Sample records for PLANOS CRISTALINOS (crystal faces)
from WorldWideScience.org

Sample records 1 - 19 shown.



1

The structure of plasmid-encoded transcriptional repressor CopG unliganded and bound to its operator

Gomis-Rüth, F. Xavier; Solà, Maria; Acebo, Paloma; Párraga, Antonio; Guasch, Alicia; Eritja Casadellà, Ramón; González, Ana; Solar, Gloria del; Coll, Miquel
1998-12-15

Digital.CSIC (Spain)

3

The C form of n-hexadecanoic acid

Moreno, Evelyn; Cordobilla, Raquel; Calvet, Teresa; Lahoz, Fernando J.; Balana, Ana I.
2006-03-01

Digital.CSIC (Spain)

4

Structure refinement of samarium monothio oxide

Llanos, Jaime; Mujica, Carlos; Henríquez, Alicia; Gómez-Romero, P.; Molins Grau, Elíes
2001-03-02

Digital.CSIC (Spain)

5

Reaction Sintering of Mexican Dolomite – Zircon Mixtures

Rodríguez Galicia, J. L.; Fernández Arguijo, B.; Rendón-Angeles, J. C.; Pena Castro, María del Pilar; Valle Fuentes, Francisco José; López-Cuevas, J.
2005-07-01

Digital.CSIC (Spain)

6

Photonic crystal properties of packed submicrometric SiO2 spheres

Míguez García, Hernán Ruy; López, C.; Meseguer Rico, Francisco; Blanco, Álvaro; Vázquez, Luis; Mayoral, R.; Ocaña Jurado, Manuel; Fornés, Vicente; Mifsud, A.
1997-09-01

Digital.CSIC (Spain)

7

Petrográfica y Geoquímica de la dolomía hospedante de una mineralización de Zn y Pb. Puesto Gregor, Neuquén, Argentina/ Petrography and geochemistry of a Zn- Pb mineralization hosted in a dolostone, Puesto Gregor, Neuquen, Argentina

Gómez, M. Cristina; Garrido, Mirta; Cesaretti, Nora; Domínguez, Eduardo
2008-07-01

Resumen en español En la Cuenca Neuquina (Argentina) y asociada a la Formación Lajas (Jurásico) se mencionó por primera vez una mineralización de esfalerita y galena asociada a carbonatos. En el área del yacimiento Puesto Gregor, ésta Formación está constituida por una secuencia clástico carbonática. Para caracterizar el ambiente de depositación de la dolomía hospedante de la mineralización de Zn y Pb se realizaron estudios petrográficos y geoquímicos. Entre los últimos los (mas) más utilizados son los análisis e interpretación de isótopos estables (O, C), elementos mayoritarios y trazas e inclusiones fluidas. En el horizonte dolomítico de 0,90 m de espesor y 300 m de corrida se distinguen petrográficamente dos tipos de dolomita: el primer tipo es penetrativo, sin preservación de la fábrica sedimentaria original y es anterior a la mineralización, el segundo tipo está vinculado a la precipitación de sulfuros y consiste en una dolomita de tipo silla de montar (saddle). El estudio de las inclusiones fluidas en la dolomita penetrativa indica la presencia de fluidos orgánicos y fluidos acuosos. Determinaciones microtermométricas sobre inclusiones fluidas acuosas revelaron temperaturas de 140º C. Geoquímicamente la capa presenta proporciones casi estequiométricas y promedios de CaCO3 y MgCO3 iguales al 52 y 48% molar, respectivamente. En cuanto a los elementos trazas, el Sr varió entre 79 y 159 ppm y el Na entre 74 y 225 ppm. Los contenidos de Mn y Fe son mucho más altos que los valores determinados para estos elementos en rocas carbonáticas. El contenido en ETR es bajo y los diagramas de ETR muestran una anomalía negativa de Ce y de Eu. Se determinaron valores de isótopos de C y O. Los valores de ä13 C (VPDB) entre -2,9 y -9 0/00 no son coherentes con los datos informados para calizas marinas de edad jurásica mientras que los valores de ä18O(VPDB) entre -2,6 y -4 0/00 coinciden con los valores informados para carbonatos de igual edad. Los datos de ä18O indican que la interacción entre el fluido y la roca de caja fue baja. Los valores del ä18O del fluido en equilibrio con la dolomía a temperaturas de 140ºC indican que este fluido corresponde a una salmuera de cuenca. Por otro lado, los isótopos de carbono indican un aporte de carbono procedente de la diagénesis de la materia orgánica causada por un aumento de temperatura vinculada al soterramiento de la cuenca. Los resultados petrográficos y geoquímicos son consistentes con la dolomitización de un carbonato de origen marino que sufrió soterramiento. Resumen en inglés In Neuquen Basin, Argentina, a Zn-Pb mineralization was first reported by Garrido et al. (2000). The ore occurs in a carbonatic level located in Puesto Gregor, 50 km SSE from the city of Zapala at 39°11'34'' S, 69° 59'18'' W (Fig. 1). The hosting bed, a dolostone, belongs to a carbonatic-siliciclastic sequence of Lajas Formation, which is part of the Cuyo Group, Jurassic age. In the mineralization of Pb-Zn deposits associated to dolostones, the fluids that were involved (mas) in the ore precipitation process were also related to the dolomitization of the carbonatic rock (Warren, 2000). In this contribution, field, petrographic and geochemical studies were carried out in order to determine the temperature and composition of the dolimitizing fluids. The obtained results were then compared to those obtained from Carbon and Oxygen isotopes (Garrido et al., 2001) to discuss the dolimitization process. The mineralized bed, 0.90 m thick, outcrops for about 300 m along the strike (W-E) and 60 m in the dip direction (Fig. 2). This bed pinches out toward the east and toward the west it is no longer visible, it is cover by scours. Petrographic studies determined that the host rock is a dolostone with a breccia texture that becomes more siliciclastic towards the east grading thus to a fine sandstone with carbonatic cement. The hypogenic mineralization, mainly sphalerite, low quantities of galena, pyrite and marcasite is found within the small fractures. Some ghosts of fossils are still visible, but pervasive dolomitization characterizes the horizon. Two distinct dolomites are recognized by crosscutting relationships: a fine to medium grained crystalline dolomite, and a coarse grained crystalline dolomite related to the mineralization. The fomer shows dark-orange and white crystals which occur as patches or partially filled vugs. These crystals are 120-400 mm in size and exhibit subhedral to anhedral shapes (Fig. 3). According to Sibley and Gregg (1987), the texture is no planar -a- unimodal to polimodal. The latter dolomite presents well developed crystals (> 5 mm); they are translucent with pink color and pearl shine and have crystal faces that look like a pavement and is referred as "saddle" dolomite according to Radke and Mathis (1980). This "saddle" dolomite is found into dissolution cavities or as clusters of crystals located on the wall fractures; it is always associated to the mineralization. Chemical analysis of major, traces and rare earth elements are homogeneous throughout the bed. Mean values are 15% MgO, 29,66% CaO and 40,43 % CO2, with high MnO and Fe2O3 contents. The molar percentages of CaCO3 and MgCO3 indicate near stoichiometric ratio (52% and 48%) with a light excess of Ca (Table 1, Fig. 4). The trace elements Sr, Na, Fe and Mn are used to constrain dolomite evolution. Sr values varies from 79 to 159 ppm and Na from 74 to 225 ppm; Mn and Fe contents are higher than the values determined for carbonatic rocks (Turekian and Wedepohl, 1961). ÓREE and LREE contents are low, and the diagram normalized to chondrite shows a negative anomaly of Eu and a great negative anomaly of Ce. The 13C (VPDB) and 18O (VPDB) values vary from -2,9 to -9(0)/00 and from -2,6 to -4 0/00 respectively (Table 2). The 13C are incoherent with the data recorded for Jurassic marine carbonates (near 0 0/00) while 18O values can be correlated with carbonates of the same age (Veizer et al., 1999). Petrography and chemical analysis allow characterizing the depositional environment of the Zn- Pb mineralized dolostone. The xenotopic texture of the dolomite with no planar crystals, gives evidence that the temperatures of deposition should have been higher than 50-60°C (Gregg and Sibley, 1984). On the other hand, the chemical composition, near ideal dolomites (stoichiometric ratio), indicates slow crystallization at high temperature (Morrow, 1982). Morover, the destructive fabric and the homogeneous composition suggest a high temperature dolomitization (Machel, 2004). Trace element values, mainly Na and Sr, agree with burial dolomites, as well as the fluid inclusions reported for these samples by Cesaretti et al. (2002). The negative Ce anomaly indicates that these rocks were formed in a marine environment. Two different processes of carbonate precipitation can produce negative Ce anomaly (Möller, 1989; Bau and Möller, 1992): deposition from seawater or from hydrothermal solutions equilibrated with highly oxydized sediments. The latter is discarded because of the presence of framboidal pyrite and organic matter, which, along with the Eu negative anomaly indicates that the dolimitization were generated under euxinic conditions. This dolostone is in contact with anoxic mudstones (Los Molles Formation, Cuyo Group). Petrographic and geochemical criteria reflect that the dolomitization were caused by normal or modified sea water in a burial environment at temperatures above 140ºC. In burial or altered dolostones, the oxygen isotopes reflect temperature of precipitation and isotope composition of the dolomitizing fluids. The oxygen isotope values of this dolomitized bed are compatible with the isotope composition of carbonates precipitated from sea water at 25°C. The narrow range in the obtained values indicates that there was no influence of meteoric water during this process (Allan and Mathews, 1982). The homogeneous values of 18O isotope suggest that the physic-chemical conditions remained constant during dolomitization, what is in agreement with the textural and geochemical homogeneity found in the study samples. The 18O isotope values of a fluid equilibrated with carbonate at 140°C indicate that the fluid belongs to a basinal fluid. The 13C isotopes reflect an organic origin for the carbon. This carbon came from the diagenesis of organic matter caused by an increase in temperature during the burial of the basin (Garrido et al., 2001; Cesaretti et al., 2002). In contrast with other MVT deposits of the world, in Puesto Gregor, the dolomitization was slow process acting at high temperatures, what has been confirmed by the homogeneity of the fabric and the narrow range in the isotope and trace elements composition. These conditions were reached during burial of the basin where the rocks interact with the basin fluids associated to the ore minerals.

Scientific Electronic Library Online (Spanish)

8

Magneto-volume effects in Fe-Cu solid solutions

Gorria, P.; Martínez-Blanco, D.; Iglesias, R.; Palacios, S. L.; Pérez, M. J.; Blanco, J. A.; Fernández Barquín, L.; Hernando, A.; González, Miguel A.
2006-05-01

Digital.CSIC (Spain)

9

Li deficiencies in LiNbO3 films prepared by pulsed laser deposition in a buffer gas

Gonzalo de los Reyes, José; Afonso, Carmen N.; Ballesteros, J. M.; Grosman, A.; Ortega, C.
1997-09-15

Digital.CSIC (Spain)

10
11

Influence of lysozyme on the precipitation of calcium carbonate: a kinetic and morphologic study

Jiménez-López, Concepción; Rodríguez-Navarro, Alejandro; Domínguez-Vera, José M.; García Ruiz, Juan Manuel
2003-05-01

Digital.CSIC (Spain)

12

In situ observation of the joint gel/impurity effect on protein crystal growth kinetics.

Driessche, Alexander E. S. Van; Otalora, Fermín; Gavira Gallardo, J. A.; Sazaki, Gen
2008-09-09

Digital.CSIC (Spain)

13

Estudio estructural del MoO3 y sus planos cristalinos/ Structural study of MoO3 and its crystal faces

Gesari, Susana; Irigoyen, Beatriz; Juan, Alfredo
1997-02-01

Resumen en inglés In the present work we present geometric models of the most studied MoO3 surfaces, which were obtained using the DTMM 2.0 Molecular Modeller software. MoO3 has an orthorhombic layered structure, with each layer comprised of two interleaved planes of MoO6 octahedral. These layers are parallel to the (010) crystal plane and only oxygen ions are exposed on their surfaces. This situation results in weak van der Waals bonding between layers and in a relatively inert surface. I (mas) n our approach to surface geometric structure we consider "ideal" crystal surface, in which the bulk atomic arrangement is maintained. These surfaces were generated by imaginary cleavage along appropriate planes in the bulk crystal structure.

Scientific Electronic Library Online (Spanish)

14

Direct and noninvasive observation of two-dimensional nucleation behavior of protein crystals by advanced optical microscopy

Van Driessche, Alexander E. S.; Sazaki, Gen; Otalora, Fermín; González-Rrico, Francisco M; Dold, Peter; Tsukamoto, Katsuo; Nakajima, Kazuo
2007-01-01

Digital.CSIC (Spain)

15

Crystal structure of a bacterial family-III cellulose-binding domain: a general mechanism for attachment to cellulose

Tormo, José; Lamed, Raphael; Chirino, Arthur J.; Morag, Ely; Bayer, Edward A.; Shoham, Yuval; Steitv, Thomas A.
1996-11-01

Digital.CSIC (Spain)

17

Composition of Tartrate Precipitates in White Wines used for Making Spanish Sparkling Wine

Correa-Gorospe, I.; Polo, M. C.; Rodríguez-Badiola, E.; Rodríguez-Clemente, R.
1991-01-01

Digital.CSIC (Spain)

18

An electron transparent proton detector for neutron decay studies

Hoedl, S. A.; Young, A. R.; Ade, H.; Lozano Fantoba, Antonio
2006-04-19

Digital.CSIC (Spain)