Luisa Ottolini

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Luisa Ottolini (born July 10, 1954, in Tortona, province of Alessandria, Italy) is an Italian physicist.

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Biography

In 1978, Luisa Ottolini graduated in Physics at the University of Pavia. From 1982 to 1986, she was the Head of the Structuristic Section at the Istituto Sperimentale dei Metalli Leggeri (I.S.M.L.) in Novara. [1] In 1987, she activated the Strategic Project of the National Research Council of Italy (CNR) An Ion Microprobe for Advanced Researches in the Earth Sciences with the installation at the “Centro di Studio per la Cristallografia Strutturale” in Pavia of the first, and so far, the only one National Laboratory of Secondary Ion Mass Spectrometry (SIMS) in the Earth Sciences. Since that time she has been the Head of the SIMS Lab. Starting from 1989, she activated the National SIMS service for University and CNR Institutions offering the Earth Science Committee (05), following more than 90 research projects. [2] In 2002-2005 she coordinated a research Unit in Pavia, sponsored by the European Framework Project EUROMELT [3] (European Community’s Human Potential Programme, contract HPRN-CT-2002-00211). Between December 2005 and September 2017 she was the Head of CNR-Institute of Geosciences and Geo-resources (IGG)-Section of Pavia.

She has co-authored more than 150 international ISI publications, of which 5 in Nature ; [4] [5] [6] [7] [8] more than 200 Abstracts at International and National Meetings, 35 monographs and inner reports. [9]

Main scientific interests

Her research activities mainly concerned the use of SIMS for the quantitative measurement of low-concentration constituents, of light (Lithium, Beryllium and Boron) and volatile elements (Hydrogen, Fluorine, Chlorine, Carbon) in geological samples, with particular reference to the investigation of the physical/chemical processes underlying the production of secondary ions, aiming at overcoming the limitations of the technique (interferences and non-linear effects, “matrix effects”); the development, set up and optimization of SIMS procedures for trace elements, [10] light and volatile elements, [11] [12] and ultra-trace elements [13] in the frame of petrologic, geochemical and crystal-chemical studies, with particular reference to the investigation of melt inclusions, [14] [15] silicate minerals, [16] [17] artificial glasses, [18] chemically-complex silicate [19] and non-silicate matrixes, [20] experimental charges. [21] [22]

Awards and honors

Related Research Articles

<span class="mw-page-title-main">Magma</span> Hot semifluid material found beneath the surface of Earth

Magma is the molten or semi-molten natural material from which all igneous rocks are formed. Magma is found beneath the surface of the Earth, and evidence of magmatism has also been discovered on other terrestrial planets and some natural satellites. Besides molten rock, magma may also contain suspended crystals and gas bubbles.

<span class="mw-page-title-main">Peridot</span> Green gem-quality mineral

Peridot, sometimes called chrysolite, is a yellowish-green transparent variety of olivine. Peridot is one of the few gemstones that occur in only one color.

<span class="mw-page-title-main">Zircon</span> Zirconium silicate, a mineral belonging to the group of nesosilicates

Zircon is a mineral belonging to the group of nesosilicates and is a source of the metal zirconium. Its chemical name is zirconium(IV) silicate, and its corresponding chemical formula is ZrSiO4. An empirical formula showing some of the range of substitution in zircon is (Zr1–y, REEy)(SiO4)1–x(OH)4x–y. Zircon precipitates from silicate melts and has relatively high concentrations of high field strength incompatible elements. For example, hafnium is almost always present in quantities ranging from 1 to 4%. The crystal structure of zircon is tetragonal crystal system. The natural color of zircon varies between colorless, yellow-golden, red, brown, blue, and green.

<span class="mw-page-title-main">Peridotite</span> Coarse-grained ultramafic igneous rock type

Peridotite ( PERR-ih-doh-tyte, pə-RID-ə-) is a dense, coarse-grained igneous rock consisting mostly of the silicate minerals olivine and pyroxene. Peridotite is ultramafic, as the rock contains less than 45% silica. It is high in magnesium (Mg2+), reflecting the high proportions of magnesium-rich olivine, with appreciable iron. Peridotite is derived from Earth's mantle, either as solid blocks and fragments, or as crystals accumulated from magmas that formed in the mantle. The compositions of peridotites from these layered igneous complexes vary widely, reflecting the relative proportions of pyroxenes, chromite, plagioclase, and amphibole.

<span class="mw-page-title-main">Phlogopite</span> Member of the mica family of phyllosilicates

Phlogopite is a yellow, greenish, or reddish-brown member of the mica family of phyllosilicates. It is also known as magnesium mica.

<span class="mw-page-title-main">Stishovite</span> Tetragonal form of silicon dioxide

Stishovite is an extremely hard, dense tetragonal form (polymorph) of silicon dioxide. It is very rare on the Earth's surface; however, it may be a predominant form of silicon dioxide in the Earth, especially in the lower mantle.

<span class="mw-page-title-main">Frank Hawthorne</span> Canadian mineralogist and crystallographer

Frank Christopher Hawthorne is a Canadian mineralogist, crystallographer and spectroscopist. He works at the University of Manitoba, Winnipeg, Manitoba, Canada, and is currently Distinguished Professor Emeritus. By combining Graph Theory, Bond-Valence Theory and the moments approach to the electronic energy density of solids he has developed Bond Topology as a rigorous approach to understanding the atomic arrangements, chemical compositions and paragenesis of complex oxide and oxysalt minerals.

<span class="mw-page-title-main">Ringwoodite</span> High-pressure phase of magnesium silicate

Ringwoodite is a high-pressure phase of Mg2SiO4 (magnesium silicate) formed at high temperatures and pressures of the Earth's mantle between 525 and 660 km (326 and 410 mi) depth. It may also contain iron and hydrogen. It is polymorphous with the olivine phase forsterite (a magnesium iron silicate).

<span class="mw-page-title-main">Melt inclusion</span>

A melt inclusion is a small parcel or "blobs" of melt(s) that is entrapped by crystals growing in magma and eventually forming igneous rocks. In many respects it is analogous to a fluid inclusion within magmatic hydrothermal systems. Melt inclusions tend to be microscopic in size and can be analyzed for volatile contents that are used to interpret trapping pressures of the melt at depth.

<span class="mw-page-title-main">Tobermorite</span> Inosilicate alteration mineral in metamorphosed limestone and in skarn

Tobermorite is a calcium silicate hydrate mineral with chemical formula: Ca5Si6O16(OH)2·4H2O or Ca5Si6(O,OH)18·5H2O.

<span class="mw-page-title-main">Fluor-liddicoatite</span>

Fluor-liddicoatite is a rare member of the tourmaline group of minerals, elbaite subgroup, and the theoretical calcium endmember of the elbaite-fluor-liddicoatite series; the pure end-member has not yet been found in nature. Fluor-liddicoatite is indistinguishable from elbaite by X-ray diffraction techniques. It forms a series with elbaite and probably also with olenite. Liddiocoatite is currently a non-approved mineral name, but Aurisicchio et al. (1999) and Breaks et al. (2008) found OH-dominant species. Formulae are

<span class="mw-page-title-main">Edenite</span> Amphibole, double chain inosilicate mineral

Edenite is a double chain silicate mineral of the amphibole group with the general chemical composition NaCa2Mg5(Si7Al)O22(OH)2. Edenite is named for the locality of Edenville, Orange County, New York, where it was first described.

<span class="mw-page-title-main">Fluoborite</span>

Fluoborite has a chemical formula of Mg3(BO3)(F,OH)3. Its name comes from its main chemical components, fluorine and boron. It was first described in 1926.

<span class="mw-page-title-main">Fluor-uvite</span>

Fluor-uvite is a tourmaline mineral with the chemical formula CaMg3(Al5Mg)(Si6O18)(BO3)3(OH)3F. It is a rare mineral that is found in calcium rich contact metamorphic rocks with increased amounts of boron. Uvite is trigonal hexagonal, which means that it has three equal length axes at 120 degrees, all perpendicular to its fourth axis which has a different length. Uvite is part of the space group 3m. Uvite's hardness has been measured to be 7.5 on the Mohs hardness scale. The color of uvite widely varies, depending on the sample, but is mostly deep green or brown. In regard to uvite's optical properties, it is uniaxial (-) and anisotropic, meaning that the velocity of light in the mineral depends on the path that it takes. In plane polarized light, uvite is colorless to pale yellow and shows weak pleochroism.

Silicate perovskite is either (Mg,Fe)SiO3 or CaSiO3 when arranged in a perovskite structure. Silicate perovskites are not stable at Earth's surface, and mainly exist in the lower part of Earth's mantle, between about 670 and 2,700 km depth. They are thought to form the main mineral phases, together with ferropericlase.

<span class="mw-page-title-main">Mineral evolution</span> Increasing mineral diversity over time

Mineral evolution is a recent hypothesis that provides historical context to mineralogy. It postulates that mineralogy on planets and moons becomes increasingly complex as a result of changes in the physical, chemical and biological environment. In the Solar System, the number of mineral species has grown from about a dozen to over 5400 as a result of three processes: separation and concentration of elements; greater ranges of temperature and pressure coupled with the action of volatiles; and new chemical pathways provided by living organisms.

<span class="mw-page-title-main">Mantle oxidation state</span> Application of oxidation state to the study of the Earths mantle

Mantle oxidation state (redox state) applies the concept of oxidation state in chemistry to the study of the Earth's mantle. The chemical concept of oxidation state mainly refers to the valence state of one element, while mantle oxidation state provides the degree of decreasing of increasing valence states of all polyvalent elements in mantle materials confined in a closed system. The mantle oxidation state is controlled by oxygen fugacity and can be benchmarked by specific groups of redox buffers.

<span class="mw-page-title-main">Deep water cycle</span> Movement of water in the deep Earth

The deep water cycle, or geologic water cycle, involves exchange of water with the mantle, with water carried down by subducting oceanic plates and returning through volcanic activity, distinct from the water cycle process that occurs above and on the surface of Earth. Some of the water makes it all the way to the lower mantle and may even reach the outer core. Mineral physics experiments show that hydrous minerals can carry water deep into the mantle in colder slabs and even "nominally anhydrous minerals" can store several oceans' worth of water.

<span class="mw-page-title-main">Diamond inclusions</span>

Diamond inclusions are the non-diamond materials that get encapsulated inside diamond during its formation process in the mantle. The trapped materials can be other minerals or fluids like water. Since diamonds have high strength and low reactivity with either the inclusion or the volcanic host rocks which carry the diamond to the Earth's surface, the diamond serves as a container that preserves the included material intact under the changing conditions from the mantle to the surface. Although diamonds can only place a lower bound on the pressure of their formation, many inclusions provide additional constraints on the pressure, temperature and even age of formation.

<span class="mw-page-title-main">Breyite</span>

Breyite is a high pressure calcium silicate mineral (CaSiO3) found in diamond inclusions. It is the second most abundant inclusion after ferropericlase, for diamonds with a deep Earth origin. Its occurrence can also indicate the host diamond's super-deep origin. This mineral is named after German mineralogist, petrologist and geochemist Gerhard P. Brey.

References

  1. ↑ scegliere, Niklas Andersson, Lorena Nurzia - Conosci per. "CNR - Comitato per le Pari Oportunità - ricercatrici d'eccelenza - Luisa Ottolini". www.cpseditrice.it.{{cite web}}: CS1 maint: multiple names: authors list (link)
  2. ↑ "CNR-->Storia del CNR al femminile". www.cnr.it.
  3. ↑ EUROMELT, January 2013
  4. ↑ Schiano, Pierre; Clocchiatti, Roberto; Ottolini, Luisa; Busà, Tiziana (2001). "Transition of Mount Etna lavas from a mantle-plume to an island-arc magmatic source". Nature. 412 (6850): 900–904. Bibcode:2001Natur.412..900S. doi:10.1038/35091056. PMID   11528476. S2CID   4425759.
  5. ↑ Rampone, Elisabetta; Bottazzi, Piero; Ottolini, Luisa (1991). "Complementary Ti and Zr anomalies in orthopyroxene and clinopyroxene from mantle peridotites". Nature. 354 (6354): 518. Bibcode:1991Natur.354..518R. doi:10.1038/354518a0. S2CID   4335564.
  6. ↑ Ligi, Marco; Bonatti, Enrico; Cipriani, Anna; Ottolini, Luisa (2005). "Water-rich basalts at mid-ocean-ridge cold spots". Nature. 434 (7029): 66–69. Bibcode:2005Natur.434...66L. doi:10.1038/nature03264. PMID   15744299. S2CID   254959.
  7. ↑ Bonatti, Enrico; Ligi, Marco; Brunelli, Daniele; Cipriani, Anna; Fabretti, Paola; Ferrante, Valentina; Gasperini, Luca; Ottolini, Luisa (2003). "Mantle thermal pulses below the Mid-Atlantic Ridge and temporal variations in the formation of oceanic lithosphere". Nature. 423 (6939): 499–505. Bibcode:2003Natur.423..499B. doi:10.1038/nature01594. PMID   12774114. S2CID   4416441.
  8. ↑ Spengler, Dirk; Roermund, Herman L. M. van; Drury, Martyn R.; Ottolini, Luisa; Mason, Paul R. D.; Davies, Gareth R. (2006). "Deep origin and hot melting of an Archaean orogenic peridotite massif in Norway". Nature. 440 (7086): 913–917. Bibcode:2006Natur.440..913S. doi:10.1038/nature04644. PMID   16612379. S2CID   4419956.
  9. ↑ Web of Knowledge, January 2013
  10. ↑ AN ION PROBE CONTRIBUTION TO RARE-EARTH ELEMENT INVESTIGATION OF GABBRO GOG-1 USING SECONDARY ION MASS-SPECTROMETRY
  11. ↑ Ottolini, Luisa.; Bottazzi, Piero.; Vannucci, Riccardo. (1 August 1993). "Quantification of lithium, beryllium, and boron in silicates by secondary-ion mass spectrometry using conventional energy filtering". Analytical Chemistry. 65 (15): 1960–1968. doi:10.1021/ac00063a007.
  12. ↑ Ottolini, Luisa; Bottazzi, Piero; Zanetti, Alberto; Vannucci, Riccardo (1 January 1995). "Determination of hydrogen in silicates by secondary ion mass spectrometry". Analyst. 120 (5): 1309. Bibcode:1995Ana...120.1309O. doi:10.1039/AN9952001309.
  13. ↑ Ottolini, Luisa; Le Fèvre, Brieuc; Vannucci, Riccardo (2004). "Direct assessment of mantle boron and lithium contents and distribution by SIMS analyses of peridotite minerals" (PDF). Earth and Planetary Science Letters. 228 (1–2): 19. Bibcode:2004E&PSL.228...19O. doi:10.1016/j.epsl.2004.09.027.
  14. ↑ Gioncada, A.; Clocchiatti, R.; Sbrana, A.; Bottazzi, P.; Massare, D.; Ottolini, L. (6 April 1998). "A study of melt inclusions at Vulcano (Aeolian Islands, Italy): insights on the primitive magmas and on the volcanic feeding system". Bulletin of Volcanology. 60 (4): 286–306. Bibcode:1998BVol...60..286G. doi:10.1007/s004450050233. S2CID   128674809.
  15. ↑ Pierre, Schiano; Robert, Clocchiatti; Luisa, Ottolini; Alessandro, Sbrana (1 March 2004). "The relationship between potassic, calc-alkaline and Na-alkaline magmatism in South Italy volcanoes: A melt inclusion approach". Earth and Planetary Science Letters. 220 (1–2): 121. Bibcode:2004E&PSL.220..121S. doi:10.1016/S0012-821X(04)00048-2.
  16. ↑ Ottolini, Luisa; Cámara, Fernando; Bigi, Simona (1 January 2000). "An investigation of matrix effects in the analysis of fluorine in humite-group minerals by EMPA, SIMS, and SREF". American Mineralogist. 85 (1): 89–102. Bibcode:2000AmMin..85...89O. doi:10.2138/am-2000-0110. S2CID   53442574.
  17. ↑ Ottolini, Luisa; Hawthorne, Frank C. (2 November 2001). "SIMS ionization of hydrogen in silicates: a case study of kornerupine". Journal of Analytical Atomic Spectrometry. 16 (11): 1266–1270. doi:10.1039/B105674N.
  18. ↑ Fevre, Brieuc Le; Ottolini, Luisa (1 September 2006). "Preparation of Reference Glasses for in-situ Analysis of Lithium and Boron". Microchimica Acta. 155 (1–2): 189–194. doi:10.1007/s00604-006-0541-x. S2CID   96668352.
  19. ↑ Ottolini, Luisa; Cámara, Fernando; Devouard, Bertrand (1 April 2004). "New SIMS Procedures for the Characterization of a Complex Silicate Matrix, Na3(REE,Th,Ca,U)Si6O15·2.5H2O (Sazhinite), and Comparison with EMPA and SREF Results". Microchimica Acta. 145 (1–4): 139–146. doi:10.1007/s00604-003-0143-9. S2CID   97979248.
  20. ↑ Cámara, Fernando; Ottolini, Luisa (2000). "New data on the crystal-chemistry of fluoborite by means of SREF, SIMS, and EMP analysis" (PDF). American Mineralogist. 85 (1): 103. Bibcode:2000AmMin..85..103C. doi:10.2138/am-2000-0111. S2CID   101968776.
  21. ↑ Médard, Etienne; Schmidt, Max W.; Schiano, Pierre; Ottolini, Luisa (1 March 2006). "Melting of Amphibole-bearing Wehrlites: an Experimental Study on the Origin of Ultra-calcic Nepheline-normative Melts". Journal of Petrology. 47 (3): 481–504. Bibcode:2005JPet...47..481M. doi: 10.1093/petrology/egi083 . hdl: 20.500.11850/1394 .
  22. ↑ Kägi, Ralf; Müntener, Othmar; Ulmer, Peter; Ottolini, Luisa (1 April 2005). "Piston-cylinder experiments on H2O undersaturated Fe-bearing systems: An experimental setup approaching fO2 conditions of natural calc-alkaline magmas". American Mineralogist. 90 (4): 708–717. Bibcode:2005AmMin..90..708K. doi:10.2138/am.2005.1663. S2CID   128650303.
  23. ↑ History of the Women in the CNR
  24. ↑ Abstract on Ferri-ottoliniite from American Mineralogist, May 2004
  25. ↑ Barthelmy, Dave. "Ferri-ottoliniite Mineral Data". webmineral.com.
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