Rock magnetic and AMS fabrics characterization of suevitic breccias from the Cretaceous-Paleogene Chicxulub impact crater

Caracterizacion de propiedades magneticas y anisotropia de susceptibilidad magnetica de las brechas sueviticas del crater Cretacico-Paleogeno Chicxulub

Margarita Delgadillo-Peralta, Jaime Urrutia-Fucugauchi*, Ligia Pérez-Cruz, and Miriam Velasco-Villarreal

Programa Universitario de Perforaciones en Océanos y Continentes, Laboratorio de Paleomagnetismo y Paleoambientes, Instituto de Geofísica, Universidad Nacional Autónoma de México, Coyoacán 04510 México D.F., Mexico. *juf@geofisica.unam.mx

Manuscript received: May 4, 2014
Corrected manuscript received: January 23, 2014
Manuscript accepted: January 28, 2015

ABSTRACT

Results of a paleomagnetic and magnetic fabrics study of the basal suevitic breccias in the Chicxulub impact crater, Yucatán platform, Gulf of Mexico are presented. The breccias were cored in the Yaxcopoil-1 borehole, which is located at about 62 km radial distance from the crater center. The impactite sequence in the Yaxcopoil-1 borehole is ~100 m thick and formed by six subunits with distinct petrographic and geochemical characteristics. Here we investigate the basal subunit interpreted as: a ground surge in the transient cavity, a melt breccia with clastic material, or an excavation flow from the ejecta curtain interacting with the ejecta plume collapse. Characterization of the magnetic fabrics using rock magnetics and anisotropy of magnetic susceptibility (AMS) are used to investigate on the emplacement mechanism of the suevites. Magnetic hysteresis and k-T curves show that the magnetic mineralogy is dominated by low-Ti titanomagnetites and magnetite. The AMS fabrics record mixtures of oblate and prolate ellipsoids and principal susceptibility axial distributions with relatively high angular scatter, related to turbulent high temperature conditions during ejecta emplacement. Magnetic fabric parameters and principal susceptibility axial distributions correlate with modal composition, relative contents and orientation of melt particles. Results are interpreted in terms of an emplacement mode as an early excavation flow that incorporated ground surge components.

Key words: anisotropy of magnetic susceptibility; suevite; ejecta emplacement; Yaxcopoil-1 borehole; Chicxulub crater.

RESUMEN

Palabras clave: anisotropía de susceptibilidad magnética; suevitas; emplazamiento de eyecta; pozo Yaxcopoil-1; cráter Chicxulub.

INTRODUCTION

Chicxulub crater is a large ~200 km diameter multi-ring structure formed 66 Ma ago by a bolide impact in the southern Gulf of Mexico (Hildebrand et al., 1991, 1998; Sharpton et al., 1992; Schulte et al., 2010; Urrutia-Fucugauchi et al., 2011). Following formation, the crater was covered by carbonate sediments and now lies buried in the Yucatán carbonate platform. The crater preserves the ejecta deposits that have been drilled within the Chicxulub Scientific Drilling Program. The Yaxcopoil-1 borehole was drilled inside the crater in the southern sector, some 62 km away from the crater center (Urrutia-Fucugauchi et al., 2004a). The impactite sequence is formed by ~100 m of melt-rich and carbonate-rich breccias with basement, melt and sedimentary clasts. High contrasts in physical properties have been documented between the carbonates, crystalline basement and melt (Urrutia-Fucugauchi et al., 2004b). Petrologic, textural, mineralogical and chemical analyses indicate that the breccias sequence is formed by distinct subunits, with varying characteristics in matrix and clast contents and composition (Stöffler et al., 2004, Kring et al., 2004; Tuchscherer et al., 2006). The breccias subunits have been interpreted in terms of their origin, emplacement mode and post-impact alteration effects (Wittmann et al., 2007).

The grain sizes, texture and composition of matrix and clasts are investigated and characterized by petrographic, geochemical and paleomagnetic studies (Urrutia-Fucugauchi et al., 1996, 2004b). Logs of low-field magnetic susceptibility along the core provide information on relative distribution of carbonate and melt and basement components. Development of models proposed for emplacement of impact breccias is complicated by the high-energy and high-temperature environment, lack of observational evidence, and difficulty of scaling laboratory experiments.

In this paper, we present initial results of a rock magnetic and fabrics study of the basal carbonate-rich breccias from the sequence, recovered in the Yaxcopoil-1 borehole (Figure 1). The study forms part of the core documentation of mineralogical, chemical and physical properties and aims to characterize the magnetic properties. Further interest in analyzing the basal deposits focuses on investigating the emplacement mechanisms and crater collapse. Emplacement of the basal ejecta may involve components from the ejecta curtain and plume in the early stages, with a characteristic fabrics possibly resolvable by magnetic methods. Anisotropy of magnetic susceptibility (AMS) and rock magnetic properties have been used in studying ignimbrites and basal surge deposits and seem suited for investigating and characterizing the impact breccias.

Chicxulub Crater

The Chicxulub impact crater was first identified from the gravity and magnetic anomaly surveys conducted as part of the oil exploration programs of Petróleos Mexicanos in the Yucatán peninsula (Penfield and Camargo-Zanoguera, 1981). The Chicxulub impact has been related to the mass extinction and global environmental events marking the Cretaceous-Paleogene (K/Pg) boundary, and represents a major catastrophic event in the Phanerozoic (Hildebrand et al., 1991, 1998; Schulte et al., 2010). Complex multi-ring and peak-ring impact craters are formed by one of the most energetic phenomena in the geological record (Melosh, 1989). Chicxulub is one of only three large multi-ring basins documented in our planet (Collins et al., 2008; Urrutia-Fucugauchi and Pérez-Cruz, 2009; Schulte et al., 2010). The impact occurred in a shallow extensive carbonate platform in the southern sector of the proto-Gulf of Mexico; the crust was deformed, fragmented and pushed downwards to excavate a cavity some 25 km deep, which collapsed to form a multi-ring basin with a central uplift and inner peak-ring (Hildebrand et al., 1998; Ortiz-Alemán and Urrutia-Fucugauchi, 2010; Collins et al., 2008).

Initial rock magnetic studies in core samples from the UNAM boreholes Santa Elena, Peto and Tekax distinguished two distinct breccias sequences (Urrutia-Fucugauchi et al., 1996). An upper sequence rich in basement clasts and melt fragments and a lower sequence rich in carbonate clasts, which are similar to the suevitic breccias and Bunte breccias documented in the Ries crater, Germany (Newsom et al., 1986; Engelhardt et al., 1995; Osinski et al., 2004; Meyer et al., 2011). Further, magnetic susceptibility data appeared to provide a simple proxy for the distribution and relative content of basement and melt material within the breccias. For instance, data for the upper breccia unit in UNAM-7 borehole show a trend of high susceptibility values towards the bottom of the unit, suggesting an increasing content of ferromagnetic minerals varying with depth. Susceptibility data could also be used for lateral correlation of the ejecta sequence, modeling of magnetic anomalies and study of hydrothermal activity. Hydrothermal post-impact alteration processes have affected the breccia sequence, which are reflected in the magnetic mineralogy (Urrutia-Fucugauchi et al., 2004b; Pilkington et al., 2004). Paleomagnetic analyses of melt and breccia samples collected from the Yucatán-1 borehole showed the occurrence of a stable remanent magnetization with an upward inclination of about 40°, which is consistent with the expected magnetic polarity at the time of the impact (Urrutia-Fucugauchi et al., 1994). The K/Pg boundary occurs within the upper half of reverse polarity C29r chron, consistent with the 38Ar/39Ar dates reported for melt samples from the Chicxulub-1 borehole. The age of impact and the correlation with the K/Pg boundary has been analyzed and discussed in several works (e.g., Schulte et al., 2010). In the boreholes drilled in the crater area, the stratigraphy of the impactites and basal carbonate sequence is being examined to constrain the sequence of events and analyze the impact effects at local and global scales. Recent studies in the Santa Elena borehole using stable isotope and magnetic polarity stratigraphy documents the occurrence of a short hiatus following crater formation (Urrutia-Fucugauchi and Pérez-Cruz, 2008).

Magnetic susceptibility logs on the Yaxcopoil-1 cores shows a complex heterogeneous assemblage of paramagnetic, diamagnetic and ferrimagnetic minerals in the melt, basement and carbonate clasts melt and matrix (Figure 2; Urrutia-Fucugauchi et al., 2004b; Pilkington et al., 2004). The magnetic polarity stratigraphy documents that the normal to reverse C29r to C29n polarity transition lies within the basal carbonates in the first 50 cm interval above the breccias contact (Rebolledo-Vieyra and Urrutia-Fucugauchi, 2004). The polarity transition is consistent with the impact occurring within C29r chron.

Yaxcopoil-1 Breccia Sequence

An INDECO rotary drill equipped with a top-drive coring device were used for the drilling/coring operations. Rotary mode was employed from the surface to 404 m in depth. This interval was logged and cased. From 404 m to 1511 m, continuous wireline coring was used, which permitted to sample the complete sequence. Cores 63.5 mm diameter were obtained to a depth of 993 m, and cores 47.6 mm diameter to final depth. Yaxcopoil-1 borehole sampled the Paleogene carbonate sequence, impact breccias and overlying Cretaceous carbonates. Core recovery was 98.5 %. Cores were marked, digitally scanned and described. After completion of drilling, cores were packed and shipped to our UNAM Core Repository in Mexico City. Cores were further examined and then cut longitudinally in halves, which were again digitally scanned for high-resolution imaging (Urrutia-Fucugauchi et al., 2004a, 2004b).

The breccia sequence in the Yaxcopoil-1 borehole occurs from about 794.63 m to 894.94 m in depth; the 100 m thick breccias have been divided into six subunits (Stöffler et al., 2004; Kring et al., 2004). From top to bottom subunits have been named as: (1) USS Upper Sorted Suevite (794-808 m), (2) LSS Lower Sorted Suevite (808-823 m), (3) US Upper Suevite (823-846 m), (4) MS Middle Suevite ((846-861 m), (5) BMR Brecciated Impact Melt Rock (861-885 m) and (6) LS Lower Suevite (885-895 m) (Figure 1).

The LS subunit is a variegated polymictic allogenic clast melt breccia, distinguished from the other subunits for its relative abundance, type and size of clasts, mainly composed of carbonates (Figure 3). Stöffler et al. (2004) described intervals formed by agglomerates of large rounded carbonates mixed with polymictic breccias with abundant melt particles, suggesting they could represent carbonate melts. The fine grained fractions are poor in lithics and rare silicate melt clasts. The LS subunit was emplaced in the early cratering stages and has been interpreted in terms of emplacement from the ejecta curtain, as a ground surge in the transient cavity, a melt breccia with clastic material and as an excavation flow with interaction with the ejecta plume (Kring et al., 2004; Stöffler et al., 2004; Tuchscherer et al., 2006; Wittmann et al., 2007).

For the paleomagnetic and AMS fabrics study, sampling was completed for the basal LS subunit of suevitic breccias, with twenty four 2.3 cm cubic samples cut between 885 m and 895 m in depth. For the magnetic hysteresis and thermomagnetic analyses, thirty additional samples were collected.

The low-field magnetic susceptibility of samples was measured using the Bartington MS2 susceptibility instrument with the dual frequency laboratory sensor. Magnetic susceptibility is in the range 0–2000 × 10^-6SI, with higher values up to 6500 × 10^-6SI (Figure 2c). The intensity and direction of natural remanent magnetization (NRM) were measured using a spinner JR6 magnetometer. NRM intensity shows a similar pattern to that observed in the susceptibility logs, with values in the range 0 to 100 mA/m, with a peak of about 550 mA/m (Figure 2b). The breccias are characterized by their heterogeneous nature, composed of melt particles and lithic fragments. The LS suevites contain mainly clasts of carbonate target rocks and few basement clasts. The NRM intensity and susceptibility logs show a peak, which corresponds to a basement clast. Low values characterize the suevite, indicating the dominance of carbonate lithics.

Magnetic mineralogy was further investigated by determining magnetic hysteresis properties and the variation of magnetic susceptibility with increasing temperature. Hysteresis loops were measured with a MicroMag system on small-sized microgram samples. Hysteresis loops and direct-field isothermal remanent magnetization (IRM) acquisition and back-field demagnetization show occurrence of low coercivity minerals (Figure 4a), possibly fine-grained magnetite and titanomagnetites.

Magnetic domain states are estimated from analysis of the ratios of hysteresis parameters (Ms, Mr, Hc, and Hcr) using the ratio plots of magnetization ratio (Mr/Ms) as a function of coercivity (Hc) (Day et al., 1977; Dunlop, 2002). Hysteresis parameter ratios allow identification of domain states, with single domain (SD), pseudo-single domain (PSD) and multi-domain (MD) states. The analyzed samples are characterized by low magnetization and coercivity ratios, which plot in the PSD sector (Figure 4b).

The variation of magnetic susceptibility with increasing temperature was measured with the Bartington high temperature system. Heating and cooling curves were recorded from room temperature up to 600–700 °C. The heating and cooling curves show an irreversible behavior marking relatively infrequent magnetic mineral alteration with temperature as compared to the more frequent observed case with higher susceptibilities in the cooling curves (e.g., Hrouda, 2003; Hrouda et al., 2003). The cooling curves fall below the heating curves, indicating dissolving titanomagnetite lamellae in less magnetic host minerals as a result of temperature alteration (Figure 5). In some of the experiments, noisy curves were measured due to the weak magnetic susceptibilities of the carbonate lithics. Curie temperatures of around 520 to 575 °C, indicative of low-Ti titanomagnetites, were determined.

AMS tensor was measured with a Kappabridge KLY-2. Data are analyzed in terms of the magnitudes and orientation of the principal susceptibility axes and the AMS parameters. Low magnitude magnetic fields applied to isotropic materials result in induced magnetizations that depend on the susceptibility of the material. In anisotropic materials, the induced magnetization is not parallel to the applied field and the angular deflection depends on the anisotropy degree. In anisotropic materials, susceptibility is represented by a second-rank tensor whose principal orthogonal axes are the maximum (K₁), intermediate (K₂) and minimum (K₃) principal susceptibilities (Tarling and Hrouda, 1993).

The relations among the magnitudes of principal susceptibilities are used to quantify the anisotropy degree (P' parameter) and shape of susceptibility ellipsoid (T shape parameter) (Jelinek, 1981; Tarling and Hrouda, 1993). Magnitude and shape of susceptibility ellipsoid are determined from the shape parameter and the anisotropy degree. T-P' plots permit distinction of susceptibility ellipsoid, with prolate, oblate and triaxial (neutral) ellipsoids. Oblate ellipsoids show positive T values and predominantly foliated ellipsoids. Prolate ellipsoids show negative T values and predominantly lineated ellipsoids.

The Lower Suevite is characterized by mixed prolate and oblate shaped ellipsoids. Plot of shape, T, parameter as a function of the anisotropy degree, P' (Figure 6a), shows that prolate and oblate fabrics occur at low and high anisotropy degrees. In the graph, some samples show T values close to zero, which are arbitrarily marked with the discontinuous lines. This range in T parameters gives four apparent groups, which are discussed further below. The principal susceptibility axis distributions in equal-area stereographic plots show angular distributions corresponding to Fisherian, girdle and scattered distributions (Figure 6b). Prolate and oblate fabrics are distinguished with different symbols. The maximum K₁ principal axes vary from horizontal to near-vertical. In the sterograms, it can be noted that the principal axes show apparent groupings of oblate and prolate fabrics. The minimum K₃ principal axes range from shallow inclinations to vertical. Although the core was not azimuthally oriented, core segments were kept with orientation marks for the 3 m long core barrels used in the drilling/coring operations. LS subunit is characterized by mixed fabrics, with oblate and prolate shaped ellipsoids with horizontal, intermediate and near vertical axial orientations.

The AMS parameters are plotted as a function of depth, to investigate on the fabric variations along the breccia subunit (Figure 7). The mixed fabrics, with prolate and oblate shape ellipsoids are observed along the breccias interval. Marked lineated fabrics are present at three intervals, with lineated prolate ellipsoids at ~889.5 m. Foliated fabrics are observed at 889.5 m and 886 m, corresponding to high anisotropy degrees.

DISCUSSION

The impactite sequence cored in the Yaxcopoil-1 borehole (Figure 1) is formed by six distinct subunits, which are characterized by distinct composition, texture, matrix type and relative contents and type of basement, melt and carbonate particles. Clasts show different morphologies, sizes, preferential alignments and alteration degrees. Rock magnetic analyses take advantage of the high contrasts between the sedimentary clasts, carbonate-rich matrix, melt and basement clasts and melt-rich matrix. The variations in magnetic mineralogy, grain sizes and textures along the Yaxcopoil-1 subunits are recorded in the magnetic susceptibility logs (Urrutia-Fucugauchi et al., 2004b; Pilkington et al., 2004). The basal subunit formed in the early stages of cratering has been interpreted as: a) a ground surge in the transient cavity, b) a melt breccia with clastic material, and c) an excavation flow from the ejecta curtain interacting with the ejecta plume collapse (Stöffler et al., 2004; Kring et al., 2004; Tuchscherer et al., 2006).

Magnetic susceptibility and NRM intensities are low in the LS subunit (Figure 8), corresponding to its carbonate-rich character. The low-frequency susceptibility ranges from 5.48–6485 × 10^-6SI, with a mean value of 889.51 × 10^-6SI. The NRM intensity varies from 0.07 to 519.1 mA/m, around mean values of 52 mA/m. NRM intensity and susceptibility distributions are skewed to low values (Figure 8a, 8b), characterized by log-normal distributions. The anisotropy degree varies from low to high anisotropies with a range of P' values from 1.01 up to 1.12 (Figure 8c). Samples with oblate shaped ellipsoids tend to present low NRM intensities and susceptibilities and those with lineated fabrics show high NRM intensities and susceptibilities (Figure 8e). The NRM intensities and susceptibilities correlate, particularly for the prolate fabrics. Relationships with anisotropy degree appear more complex. Oblate fabrics show weak susceptibilities and a wide range of P' values, from weak anisotropies to strong anisotropies (Figure 8d). Prolate fabrics show narrow range in anisotropy degree (except for an anomalous value of 1.09) and a rough tendency to decrease with increasing susceptibility. This is better displayed in a semi-log graph; the anisotropy degree shows a tendency to decrease with increasing bulk susceptibility, and the tendency is apparent for both the oblate and prolate fabrics (Figure 8f).

Distribution of the principal susceptibility axes gives the axial orientations for prolate shaped and oblate ellipsoids (Figure 6b). Prolate ellipsoids show K₁ lineation, with intermediate to shallow dips. Oblate ellipsoids show K₁ axes with intermediate to steep dips. Wittmann et al. (2007) discussed the emplacement mechanisms for the impactite sequence in Yaxcopoil-1 borehole from petrologic and image analytical analyses of core samples. They proposed that emplacement of the LS began in the first minute after impact, with the ejecta curtain interacting with the high volume ejecta plume. Their reconstruction relied on the petrographic characteristics and modal compositional variations, using relative abundance, size distributions, preferred alignment and shape parameters (elongation) of melt particles. Melt particles have been described and characterized by detailed petrographic and geochemical analyses in several studies (Kring et al., 2004; Stöffler et al., 2004; Tuchscherer et al., 2006). Melt particles are highly magnetic compared to the carbonate-rich matrix and carbonate clasts. Therefore, possible correlation with the AMS derived fabrics could be expected.

The modal compositions, with relative contents of melt particles, basement and sedimentary clasts and matrix for the LS subunit are summarized in Figure 9a as a function of depth (Wittmann et al., 2007). Melt particles are characterized by high magnetic susceptibilities and NRM intensities (Urrutia-Fucugauchi et al., 2004b; Pilkington et al., 2004). Melt particles present in the LS are type 3 brecciated melt rock particles and type 3 schlieren melt particles. Melt particles types 4 and 1 are rare and there are no type 2 melt particles. Matrix represents about 40 % in volume up to 60 %. Basement clasts are less abundant and sedimentary carbonate clasts are around 20 %, reaching up to 70 % in the upper half of the subunit. The component size distribution covers the range 0.5 to 64 mm with mode of 4-2 mm; data are shown in a histogram in Figure 9b.

The depth patterns of modal composition data (Figure 9a) show a rough correlation with the AMS parameter data (Figure 7), with the peaks of lineation, foliation and anisotropy degree corresponding to the increases in type 3 BMR and schlieren melt particles. Lack of type 2 and low contents of type 4 melt particles in the LS indicate absence of airborne deposition for the subunit (Stöffler et al., 2004; Wittmann et al., 2007). The long axes of elongated melt particles show a tendency to lie in the horizontal plane (Figure 9c), with shallow dips determined from their relative orientation with respect to the core up-down axis. Dips vary from steep to shallow, which is also apparently observed for the prolate ellipsoids K₃ axes. Similar patterns are observed for the oblate ellipsoids. Possible controls on the AMS fabrics with relative contents and distribution of type 3 BMR and schlieren melt particles require further analysis. The modal compositional data and the trend of elongation of melt particles and high scatter pattern seems consistent with the excavation-flow model of Shuvalov (2003) of ejecta flows interacting with the ejecta plume. The LS subunit represents a mixture of material from the shallow carbonate target sequence and deeply excavated basement rocks (stream-tube depositional model of Stöffler et al., 2004).

AMS studies are used in understanding emplacement mechanisms and conditions of ignimbrites, lavas, intrusive bodies and sediments. Studies documented the spatial relationships between the principal susceptibility axes and the emplacement and flow mode and directions (e.g., Paquereau-Lebti et al., 2008; Petronis and Geissman, 2009; LaBerge et al., 2009). On the other hand, there are relatively few studies of emplacement mode and fabric characteristics of impact breccias, which may present characteristics similar to those recorded in ignimbrites and ground surges. This might be particularly the case for suevitic units emplaced as part of the ejecta curtain and basal surges. This emplacement mode has been suggested for the basal suevitic LS subunit by Stöffler et al. (2004), which may have involved dynamic conditions of high turbulence and hot gases at the floor of the transient cavity. High temperature turbulent conditions are suggested by the characteristics of melt particles and lithics in the LS. Carbonate clasts are metamorphosed with incipient resorption. Zircons show coarse recrystallization during prolonged annealing at temperatures above 700 °C. Melt particles are unsorted and shape oriented consistent with formation in a low viscosity melt rapidly quenched (Wittmann et al., 2007).

For interpretation of the magnetic fabric of the impact breccias, reference to observations on high energy sedimentary and pyroclastic flows provides an analogy (e.g., Tarling and Hrouda, 1993; Capaccioni et al., 2001; Petronis and Geissman, 2009). In particular, correlation with AMS fabrics in ignimbrites and ground surges provide additional insight on the nature of magnetic fabrics in suevites (Rochette and Filion, 1988; Rochette et al., 1992; Paquereau-Lebti et al., 2008; Petronis and Geissman, 2009). AMS studies on debris gravity flows, turbidites, ignimbrites and ground surges have shown flow parallel and flow transverse dominant orientations. Hot turbulent basal surges and laminar flows have distinctive magnetic fabrics, where maximum axes tend to lie parallel to flow directions with minimum axes normal to foliation planes (Cagnoli and Tarling, 1997). In some cases, maximum axes are the ones oriented perpendicular to flow directions (MacDonald and Palmer, 1990; Tarling and Hrouda, 1993; Cagnoli and Tarling, 1997).

The LS subunit show abundant carbonate lithics possibly incorporated from the target substrate. The lithics display a wide range of thermal effects from melted clasts to unmetamorphosed clasts with microfossils preserved (Tuchscherer et al., 2006). Melt particles tend to be elongated and randomly oriented and there are no fallout airborne transported particles. The suevites contain a range of melt particles and lithics of varying sizes, which may result in meandering, shearing and chaotic alignment of the fine particles, resulting in scattered axial distributions as observed for the basal pyroclastic surges (LeBerge et al., 2009). The long axes of melt particles tend to lie in the horizontal plane (Figure 9c). These characteristics appear consistent with a surge emplacement mechanism of an excavation flow interacting with the ground and the collapsing ejecta plume (Wittmann et al., 2007).

Part of the apparent scatter in the principal axis distribution observed for the prolate and oblate fabrics could arise from inverse fabrics, affecting the K₁ and K₃ axes. For the oblate fabrics, angular scatter is reduced for instance if shallow minimum K₃ axes and near vertical maximum K₁ axes are inverted. Inverse fabrics have been observed in volcanic and sedimentary rocks, where their maximum axes lie perpendicular to apparent dominant flow directions (Rochette et al., 1992; Ferré, 2002; Tarling and Hrouda, 1993). Multi-domain magnetite assemblages have maximum axes parallel to particle long axes. For assemblages of single-domain magnetites, maximum axes tend to be perpendicular to particle long axes (Potter and Stephenson, 1988). The hysteresis ratio plots show predominant PSD domain states for the LS subunit (Figure 4), which may represent a mixture of SD and MD particles. Detailed study of magnetic domain states are required to assess dependency of AMS axial distribution on dominant domain state. For heterogeneous breccias, separation of paramagnetic and diamagnetic contributions may become important. Intermediate fabrics not simply related to any given magnetic grain anisotropy may arise, which may be the case for the LS subunit in the impact breccias sequence.

The magnetic hysteresis and temperature variation of magnetic susceptibility show magnetic minerals with Curie temperatures ranging from 520 to 575 °C and hysteresis loops with high saturation magnetizations, indicating that the main magnetic minerals are low-Ti titanomagnetites. The hysteresis parameter ratio plot shows that most samples plot in the PSD domain field. The heating/cooling curves of magnetic susceptibility with increasing temperature show irreversible behavior. The cooling curves fall below the heating curves suggesting dissolving titanomagnetite lamellae in less magnetic host minerals, which is relatively infrequent as compared to production of magnetite during heating to temperatures of 600–700 °C. The alteration of magnetic mineralogy during laboratory heating has been investigated in several studies, providing evidence for temperature-induced alterations (Hrouda, 2003; Hrouda et al., 2003). Another factor to consider in the rock magnetic analysis is the effects of hydrothermal alteration. In large impacts, the high temperatures result in formation of a coherent melt sheet and generation of a long-lived hydrothermal system. Effects of hydrothermal alteration result in formation of secondary minerals, affecting the remanent magnetization and opaque minerals (Ade-Hall et al., 1971; Sweetkind et al., 2012). Rock magnetic analyses in the Chicxulub breccias have been documented, with formation of Fe–Ti oxide minerals (Pilkington et al., 2004; Kring et al., 2004; Urrutia-Fucugauchi et al., 2004b). The effects of hydrothermal alteration on the AMS and magnetic susceptibility in the LS subunit require further investigation.

The effects of shock on the magnetic properties and magnetization record have been long studied (e.g., Cisowski and Fuller, 1978; Halls, 1979). Shock induced effects on the AMS have been analyzed experimentally, to further understand the effects on target materials. Correlation of magnetic properties on target rocks with the direction of impact has also been examined for the Lonar crater (Arif et al., 2012). Rock magnetic properties in the target basalts are symmetrically oriented with respect to the plane of impact. Laboratory experiments have shown that impacts change the remanent magnetization, resulting in demagnetization and remagnetization effects, with changes in the coercivity (Gattacceca et al., 2007). The AMS axial distribution has also been shown to be affected, with principal susceptibility directions reoriented to the shock axis (Gatacceca et al., 2007; Nishioka et al., 2007). Nishioka et al. (2007) analyzed the shock effects on basalt target samples with pressures up to 5 GPa, showing that the maximum and minimum axes are reoriented with changes in the AMS ellipsoidal shape and anisotropy degree. Changes in ellipsoid shape were more pronounced for samples close to the impact point, with no appreciable changes for samples farther from impact point. Variation of shock pressure in target and impact-generated lithologies can then result in varying degrees of fabrics modification.

CONCLUSIONS

The AMS fabrics are characterized by oblate and prolate ellipsoids with principal susceptibility axial distributions showing high angular scatter, related to turbulent high temperature conditions during emplacement. Breccias with oblate ellipsoids tend to present low NRM intensities and susceptibilities and those with developed lineated fabrics show high NRM intensities and susceptibilities. The NRM intensities and susceptibilities show similar patterns, particularly for the prolate fabrics. Oblate fabrics show weak susceptibilities and wide range of P' values, from weak anisotropies to strong anisotropies. Prolate fabrics show narrow ranges in anisotropy degree with a tendency to decrease with increasing susceptibility. Anisotropy degree tends to decrease with increasing bulk susceptibility for oblate and prolate fabrics.

The oblate fabrics show K₁ axes with intermediate to steep dips. Prolate ellipsoids show K₁ lineation, with intermediate to shallow dips. Long axes of elongated melt particles tend to lie in the horizontal plane. Long axis particle dips, however, vary from steep to shallow, which is also observed for prolate and oblate ellipsoid K₁ and K₁ axes. Considering that the LS subunit shows mixture of material from shallow carbonate target and deep basement rocks (Kring et al., 2004; Stöffler et al., 2004; Wittmann et al., 2007), suevites were likely emplaced as an excavation flow incorporating ground surge material. Studies in the Ries crater have shown that elongated particles in the suevites are distributed radially or concentrically, consistent with a lateral transport mechanism (Meyer et al., 2011). This emplacement mechanism involves horizontal transport under high temperature turbulent conditions, similar to basal surges, plus ejecta plume collapse components. Modeling of suevite emplacement mechanisms however remains difficult because of the turbulent high energy high temperature environment.

This study forms part of the Programa Universitario de Perforaciones en Océanos y Continentes and Programa de Investigaciones del Cráter Chicxulub y Límite Cretácico/Paleógeno. We thank Víctor Macías and Martín Espinosa for technical assistance in the laboratory. Useful comments on the paper were provided by three anonymous reviewers and Associate Editor Avto Gogichaishvili. We acknowledge partial support for the project from DGAPA-PAPIIT grants IN-101112 and IG-101115.

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