A numerical investigation of hydrocarbon related magnetic signatures

The iron sulphide greigite (Fe3S4) is linked to important diagenetic processes in sediments and to hydrocarbon formation and migration. The magnetic properties of this ferrimagnetic mineral are relatively obscure because it is difficult to synthesise and because it is unstable and therefore thought to be irrelevant to the geological record. However, it is increasingly recognised that greigite can remain stable on geological timescales. It is important to understand the magnetic properties of greigite to identify its presence and timing of formation as it is a proxy for environmental magnetic studies and for hydrocarbon microseepage identification. In this thesis, numerical methods are used to study the magnetic properties of greigite. Using a micromagnetic finite-element method (FEM), important questions regarding the magnetic structure and palaeomagnetic recording fidelity of gregite are addressed. For equidimensional particles, the single-domain (SD) to single-vortex (SV) threshold is found to be $d_0\approx 54$ nm and only SV particles >70 nm to carry stable magnetisations over billion-year timescales. A simplified model is developed to study the hysteresis and first-order reversal curve (FORC) properties of non-interacting idealised SD greigite particles. To understand the effects of SV magnetisations on FORC properties, a micromagnetic FEM is used to simulate randomly oriented dispersions of non-interacting greigite in the SV size range. SV effects dominate the FORC signal for particles >70 nm. Implications for FORC diagram interpretation are discussed. Magnetic inter-particle interactions are known to effect the FORC response of magnetic particle ensembles. A micromagnetic FEM is used to study the FORC signal of randomly dispersed strongly interacting clusters of greigite. The FORC response of strongly interacting greigite is found to be similar to that of multi-domain (MD) particles. Since naturally occurring greigite is rarely in a MD state, it is concluded that in greigite-bearing rocks that produce MD-like FORC signals the origin of this signal should be attributed to strong interactions between the particles.Open Acces

First-order reversal curve (FORC) diagrams of nanomagnets with cubic magnetocrystalline anisotropy: a numerical approach

First-order reversal curve (FORC) diagrams are increasingly used as a material’s magnetic domain state fingerprint. FORC diagrams of noninteracting dispersions of single-domain (SD) particles with uniaxial magnetocrystalline anisotropy (MCA) are well studied. However, a large class of materials possess a cubic MCA, for which the FORC diagram properties of noninteracting SD particle dispersions are less understood. A coherent rotation model was implemented to study the FORC diagram properties of noninteracting ensembles of SD particles with positive and negative MCA constants. The pattern formation mechanism is identified and related to the irreversible events the individual particles undergo. Our results support the utility of FORC diagrams for the identification of noninteracting to weakly-interacting SD particles with cubic MCA

Micromagnetic simulations of first-order reversal curve (FORC) diagrams of framboidal greigite

Greigite is a sensitive environmental indicator and occurs commonly in nature as magnetostatically interacting framboids. Until now only the magnetic response of isolated non-interacting greigite particles have been modelled micromagnetically. We present here hysteresis and first-order reversal curve (FORC) simulations for framboidal greigite (Fe3S4), and compare results to those for isolated particles of a similar size. We demonstrate that these magnetostatic interactions alter significantly the framboid FORC response compared to isolated particles, which makes the magnetic response similar to that of much larger (multidomain) grains. We also demonstrate that framboidal signals plot in different regions of a FORC diagram, which facilitates differentiation between framboidal and isolated grain signals. Given that large greigite crystals are rarely observed in microscopy studies of natural samples, we suggest that identification of multidomain-like FORC signals in samples known to contain abundant greigite could be interpreted as evidence for framboidal greigite

Magnetic vortex effects on first-order reversal curve (FORC) diagrams for greigite dispersions

First-order reversal curve (FORC) diagrams are used increasingly in geophysics for magnetic domain state identification. The domain state of a magnetic particle is highly sensitive to particle size, about which FORC diagrams provide valuable information. However, the FORC signal of particles with nonuniform magnetisations, which are the main carrier of natural remanent magnetisations in many systems, is still poorly understood. In this study, the properties of non-interacting, randomly oriented dispersions of greigite (Fe3S4) in the uniform single-domain (SD) to non-uniform single-vortex (SV) size range are investigated via micromagnetic calculations. Signals for SD particles () are found to be in excellent agreement with previous SD coherent-rotation studies. A transitional range from to is identified for which a mixture of SD and SV behaviour produces complex FORC diagrams. Particles have purely SV behaviour with the remanent state for all particles in the ensemble in the SV state. It is found that for SV ensembles the FORC diagram provides a map of vortex nucleation and annihilation fields and that the FORC distribution peak should not be interpreted as the coercivity of the sample, but as a vortex annihilation field on the path to saturation

The magnetic structure and palaeomagnetic recording fidelity of sub-micron greigite (Fe3S4)

We present the results of a finite-element micromagnetic model of View the MathML source to View the MathML source greigite (Fe3S4) grains with a variety of equant morphologies. This grain size range covers the magnetic single-domain (SD) to pseudo single-domain (PSD) transition, and possibly also the PSD to multi-domain (MD) transition. The SD–PSD threshold d0 is determined to be View the MathML source depending on grain shape. The nudged elastic-band method was used to determine the room temperature energy barriers between stable states and thus the blocking volumes. It is found that, in the absence of interparticle magnetostatic interactions, the magnetisation of equant SD greigite is not stable on a geological scale and only PSD grains View the MathML source can be expected to carry a stable magnetisation over billion-year timescales, i.e., all non-interacting SD particles are essentially superparamagnetic. We further identify a mechanism for the PSD to multi-domain (MD) transition, which is of a continuous nature from PSD nucleation up to View the MathML source, when structures typical of MD behaviour like closure domains begin to form

Trabajo de titulación previo a la obtención del Título de Psicóloga General

El presente estudio tiene como finalidad investigar la influencia que existe entre el funcionamiento familiar y las habilidades sociales, fundamentado con documentos bibliográficos que expliquen la relación que existe en las dos variables.El funcionamiento familiar se encuentra determinado por características que permite establecer el nivel que se encuentra en función de la familia, mientras que las habilidades sociales son conductas observables desde los inicios de vida del individuo. Para la recolección de la información se contó con la colaboración de 63 estudiantes de los octavos años de educación básica de la Unidad Educativa “Guayaquil”,comprendidos en edades de 12-14 años, a los cuales se les aplico la Escala FF-SIL de funcionamiento familiar y la Escala EHS de habilidades sociales. Una vez aplicadas se realizó la elaboración de los resultados, encontrando que más de la mitad viene de una familia funcional y moderadamente funcional y una pequeña población proviene de una familia disfuncional y severamente disfuncional. En cuanto a las habilidades sociales,cinco de seis factores no predominan, encontrando que el factor de Iniciar Interacciones con el sexo opuesto si predomina, lo que significa que el funcionamiento familiar si influye en el factor de Iniciar Interacciones con el sexo opuesto

Micromag (A micromagnetics code for high performance computing)

This is a micromagnetics code that is specifically designed to be run using high performance computing (HPC) architectures. This code was used to execute models on ARCHER, (www.archer.ac.uk), one of the UK's main supercomputer clusters. It allows modeling magnetic materials up to the micron size scale using a spatial transform technique due to Imhoff et al. and is based on the FEniCS finite element framework.This is a micromagnetics code that is specifically designed to be run using high performance computing (HPC) architectures. This code was used to execute models on ARCHER, (www.archer.ac.uk), one of the UK's main supercomputer clusters. It allows modeling magnetic materials up to the micron size scale using a spatial transform technique due to Imhoff et al. and is based on the FEniCS finite element framework.0.0.

Asymptotics for a C1-version of the KdV Equation

We consider KdV-type equations with nonlinearities u , κ ∈ (1, 5), and small dispersion ε. The first result consists in the conclusion that, in the leading term with respect to ε, the solitary waves in this model interact like KdV solitons. Next it turned out that there exists a very interesting scenario of instability in which the short-wave soliton remains stable whereas a small long-wave part, generated by perturbations of original equation, turns to be unstable, growing and destroying the leading term. At the same time, such perturbation can eliminate the collision of solitons. Numerical simulations confirming the results are also presented

Asymptotics for a C1-version of the KdV Equation

We consider KdV-type equations with nonlinearities u , κ ∈ (1, 5), and small dispersion ε. The first result consists in the conclusion that, in the leading term with respect to ε, the solitary waves in this model interact like KdV solitons. Next it turned out that there exists a very interesting scenario of instability in which the short-wave soliton remains stable whereas a small long-wave part, generated by perturbations of original equation, turns to be unstable, growing and destroying the leading term. At the same time, such perturbation can eliminate the collision of solitons. Numerical simulations confirming the results are also presented

Paleomagnetic field reconstruction from mixtures of titanomagnetites

Stepwise thermal demagnetization and alternating field (AF) demagnetization are commonly used in paleomagnetic studies to isolate remanent magnetic components of different origins. The magnetically hardest, i.e. highest unblocking temperature/peak field component is often interpreted as the primary magnetization and magnetically softer components as subsequent remagnetizations due to geological events posterior to the formation of the rock, such as reheating or formation of new magnetic minerals. The correct interpretation of the sequence of the geological events such as tectonic rotations from paleomagnetic data often relies on correctly attributing the observed magnetic directions to the remanence carriers and acquisition mechanisms. Using a numerical model to simulate remanence acquisition and stepwise thermal and AF demagnetization experiments, we show that the presence of mixtures of different magnetic minerals, such as magnetite and titanomagnetites of varying titanium-content can have very significant effects on Zijderveld plots. In thermal demagnetization experiments a spurious third component at intermediate temperatures or a continuous curvature may arise from an overlap of the primary remanence with a subsequent thermal or viscous remagnetization carried by small-grained iron-rich magnetite and large-grained titanium-rich titanomagnetite. AF demagnetization plots of magnetic mixtures are even more complex: primary and secondary remanences carried by different minerals may appear as either three or four components in Zijderveld plots. During alternating field demagnetization the highest coercivity component is not necessarily equivalent to the primary remanence and does not necessarily correspond to the highest temperature component in an analogous thermal demagnetization experiment, i.e., the primary remanence direction cannot be recovered. The effects are shown to be due to the different responsiveness of magnetite and titanomagnetites towards viscous or thermoviscous remanence acquisition: remanent magnetizations with long acquisition times are more effectively recorded by titanium-poor minerals, while short acquisition times are equally well recorded by titanium-rich minerals. In demagnetization experiments on laboratory timescales, the relative contribution of two minerals to Zijderveld plots differs to the relative contribution of remanence acquisition over geological timescales, leading to overlapping components in Zijderveld plots. The model was also used to simulate paleointensity (ancient magnetic field intensity) experiments and it was found that the grain distribution affects the slope of Arai plots, but is negligible compared to the effect of the cooling rate of NRM acquisition. The simulations suggest that for slowly cooled rocks a cooling rate correction of up to 1.5 to 1.6 may be required depending on the mineralogy