Low-temperature magnetic properties of greigite (Fe3S4)

Liao Chang and Andrew P. RobertsNational Oceanography Centre, University of Southampton, European Way, Southampton SO14 3ZH, UK(chang1@noc.soton.ac.uk)

Christopher J. RowanNational Oceanography Centre, University of Southampton, European Way, Southampton SO14 3ZH, UK

Now at School of Geosciences, University of Edinburgh, Grant Institute, The King’s Buildings, West Mains Road,Edinburgh EH9 3JW, UK

Yan TangHefei National Laboratory for Physical Sciences at Microscale and Department of Materials Science and Engineering,University of Science and Technology of China, Hefei 230026, China

Now at College of Chemical Engineering and Technology, Wuhan University of Science and Technology, Wuhan430081, China

Petr PrunerInstitute of Geology AS CR, v.v.i., Rozvojova 269, CZ-16500 Prague, Czech Republic

Qianwang ChenHefei National Laboratory for Physical Sciences at Microscale and Department of Materials Science and Engineering,University of Science and Technology of China, Hefei 230026, China

Chorng-Shern HorngInstitute of Earth Sciences, Academia Sinica, P.O. Box 1–55, Nankang, Taipei 115, Taiwan

[1] We provide comprehensive low-temperature magnetic results for greigite (Fe3S4) across the spectrumfrom superparamagnetic (SP) to multidomain (MD) behavior. It is well known that greigite has no low-temperature magnetic transitions, but we also document that it has strong domain-state dependence ofmagnetic properties at low temperatures. Blocking of SP grains and increasing thermal stability withdecreasing temperature is apparent in many magnetic measurements. Thermally stable single-domaingreigite undergoes little change in magnetic properties below room temperature. For pseudo-single-domain(PSD)/MD greigite, hysteresis properties and first-order reversal curve diagrams exhibit minor changes atlow temperatures, while remanence continuously demagnetizes because of progressive domain wallunpinning. The low-temperature demagnetization is grain size dependent for PSD/MD greigite, withcoarser grains undergoing larger remanence loss. AC susceptibility measurements indicate consistentblocking temperatures (TB) for all synthetic and natural greigite samples, which are probably associatedwith surficial oxidation. Low-temperature magnetic analysis provides much more information aboutmagnetic mineralogy and domain state than room temperature measurements and enables discrimination ofindividual components within mixed magnetic mineral assemblages. Low-temperature rock magnetometryis therefore a useful tool for studying magnetic mineralogy and granulometry of greigite-bearingsediments.

G3G3GeochemistryGeophysics

Geosystems

Published by AGU and the Geochemical Society

AN ELECTRONIC JOURNAL OF THE EARTH SCIENCES

GeochemistryGeophysics

Geosystems

Article

Volume 10, Number 1

29 January 2009

Q01Y04, doi:10.1029/2008GC002276

ISSN: 1525-2027

Copyright 2009 by the American Geophysical Union 1 of 14

Components: 6868 words, 6 figures.

Keywords: greigite; low-temperature magnetic properties; domain state.

Index Terms: 1540 Geomagnetism and Paleomagnetism: Rock and mineral magnetism; 1512 Geomagnetism and

Paleomagnetism: Environmental magnetism.

Received 9 October 2008; Revised 2 December 2008; Accepted 12 December 2008; Published 29 January 2009.

Chang, L., A. P. Roberts, C. J. Rowan, Y. Tang, P. Pruner, Q. Chen, and C.-S. Horng (2009), Low-temperature magnetic

properties of greigite (Fe3S4), Geochem. Geophys. Geosyst., 10, Q01Y04, doi:10.1029/2008GC002276.

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Theme: Magnetism From Atomic to Planetary Scales: Physical Principles and Interdisciplinary Applications in GeoscienceGuest Editors: J. Feinberg, F. Florindo, B. Moskowitz, and A. Roberts

1. Introduction

[2] Low-temperature (T < 300 K) rock magnetom-etry is widely used in rock magnetism and envi-ronmental magnetism [e.g., Dunlop and Ozdemir,1997; Moskowitz et al., 1998] for magnetic mineralidentification, magnetic granulometry, quantifica-tion of superparamagnetism in ultra-fine-grainednanophases, and detection of magnetic orderingand phase transitions. Low-temperature magneticmeasurements involve thermal dynamic processes,which provide much more information about mag-netic systems than room temperature analysisalone. Compared with high-temperature (T >300 K) measurements, low-temperature methodsalso avoid chemical alteration.

[3] The low-temperature magnetic properties ofmagnetite (Fe3O4) have been extensively studiedbecause of its importance as a terrestrial magneticmineral and because it undergoes the Verweytransition (a crystallographic change from a cubicto a monoclinic superstructure) at �120 K and themagnetic isotropic point (where the magnetocrys-talline anisotropy constant K1 is zero and changessign) at 130 K. In contrast, the magnetic behaviorof the thiospinel counterpart of magnetite, greigite(Fe3S4), which forms in sulfate-reducing sedimen-tary systems [e.g., Berner, 1984], is less wellknown because it was generally considered to bemetastable over geological timescales and thereforerare in natural systems. However, greigite has nowbeen widely identified in marine and lake sedimen-tary sequences [e.g., Snowball and Thompson,1988, 1990; Krs et al., 1990, 1992; Tric et al.,1991; Horng et al., 1992; Roberts and Turner,1993; Reynolds et al., 1994; Florindo andSagnotti, 1995; Housen and Musgrave, 1996;

Roberts et al., 1996; Horng et al., 1998; Sagnottiand Winkler, 1999; Liu et al., 2004; Rowan andRoberts, 2006; Babinszki et al., 2007; Florindo etal., 2007; Frank et al., 2007; Ron et al., 2007;Vasiliev et al., 2007] and it is also produced bymagnetotactic bacteria in anoxic marine environ-ments [e.g., Mann et al., 1990]. Its increasedrecognition has made it more important to under-stand the magnetic properties of greigite. Publishedmagnetic data for greigite have mostly been mea-sured at room temperature or high temperatures,while low-temperature data for greigite consistmainly of saturation isothermal remanent magneti-zation (SIRM) warming curves [Moskowitz et al.,1993; Roberts, 1995; Roberts et al., 1996; Torii etal., 1996; Chang et al., 2007] and a few other typesof low-temperature measurements, e.g., hysteresis[Spender et al., 1972; Roberts, 1995; Dekkers etal., 2000; Chang et al., 2008] and FORC diagrams[Chang et al., 2007]. Compared with high-temperature analysis, low-temperature analysis ofgreigite offers distinct advantages because of com-plications caused by chemical alteration at elevatedtemperatures [e.g., Spender et al., 1972; Krs et al.,1992; Roberts, 1995; Dekkers et al., 2000; Changet al., 2008]. We present comprehensive data for arange of low-temperature measurement techniques,using greigite samples that span the grain sizespectrum from superparamagnetic (SP) to multido-main (MD) behavior.

2. Samples and Methods

[4] We analyzed a range of natural and syntheticgreigite samples. The natural greigite samples arefrom Neogene marine sediments from easternNew Zealand [Rowan and Roberts, 2006]; Plio-Pleistocene marine sediments from the Lower

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Gutingkeng Formation, southwestern Taiwan[Horng et al., 1998; Jiang et al., 2001]; upperPliocene marine sediments from the Valle Riccasection near Rome, Italy [Florindo and Sagnotti,1995; van Dongen et al., 2007]; and Miocenelacustrine sediments from the Czech Republic[Krs et al., 1990]. The New Zealand greigitesamples are from two locations on the MahiaPeninsula, North Island, New Zealand: the ‘‘NR’’samples are from ‘‘Nukutaurua Road,’’ while the‘‘TC’’ samples are from ‘‘Te Waipera Cemetery’’(see Figure 1 of Rowan and Roberts [2006]). TheNew Zealand samples contain mixtures of SP andSingle domain (SD) greigite [Rowan and Roberts,2006]. The samples from Taiwan and Italy containtypical SD greigite. The sample from the CzechRepublic is a mixture of SD and MD greigite[Roberts et al., 2006]. Pure synthetic greigitesamples with dominantly coarse grains (labeled‘‘S’’) were prepared according to the hydrothermalmethod of Tang et al. [2007] by reacting ferricchloride (FeCl3) with thiourea (CH4N2S) and for-mic acid (HCOOH) at 170�C [Chang et al., 2008].The ‘‘S’’ samples with mean grain sizes as large as13 mm have pseudo-single-domain (PSD)/MD be-havior [Chang et al., 2007]. An additional fine-grained synthetic greigite sample (SYN06) wasproduced by solid state transformation of mack-inawite (FeS) to pyrite (FeS2) via the intermediategreigite [Hunger and Benning, 2007]. This syn-thetic sample is dominated by (nonmagnetic)mackinawite but contains nanophase greigite par-ticles (a few tens of nanometers across) [Hungerand Benning, 2007], which exhibit SP behavior atroom temperature [Roberts et al., 2006].

[5] Low-temperature magnetic measurements weremade at the Institute for Rock Magnetism, Univer-sity of Minnesota, USA. Low-temperature hyster-esis loops, back-field demagnetization curves, andFORCs were measured using a Princeton Measure-ments Corporation vibrating sample magnetometer(VSM) with a cryostat. FORC diagrams [Pike etal., 1999; Roberts et al., 2000] were determinedfrom 80 FORCs (averaging time of 200 ms, fieldspacing of 1.85 mT, smoothing factor of 3), usingthe FORCinel software [Harrison and Feinberg,2008]. A Quantum Design magnetic propertiesmeasurement system (MPMS) was used for sus-ceptibility and remanence measurements. For zero-field magnetization (ZFM) measurement, sampleswere cooled to 10 K in zero field. ZFM curveswere recorded in a low field (2 mT) at stepwiseincreasing temperatures to 300 K. Samples werethen cooled to 10 K in a low field (2 mT). Field-

cooled magnetization (FCM) curves were mea-sured in a low field (2 mT) during warming toroom temperature. For zero-field cooled (ZFC) andfield-cooled (FC) SIRM warming, samples werecooled to 10 K in either zero field or a large field(2.5 T). At 10 K, a 5 T field was applied and thenswitched off to impart a low-temperature SIRM.SIRM warming curves were measured duringwarming in zero field. For low-temperature cycling(LTC) of a room temperature SIRM, remanencewas measured from room temperature to 10 K andback to room temperature in zero field. Alternatingcurrent (AC) susceptibility was measured with boththe MPMS system and a Lakeshore Susceptometer.Samples were cooled in zero field to either 4 K or20 K and then measured in a low AC field atseveral frequencies up to 400 K.

3. Results

3.1. Low-Temperature HysteresisProperties

[6] Hysteresis and backfield demagnetizationparameters (Bc, Bcr, Mrs/Ms, and Bcr/Bc, where Bc

is coercivity, Bcr is coercivity of remanence, Mrs issaturation remanent magnetization, and Ms is sat-uration magnetization) for the studied greigitesamples are variable below room temperature(Figure 1). For typical SD greigite from Taiwanand Italy, Bc and Bcr decrease monotonically withwarming. Bcr values are noisy because this param-eter can be difficult to measure. Mrs/Ms alsodecreases monotonically with increasing tempera-ture but less rapidly than Bc and Bcr, and it alwayshas values above 0.5 (Figure 1c). Bcr/Bc is stable atlow temperatures for SD greigite (Figure 1d);values for the Italian greigite sample increase byonly �2% from 20 K to room temperature. Roomtemperature hysteresis parameters for a series ofnatural greigite samples [Snowball, 1997a, 1997b]have similar values to those of our SD greigitesamples measured at 50 K. This probably indicatesthat the greigite samples measured by Snowball[1997a, 1997b] are even more thermally stable thanour stable SD greigite samples.

[7] Hysteresis parameters for coarse-grained syn-thetic greigite samples are nearly temperature in-dependent below room temperature (Figure 1).Chang et al. [2008] observed a local coercivityminimum at �130 K for these samples, which isnot visible at the scale of Figure 1a. The minimumis probably associated with domain wall reaccom-modations in the PSD/MD greigite samples.

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(Figure 1f), which is consistent with the behaviorof sample SYN06 (Figure 1e), and indicates pro-gressive blocking of fine magnetic particles withdecreasing temperature. Bc and Bcr of sampleNR08 decrease rapidly with warming, particularlybelow �100 K (Figures 1a and 1b). Mrs/Ms andBcr/Bc approach SD values at �10 K (Figures 1cand 1d).

[9] Low-temperature hysteresis data for naturalgreigite from the Czech Republic are intermediatebetween those of SD and PSD/MD samples(Figure 1). Bc and Bcr decrease upon warming,with �20% and �23% decreases from 20 K to

room temperature, respectively (Figures 1a and1b). Hysteresis ratios are more stable, with only�5% and �3% increases for Mrs/Ms and Bcr/Bc,respectively (Figures 1c and 1d). These observa-tions are consistent with the conclusion of Robertset al. [2006] that this sample contains a mixture ofSD and MD greigite.

3.2. Low-Temperature FORC Diagrams

[10] Low-temperature FORC diagrams illustratedomain-state characteristics for greigite (Figure 2).FORC distributions indicate high coercivity andstrong magnetostatic interactions for natural SD

Figure 2. FORC diagrams for greigite samples at various temperatures. (a–d) A natural SD greigite sample fromItaly. (e–h) Fine-grained synthetic greigite sample (SYN06) with dominantly SP behavior at room temperature. (i– l)A coarse-grained synthetic greigite sample (S504) with dominantly PSD behavior. (m–p) A natural greigite samplefrom the Czech Republic with a mixture of SD and PSD/MD grains. A smoothing factor (SF) [see Roberts et al.,2000] of 3 was used for all FORC diagrams, except for Figures 2e and 2f for which SF = 5.

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greigite [cf. Roberts et al., 2000, 2006; Rowan andRoberts, 2006; Florindo et al., 2007; Vasiliev et al.,2007], without substantial low temperature varia-tions (Figures 2a–2d). The concentric SD contoursmigrate toward slightly higher coercivities as tem-perature decreases (Figures 2a–2d), as expectedfor progressive blocking of a small fraction of fineparticles [Pike et al., 2001]. Interaction field dis-tributions (Bi) for SD greigite undergo negligiblechanges at low temperatures, unlike SD magnetite[e.g., Carvallo and Muxworthy, 2006].

[11] Although FORC distributions for fine-grainedsynthetic greigite are noisy, they clearly migrate tohigher coercivities at low temperatures (Figures 2e–2h), which confirms the dominantly SP behavior atroom temperature for sample SYN06 [Roberts et al.,2006]. This behavior is consistent with models [Pikeet al., 2001] and with low-temperature observationsfor samples with dominantly SP behavior [e.g.,Carvallo and Muxworthy, 2006].

[12] FORC distributions for PSD/MD greigite sam-ples are unchanged at low temperatures(Figures 2i–2l) [Chang et al., 2007], as expectedfor MD assemblages. This contrasts with PSDmagnetite, where FORC distributions split intotwo sets of concentric contours at low temperatures[e.g., Carvallo and Muxworthy, 2006; Smirnov,2006]. The splitting is probably associated withinduced anisotropy effects [Smirnov, 2006], whichdo not appear to be present for greigite.

[13] Low-temperature FORC diagrams for theCzech sample indicate mixed SD and PSD/MDbehavior, as suggested by Roberts et al. [2006].Migration of the concentric peak to higher coer-civities at low temperature indicates SD behaviorwith minor thermal relaxation, while the divergentouter contours indicate the presence of PSD/MDgrains (Figures 2m–2p).

3.3. Low-Temperature ZFM/FCM

[14] When cooled in zero magnetic field, the mag-netic moments of fine particles are randomly ori-ented. When subsequently warmed in a weak fieldfrom low temperature, magnetic moments of therandomly oriented particles become progressivelyaligned with the field due to increasing thermalenergy. Maximum susceptibility (where magneticmoments are maximally aligned with the field) isobserved at the blocking temperature (TB). AboveTB, susceptibility decreases as thermal energy grad-ually randomizes the aligned magnetic moments[Dormann et al., 1997].

[15] A ZFM curve for sample SYN06 rapidlyincreases upon warming (Figure 3a), which indi-cates progressive alignment of magnetic momentswith the weak field. The rapid increase over thewhole temperature range probably indicates abroad grain size distribution. Although the meanTB is above room temperature, there is significantSP behavior at room temperature. ZFM/FCMcurves for some New Zealand greigite samplesindicate large paramagnetic contributions, as indi-cated in a plot of inverse susceptibility (Figure 3b),which completely swamp ferrimagnetic greigitesignals. After magnetic separation, sample NR08has a dominant ferrimagnetic signal: the magneti-zation increases sharply from low temperature upto 120 K and decreases sharply from 270 K toroom temperature with a broad plateau between120 K and 270 K (Figure 3c). By removing theparamagnetic susceptibility (from hysteresis loops;insert in Figure 3d), ZFM/FCM curves can beproduced that represent the ferrimagnetic signal.For sample NR27, which is dominated by SPbehavior at room temperature, a peak at �120 Kin the ZFM curve (Figure 3d) indicates the mean TB.

3.4. Low-Temperature AC Susceptibility

[16] c (T, f) curves (where T and f are temperatureand frequency, respectively) for SD greigite in-crease slightly during warming (Figure 4a), whichsuggests that the mean TB is above room temper-ature. However, both the real c0 (T, f) and imagi-nary c00 (T, f) components have frequency-dependent properties, which indicates the presenceof some SP behavior (Figures 4a and 4d). A TBbetween 6 K and 20 K is detected in the c00 (T, f)curve (Figure 4d). Coarse-grained synthetic grei-gite samples undergo small susceptibility varia-tions at low temperatures (Figure 4b), although alocal susceptibility maximum was observed be-tween 100 K and 110 K (Figure 4b). This maxi-mum does not likely represent a TB because it doesnot display frequency dependence and because it isnot detected in the c00 (T, f) curve at this temper-ature (Figures 4b and 4e). This local susceptibilitymaximum is therefore probably an intrinsic prop-erty of PSD/MD greigite. Chang et al. [2008]observed a local coercivity minimum for the samesamples at �130 K, but it is not clear if theseproperties are related. SP behavior (with a TBbetween 8 K and 20 K) is indicated in the c0 (T, f)and c00 (T, f) curves with strong frequency depen-dence. The observed TB below 20 K for bothsynthetic and natural greigite samples (Figures 4d,4e, and 4f) probably has a similar origin. Chang et

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al. [2008] observed a magnetically ordered phasein synthetic greigite samples at 4 K fromMossbauerspectroscopy, which they attributed to slight surfi-cial oxidation of greigite particles, which may beassociated with the observed TB below 20 K. Thisinterpretation is supported by transmission electronmicroscope (TEM) observations of surfical oxida-tion on fine greigite grains [Letard et al., 2005;Kasama et al., 2006]. The c0 (T, f) curves for

natural greigite-bearing sediments from New Zea-land rapidly decrease upon warming (Figures 4g–4i), which indicates substantial paramagnetism.Weak ferrimagnetic greigite signals are often there-fore swamped by paramagnetism. However, mea-surement of a magnetic separate (sample NR08)indicates characteristic frequency-dependent sus-ceptibility that is associated with SP behavior(Figures 4c and 4f).

Figure 3.(a– d) ZFM/FCM curves for greigite samples in a smal l field (2 mT). The inserts in Figures 3b and 3d areinverse ZFM curves that indicate dominant parama gnetism across the whole temperature range. (d) ZFM/FCM curvesfora greigit e-bearingsediment samplefrom New Zealand (sampleNR27 ) after removingthe paramagneticmagnetiza tion, which was calculated from high-fieldmagnetizationmeasurements (insert). See textfor detaileddescription.Figure 4.(a– f) The AC susceptibility for three greigite samples with SP/SD , PSD/MD, and SP properties duringwarm ing. The insert in Figure 4b is an expanded view of the main susceptibilitycurve s. (g– i) The measured AC

susceptibili ty (real compo nentcÂ(T,f))fornaturalgreigitesamplesfromeasternNewZealand.(j–l)TheinverseAC susceptibilityforthesamesamplesinFigures4g–4i.Linesarelinearfitsto cÃ1=

AÄT(where cand Taresusceptibilityandtemperature,respectively; Aisacoefficient)forT<50K,whichrepresentparamagnetic signals.Themeasuredsusceptibilitydatadeviatefromlinearityatelevatedtemperatures,whichindicatesthe increasingdominanceofferrimagneticsignalsandarapidlydecreasinginfluenceofparamagneticsusceptibilitywith increasingtemperature.(m–o)Susceptibilitycurvesaftersubtractionofthefittedparamagneticsusceptibilityfrom themeasuredsusceptibilityforgreigitesamplesinFigures4g–4i.Thesecurvesrepresentferrimagneticgreigite signalswithvariablegrainsizedistributions.Seetextfordetaileddescription.SamplesinFigures4a–4fandFigures 4g–4oweremeasuredwithaMPMSandLakeshoreSusceptometer,respectively. G e o c h e m i s t r yG e o p h y s i c sG e o s y s t e m sG3G3

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[17] To remove the dominating effect of paramag-netic signals from matrix minerals, we linearlyfitted the temperature-dependent paramagneticAC suscept ibi l i ty for T < 50 K to 1/T(Figures 4j–4l). We subtracted this paramagneticsusceptibility from the measured susceptibility toobtain the ferrimagnetic signal (Figures 4m–4o).Sample NR15 has a clear peak at �180 K(Figure 4m). The imaginary component c00 (T, f)for this sample also has peaks at this temperature,which confirms a TB of �180 K. For samples TC15and TC29, the ferrimagnetic susceptibility increasesrapidly up to 190 and 120 K, respectively, and isfollowed by nearly stable susceptibility up to roomtemperature (Figures 4n and 4o). These temperatures

probably indicate the TB for the SP component of thesamples with a broader superposed grain size distri-bution that includes a stable SD component.

3.5. Low-Temperature Remanence

[18] Cooling conditions (ZFC or FC) have noeffect on SIRM warming of greigite because thereis no low-temperature transition for greigite[Moskowitz et al., 1993; Chang et al., 2007]. Wetherefore only show FC SIRM warming curves inFigure 5. SIRM warming curves for samples dom-inated by SD greigite undergo minor decreaseswith warming (Figures 5a and 5b), which agreeswith the results of Roberts [1995]. SIRM decreasesby 23% and 30% from 20 to 300 K for the SD

Figure 5. (a–i) SIRM warming curves for greigite samples. Solid points represent measured data. Dashed lines arethe first derivative of the SIRM with respect to temperature (dM/dT). The SIRM was imparted in a 5 T field at 10 K.TV represents the Verwey transition for magnetite. The insert in Figure 5d is the correlation between coercivity andremaining remanence after zero-field SIRM warming from 10 K to 300 K for a range of synthetic PSD/MD greigitesamples.

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greigite samples from Italy and Taiwan, respective-ly, which indicates different SP contributions. TheCzech sample has similar behavior to a previouslyreported sample from this locality (Figure 5c)[Moskowitz et al., 1993; Roberts, 1995]. The SIRMfor synthetic sample S706 (mean grain size of�8 mm) decreases by 34% from 20 to 300 K(Figure 5d), which is larger than the SIRM de-crease (28%) for synthetic PSD sample S504 withsmaller mean grain size (<4 mm; grain sizes are

reported by Chang et al. [2007]). Low-temperatureSIRM warming curves for a range of coarse-grained synthetic greigite samples confirm thatthe remanence drop correlates with coercivity (in-sert in Figure 5d), which is a sensitive indicator ofgrain size for PSD/MD greigite [e.g., Chang et al.,2007]. Our results therefore indicate that low-temperature SIRM warming curves are grain-sizedependent for PSD/MD greigite. Coarser-grainedgreigite undergoes larger remanence loss duringwarming, although unblocking due to minor SPparticles will also contribute to remanence loss.

[19] Our fine-grained synthetic greigite sample hascomplex SIRM warming behavior (Figure 5e). Theabrupt remanence decrease from 10 to 20 K isprobably due to impurities, such as an oxidizedsurface layer, e.g., iron oxide or hydroxide [Letardet al., 2005; Kasama et al., 2006]. TEM observa-tions indicate that this sample contains extremelyfine greigite grains [Hunger and Benning, 2007].Therefore, surface oxidation could have a signifi-cant effect on the magnetic properties. The largeremanence drop between 20 K and 230 K is likelydue to unblocking of fine greigite particles. Therelatively small decrease from 230 K to roomtemperature is probably due to an additional grainsize distribution (i.e., there are bimodal and over-lapping grain size distributions). The remainingremanence at room temperature is carried by SDgrains, which is consistent with ZFM/FCM meas-urements that indicate a mixture of SP/SD grains.SIRM warming curves for the New Zealand grei-gite samples abruptly decrease between 20 and300 K (Figures 5f–5i). First derivatives of SIRMwarming curves indicate the presence of minormagnetite in the greigite-dominated TC samples(Figures 5g–5i), which is likely to be from detritaltuffaceous material that was not dissolved duringreductive diagenesis [Rowan and Roberts, 2006].Magnetite, even when present in small concentra-tions, can be detected by low-temperature magneticmeasurements because of the effect of the Verweytransition. Regardless, trace amounts of magnetitedo not significantly affect our conclusions.

[20] Finally, LTC measurements of a RT-SIRM fora natural SD greigite sample and for a range ofcoarse-grained synthetic samples resemble theresults of Chang et al. [2007], which indicatecontrasting behavior for SD and PSD/MD samples(Figure 6a). SP particles make no contribution toremanence, so they are not relevant to LTC of RT-SIRM measurements. For SD greigite (from Tai-wan), the remanence increases slightly due to

Figure 6. (a) Normalized zero-field cooling andwarming of a RT-SIRM for a representative range ofgreigite samples that span the grain size range from SDand to PSD/MD. (b) The correlation between coercivityand remaining remanence after zero-field LTC of RT-SIRM for a range of synthetic PSD/MD greigitesamples. Mean grain sizes for the synthetic coarse-grained greigite samples S504, S510, S630, and S706are �4 mm, �9 mm, �11 mm, and �8 mm, respectively[cf. Chang et al., 2007].

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decreased thermal energy upon cooling [Dekkers etal., 2000; Chang et al., 2007]. The remanencememory is nearly complete when warmed back toroom temperature. In contrast, PSD/MD greigitedemagnetizes during cooling and the warmingcurve is irreversible with respect to the coolingcurve [Chang et al., 2007]. Measurements oncoarse-grained synthetic greigite samples indicatethat the remanence memory after LTC is stronglycorrelated to Bc, which, in turn, is dependent ongrain size (Figure 6b). LTC of a RT-SIRM there-fore provides a useful tool for magnetic granulom-etry by enabling discrimination between SD andPSD/MD grains.

4. Discussion

[21] Comprehensive low-temperature magneticmeasurements of SP to MD greigite consistentlyprovide no evidence of a low-temperature transi-tion. This confirms previous observations [e.g.,Coey et al., 1970; Spender et al., 1972; Moskowitzet al., 1993; Roberts, 1995; Torii et al., 1996;Dekkers et al., 2000; Chang et al., 2007, 2008].There is also no evidence for a low-temperaturephase transition from structural investigations fromeither Mossbauer spectroscopy [Vandenberghe etal., 1991; Chang et al., 2008]. Greigite probablyalso has no low-temperature magnetic isotropicpoint. Low-temperature SIRM warming curveshave been used to discriminate greigite from othermagnetic minerals with low-temperature magnetictransitions, e.g., magnetite and pyrrhotite (Fe7S8)[e.g., Moskowitz et al., 1993; Roberts, 1995;Housen and Musgrave, 1996; Roberts et al.,1996; Torii et al., 1996; Horng et al., 1998; Jianget al., 2001; Babinszki et al., 2007]. However, itshould be noted that the absence of a magnetictransition does not enable positive identification ofgreigite. Additional analyses, e.g., X-ray diffrac-tion and scanning electron microscope observa-tions, are needed to enable unambiguous detection.

[22] At room temperature, hysteresis parametersfor greigite-bearing sediments from eastern NewZealand [Rowan and Roberts, 2006] fall on asimilar trend to SP/SD mixing lines calculated formagnetite [Dunlop, 2002]. Representative hystere-sis loops are slightly wasp-waisted (Figure 1f)[Rowan and Roberts, 2006], which is consistentwith the presence of SP/SD mixtures [Roberts etal., 1995]. The dominantly SP greigite samplesundergo the most rapid low-temperature change inmagnetic properties. Low-temperature hysteresismeasurements, along with ZFM/FCM and low-

temperature AC susceptibility curves, also confirmthe dominance of SP behavior in these sediments.Variations in the observed TB reveal fine butvariable grain size distributions. SP behavior isalso present in samples dominated by SD greigite(e.g., Bc decreases by �28% and �44%, whileSIRM decreases by 23% and 30% from 20 to 300 Kfor the natural greigite samples from Italy andTaiwan, respectively). These low-temperatureobservations are consistent with room temperaturehysteresis measurements, where the Italian samplehas a larger Bc value than the sample from Taiwan(50 versus 44 mT). The different decreases prob-ably reflect different SP contributions. SP behaviorin greigite-bearing sediments is unsurprising con-sidering that greigite progressively grows fromsolution to a finite grain size, which favors forma-tion of ultrafine particles [Rowan and Roberts,2006]. Progressive blocking during cooling tolow temperatures means that Bc, Bcr, and Mrs/Ms

increase rapidly where SP behavior dominates,while Bcr/Bc decreases rapidly with decreasingtemperature [cf. Coey et al., 1970; Spender et al.,1972; Dekkers et al., 2000]. Concentric FORCcontours move rapidly to higher coercivities.ZFM/FCM and AC susceptibility curves for dom-inantly SP samples have characteristic maxima thatcorrespond to the mean TB of the fine greigiteparticles. Low-temperature SIRM also decreasesrapidly during warming [cf. Roberts, 1995; Changet al., 2007].

[23] SD greigite has relatively stable magneticproperties at low temperatures. Hysteresis parame-ters undergo only small changes, with slightlyincreasing Bc, Bcr, and Mrs/Ms and decreasingBcr/Bc during cooling. FORC diagrams indicate aminor migration of the SD distribution towardhigher coercivities with decreasing temperature,but these changes are much smaller than fordominantly SP samples. ZFM and AC susceptibil-ity increases slightly during warming. SIRMdecreases slightly from low to room temperature[cf. Roberts, 1995; Chang et al., 2007]. Zero-fieldcycling of RT-SIRM indicates a small increaseduring cooling, with nearly reversible warmingcurves [e.g., Chang et al., 2007].

[24] Temperature dependence of magnetic proper-ties for PSD/MD greigite is mainly controlled bydomain wall movements. Magnetization (hystere-sis, FORC, ZFM/FCM, AC susceptibility) is usu-ally stable, while remanence (warming, zero-fieldcycling) is unstable. He et al. [2006] observed low-temperature magnetization jumps in ZFM curves

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for a synthetic greigite microrod, which they at-tributed to domain wall pinning effects. We did notobserve such behavior, probably because of acomparatively low magnetic anisotropy for ourmore equant PSD/MD greigite samples [Chang etal., 2008]. By contrast, the remanence is demag-netized in our samples at low temperatures asdomain walls become progressively unpinned.Low-temperature demagnetization of SIRM forPSD/MD grains is associated with domain wallunpinning [e.g., Moskowitz et al., 1998]. Low-temperature SIRM warming curves vary with grainsize for PSD/MD greigite: coarser-grained greigiteundergoes larger demagnetization. More MD-likegreigite can lose significant remanence, whichcould be misinterpreted as SP behavior. Comple-mentary measurements are therefore needed toresolve such ambiguities. Zero-field cycling ofRT-SIRM causes significant demagnetization dur-ing cooling, and warming curves are not reversiblewith respect to cooling curves [Chang et al., 2007].This irreversible demagnetization is probably as-sociated with domain reordering, i.e., domain wallreequilibration or domain nucleation due totemperature-dependent changes in magnetocrystal-line anisotropy and transdomain processes [Changet al., 2007], similar to cooling processes that causeremanence decreases in PSD/MD magnetite abovethe Verwey transition [Muxworthy et al., 2003].

5. Conclusions

[25] Greigite undergoes no low-temperature transi-tion and it probably has no magnetic isotropicpoint. Low-temperature measurements indicatestrong domain-state dependence of magnetic prop-erties for greigite. SP behavior produces majorchanges in low-temperature measurements. SPgreigite is widespread in greigite-bearing sedi-ments, even in typical SD natural greigite samples,and can be detected despite large SD or PSD/MDbackground signals using SIRM warming, ZFM/FCM curves, and AC susceptibility. A TB below20 K was consistently observed in our greigitesamples by AC susceptibility measurements, whichwe attribute to minor surface oxidation of greigitegrains. SD greigite has relatively stable magneticproperties; coercivity increases slightly as thermallyrelaxed grains magnetically block at low tempera-ture. For PSD/MD greigite, hysteresis properties,FORC diagrams, ZFM/FCM curves, and AC sus-ceptibility are stable, while remanence demagnet-izes significantly due to domain wall unpinning.MD greigite can undergo significant remanence

loss during warming, which can be misinterpretedas SP behavior. Complementary measurements aretherefore needed to resolve this potential ambigu-ity. Low-temperature magnetic measurements havethe potential to unravel contributions from eithermineral mixtures or mixed domain states, whichprovides much more information than room tem-perature measurements. Low-temperature rockmagnetometry can therefore be widely useful forstudying magnetic mineralogy and granulometry ofgreigite-bearing materials.

Acknowledgments

[26] Liao Chang is supported by a Dorothy Hodgkin Post-

graduate Award, funded by Hutchison Whampoa Limited and

the U.K. Natural Environment Research Council. We thank

T. Berquo, A. Muxworthy, and Q. S. Liu for discussions and

Bruce Moskowitz, Ian Snowball, and Mark Dekkers for

helpful reviews of the manuscript. Funding for sampling in

the Czech Republic was partly provided from the Institutional

Research Plan of the GLI AS CR, v.v.i. CEZ AV0Z30130516.

The Institute for Rock Magnetism, which is funded by the

National Science Foundation, the Keck Foundation, and the

University of Minnesota, provided two visiting fellowships

that enabled the low-temperature measurements. Mike Jack-

son, Julie Bowles, Peat Sølheid, Brian Carter-Stiglitz, and

Amy Chen helped with measurements.

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