; at 30°C or in shaken conditions the presence of sulphate increased the crystal size of aragonite to calcite much more than it had influence on the crystal number. Non-biogenically the influence of sulphate lowered the threshold of Mg:Ca ratio that the switch between calcite and aragonite would be facilitated at (Bots et al., 2011). This would have implications for marine calcification as pure calcite seas would become very rare and imply that organisms would be forming calcified hard parts out with the supported mineralogies. Biogenic application of these results is complex however as organisms often have the ability to select aragonite as their main polymorph for their own functional requirements (Weiner and Dove, 2003). The growth parameters of non-biogenic polymorph formations grown from artificial seawater can be used to understand how organism control can influence the polymorph formation under similar conditions (Kawano et al., 2009). Assessing the elemental composition of mussel shells grown under know conditions of temperature and pCO2 allowed the environmental influences on mineralogy be assessed under possible the projected changes in climate forecast to occur by 2100 by IPCC (2013). Prior to this research, no study had used Mytilus edulis shell elemental composition to test the influence of aragonite-calcite sea conditions on mineralogy. This research compiles a detailed source of information on the constraints from environmental sources such as temperature and pCO2, on the elemental concentrations within shell formation and what potential changes could occur in response to a changing marine environment (Chapter 5). Here elevated temperature significantly increased the concentration of magnesium in calcite, but did not influence the magnesium concentration of aragonite unless combined with elevated pCO2. The concentrations of sulphur in calcite were significantly decreased at elevated pCO2 or combined increased temperature and pCO2 as concentrations of sodium were found to be increased under these conditions. In aragonite the concentrations of both sulphur and sodium were significantly different under all scenarios. Strontium did not yield any significant results in this research in either calcite or aragonite. Results observed indicate that the shell elemental concentrations are influenced differently in aragonite or calcite, and further influenced by environmental conditions based on the original mineralogy. This suggests that physiological mechanisms under the constraints of increased temperature and pCO2 can override the seawater chemistry influences of aragonite-calcite seas impacting on mineralogy.
This research allows comparison of how non-biogenic and biogenic CaCO3 formation is influenced by seawater chemistry and environmental parameters to determine the dominant mineralogy. Increased temperature in both formations has shown to increase the impact of magnesium on calcite enabling the facilitation of aragonite. However, magnesium has influence on biogenic aragonite in extreme combined conditions of elevated temperature and pCO2. This work indicates that CaCO3 formation is complex and requires a multi-variable approach to understanding the mechanisms that facilitate the dominant mineralogy. By including variables such as temperature, this research suggests that aragonite-calcite seas conditions do not facilitate globally homogeneous switches in mineralogy, but the mineralogy is indeed influenced on latitudinal scales by other factors that influence the mechanisms involved.
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Conci, Nicola [Verfasser], and Gert [Akademischer Betreuer] Wörheide. "Molecular biomineralization of octocoral skeletons: calcite versus aragonite / Nicola Conci ; Betreuer: Gert Wörheide." München : Universitätsbibliothek der Ludwig-Maximilians-Universität, 2020. http://d-nb.info/1211957616/34.

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Books on the topic "Aragonite"

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W, Schmoker J., and Geological Survey (U.S.), eds. Porosity, grain-density, and inferred aragonite-content data from the Miami Limestone, Miami area and lower Florida Keys. [Reston, Va.?]: U.S. Dept. of the Interior, Geological Survey, 1985.

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Jan, F. G. Bourrouilh-le. Plates-formes carbonatées et atolls du centre et sud Pacifique: Stratigraphie, sédimentologie, minéralogie et géochimie, diagenèses et émersions-- aragonite, calcite, dolomite, bauxite et phosphate. Orléans, France: BRGM, 1996.

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Caminiti, Totino. Il capitano aragonese. [Messina, Italy]: A. Siciliano, 1993.

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Casula, Francesco Cesare. La Sardegna aragonese. Sassari: Chiarella, 1990.

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Tommasino, Attilia. Sessa Aurunca nel periodo aragonese. Ferrara: G. Corbo, 1997.

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Ramón, Acín. Entre dos mundos-- y una ilusión. [Zaragoza]: Gobierno de Aragón, Departamento de Presidencia y Relaciones Institucionales, 2002.

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Francho, Nagore Laín, ed. El Aragonés hoy: Informe sobre la situación actual de la lengua aragonesa = Hodiauo de la aragona linguo = The Aragonese today. Uesca: Consello d'a Fabla Aragonesa, 1989.

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Aragüés, Chusé. Dizionario aragonés-castellán, castellano-aragonés. [Spain]: Ligallo de Fablans de L'Aragonés, 1989.

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Andolz, Rafael. Diccionario aragonés: Aragonés-castellano, castellano-aragonés. 5th ed. Zaragoza: Mira Editores, 2004.

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Ruiz, Antonio Martínez. Vocabulario básico bilingüe: Aragonés-castellano y castellano-aragonés. Uesca: Publicazions d'o Consello d'a Fabla Aragonesa, 1997.

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Book chapters on the topic "Aragonite"

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Rothwell, R. G. "Aragonite." In Minerals and Mineraloids in Marine Sediments, 36–41. Dordrecht: Springer Netherlands, 1989. http://dx.doi.org/10.1007/978-94-009-1133-8_4.

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McLaren, Sue J. "Aragonite." In Encyclopedia of Modern Coral Reefs, 47. Dordrecht: Springer Netherlands, 2011. http://dx.doi.org/10.1007/978-90-481-2639-2_179.

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Gooch, Jan W. "Aragonite." In Encyclopedic Dictionary of Polymers, 46. New York, NY: Springer New York, 2011. http://dx.doi.org/10.1007/978-1-4419-6247-8_768.

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Chen, Bin, Xiang He Peng, and Xin Yan Wu. "Lambdoidal Layup of Aragonite Sheets in Conch Shell." In Key Engineering Materials, 2532–35. Stafa: Trans Tech Publications Ltd., 2007. http://dx.doi.org/10.4028/0-87849-410-3.2532.

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Korach, Chad S., and Ranjith Krishna Pai. "Mechanical Properties of a Nanostructured Poly (KAMPS)/aragonite Composite." In Conference Proceedings of the Society for Experimental Mechanics Series, 131–36. New York, NY: Springer New York, 2011. http://dx.doi.org/10.1007/978-1-4614-0219-0_18.

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Luo, Cheng, Lei Xie, and Xiao Xiang Wang. "In Vitro Growth of Aragonite Crystal on Nacre Surface." In Key Engineering Materials, 1335–38. Stafa: Trans Tech Publications Ltd., 2007. http://dx.doi.org/10.4028/0-87849-422-7.1335.

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Chen, Bin, Xiang He Peng, and Shi Tao Sun. "Research on the Curving Aragonite Sheets in Clam’s Shell." In Bioceramics 20, 475–78. Stafa: Trans Tech Publications Ltd., 2007. http://dx.doi.org/10.4028/0-87849-457-x.475.

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Sandberg, Philip A. "Nonskeletal Aragonite and pCO2 in the Phanerozoic and Proterozoic." In The Carbon Cycle and Atmospheric CO2 : Natural Variations Archean to Present, 585–94. Washington, D. C.: American Geophysical Union, 2013. http://dx.doi.org/10.1029/gm032p0585.

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Yang, Yiqi, Zhenping Qin, Yu Qian, Hongxia Guo, and Shulan Ji. "Adsorption of Cd(II) Ion on Aragonite Calcium Carbonate Crystals." In Springer Proceedings in Energy, 759–66. Singapore: Springer Singapore, 2018. http://dx.doi.org/10.1007/978-981-13-0158-2_77.

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Gauldie, R. W., G. Raina, S. K. Sharma, and I. F. West. "Imaging Matrix Materials and Fundamental Lamellae Structure of Biogenic Aragonite." In Atomic Force Microscopy/Scanning Tunneling Microscopy, 77–84. Boston, MA: Springer US, 1994. http://dx.doi.org/10.1007/978-1-4757-9322-2_7.

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Conference papers on the topic "Aragonite"

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Dean, Christopher David, Peter A. Allison, Gary J. Hampson, Dan J. Lunt, Alexandros Avdis, and Paul J. Markwick. "SPATIAL ARAGONITE BIAS IN EPICONTINENTAL SEAS." In GSA Annual Meeting in Denver, Colorado, USA - 2016. Geological Society of America, 2016. http://dx.doi.org/10.1130/abs/2016am-286475.

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Crespo-Feo, E., J. Garcia-Guinea, V. Correcher, A. Garralon, and Arnold Gucsik. "Spectrally-Resolved Luminescence on Hydrothermal Aragonite." In MICRO-RAMAN SPECTROSCOPY AND LUMINESCENCE STUDIES IN THE EARTH AND PLANETARY SCIENCES: Proceedings of the International Conference Spectroscopy 2009. AIP, 2009. http://dx.doi.org/10.1063/1.3222877.

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Castillo Alvarez, Maria, Nicola Allison, Adrian Finch, Kirsty Penkman, Matthieu Clog, and Roland Kroger. "Experimental investigation of factors controlling aragonite crystallization." In Goldschmidt2021. France: European Association of Geochemistry, 2021. http://dx.doi.org/10.7185/gold2021.7637.

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Wheeler, Dale. "Aragonite pseudomorphs of Guadalupe County, New Mexico." In 21st Annual New Mexico Mineral Symposium. Socorro, NM: New Mexico Bureau of Geology and Mineral Resources, 2000. http://dx.doi.org/10.58799/nmms-2000.237.

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Pederson, Chelsea, Vasileios Mavromatis, Martin Dietzel, Claire Rollion-Bard, and Adrian Immenhauser. "DIAGENETIC RESPONSE OF ARAGONITE ARCHIVES TO EXPERIMENTAL ALTERATION." In GSA 2020 Connects Online. Geological Society of America, 2020. http://dx.doi.org/10.1130/abs/2020am-359678.

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Riding, Robert, Liyuan Liang, and Philip Fralick. "OXYGEN AND THE ARCHEAN INCEPTION OF ARAGONITE SEAS." In GSA Connects 2021 in Portland, Oregon. Geological Society of America, 2021. http://dx.doi.org/10.1130/abs/2021am-365322.

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Liu, Jianjun. "Simulation of structural transformation in aragonite CaCo[sub 3]." In Fundamental physics of ferroelectrics 2000. AIP, 2000. http://dx.doi.org/10.1063/1.1324472.

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He, Ran, Meng Ning, Kang-Jun Huang, and Bing Shen. "MG ISOTOPE SYSTEMATICS DURING EARLY DIAGENETIC ARAGONITE-CALCITE TRANSITION." In GSA Annual Meeting in Indianapolis, Indiana, USA - 2018. Geological Society of America, 2018. http://dx.doi.org/10.1130/abs/2018am-318923.

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Haviv, Itai, Maytal Sadeh, Anton Vaks, Mira Bar-Matthews, Amos Frumkin, Avner Aylon, and Bar Elisha. "ARAGONITE AND CALCITE (U-TH)/HE GEOCHRONOLOGY AND THERMOCHRONOLOGY." In GSA Connects 2022 meeting in Denver, Colorado. Geological Society of America, 2022. http://dx.doi.org/10.1130/abs/2022am-381509.

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Wassenburg, Jasper, Sebastian Breitenbach, Denis Scholz, Hai Cheng, Lijuan Sha, and Yassine Ait Brahim. "Speleothem aragonite trace element partitioning: insights from cave monitoring." In Goldschmidt2023. France: European Association of Geochemistry, 2023. http://dx.doi.org/10.7185/gold2023.20821.

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Reports on the topic "Aragonite"

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Koleva-Rekalova, Elena, Ivan Genov, and Krasimira Slavova. Aragonite in the Holocene Sediments of Cores EUXRo01‑1 and EUXRo03‑3 from the NW Black Sea Slope. "Prof. Marin Drinov" Publishing House of Bulgarian Academy of Sciences, 2018. http://dx.doi.org/10.7546/crabs.2018.07.09.

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2

Schwinger, Jörg. Report on modifications of ocean carbon cycle feedbacks under ocean alkalinization. OceanNETs, June 2022. http://dx.doi.org/10.3289/oceannets_d4.2.

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Abstract:
Ocean Alkalinization deliberately modifies the chemistry of the surface ocean to enhance the uptake of atmospheric CO2. Here we quantify, using idealized Earth system model (ESM) simulations, changes in carbon cycle feedbacks and in the seasonal cycle of the surface ocean carbonate system due to ocean alkalinization. We find that both, carbon-concentration and carbon climate feedback, are enhanced due to the increased sensitivity of the carbonate system to changes in atmospheric CO2 and changes in temperature. While the temperature effect, which decreases ocean carbon uptake, remains small in our model, the carbon concentration feedback enhances the uptake of carbon due to alkalinization by more than 20%. The seasonal cycle of air-sea CO2 fluxes is strongly enhanced due to an increased buffer capacity in an alkalinized ocean. This is independent of the seasonal cycle of pCO2, which is only slightly enhanced. The most significant change in the seasonality of the surface ocean carbonate system is an increased seasonal cycle of the aragonite saturation state, which has the potential to adversely affect ecosystem health.
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3

Zurutuza-Muñoz,, Cristina, and Carmela García-Ortega. 2009 European Parliament Elections in the Aragonese Press. Revista Latina de Comunicación Social, 2011. http://dx.doi.org/10.4185/rlcs-067-945-001-022-en.

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4

Muñoz Gómez, Víctor. The Seigneurial Pedido: Exaction, Negotiation and Seigneurial Power in Late Medieval Castile (The Example of the Towns in the Aragonese Trastámara Estates). Edicions de la Universitat de Lleida, 2023. http://dx.doi.org/10.21001/itma.2023.16.09.

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5

Towards an Understanding of the Role of Aragonite in the Mechanical Properties of Nacre. Office of Scientific and Technical Information (OSTI), August 2010. http://dx.doi.org/10.2172/992942.

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