IRM acquisition curves saturated below 300 mT (Figure 4b), together with the typical shape of hysteresis loops (Figure 4a) suggest that the NRM is carried by low-coercivity magnetic mineral such as magnetite and/or titanomagnetite [Tauxe et al., 1996]. Thermomagnetic analyses (Figure 4c) point out three distinct behaviors during heating: (1) an increase in susceptibility from 200 to 300°C, (2) a weak and continuous loss in susceptibility following the 300°C peak and (3) a significant drop in susceptibility at roughly 580°C (=Curie temperature of magnetite) [Dunlop and Özdemir, 2007] in almost all samples. The drop at the Curie temperature indicates magnetite as the main remanence carrier along the core. The increase in susceptibility during heating together with the higher susceptibility values after the cooling and the asymmetry of the heating and cooling curves are indicative of alteration, transformation and growth of magnetic minerals during the course of the analysis [Dearing, 1999; Maher and Thompson, 1999]. The decrease in magnetic susceptibility at 300–350°C could be associated with a change of maghemite to hematite [Dearing, 1999; Butler, 1992], or with some alteration of greigite and/or pyrrhotite [Maher and Thompson, 1999] within specific depth-intervals. The presence of greigite is confirmed by gyroremanence (GRM) in the AF demagnetization data of NRM [Roberts et al., 2011] at a few intervals (0–4 cm, 58–88 cm, 102–115 cm, 217–235 cm, 520–535 cm), while pyrrhotite may probably be present within the 130–160 cm depth-interval (olive-black clay sediments, facies “OC”) according the values of SIRM/kLF > 20 kAm−1 (not shown) and kARM/kLF > 15 [Maher and Thompson, 1999]. The recovery of the transition temperature near 350°C on the cooling curves (Figure 4c) suggests a Curie temperature for titanomagnetite [Butler, 1992]. Within the “Uppermost Brown facies” (upper part of the core), some susceptibility remains after 600°C, hinting at the presence of hematite within the magnetic assemblage at this specific interval which is also characterized by the highest MDFNRM (Figure 3) and a* (red) values (Figure 2). As a whole, the Pseudo-S ratio varies between ∼0.8 and 1 (Figure 3). Values higher than 0.9 are observed from the top to 130 cm and from 215 cm to the bottom of the core (except within specific layers, see below), indicating that much of the saturation of the magnetic assemblage is achieved in a 0.3 T field, which is consistent with the presence of magnetite and/or titanomagnetite as main remanence. Between 130 and 215 cm, the Pseudo-S ratio shows values close to 0.8 indicating the possible presence of higher coercivity minerals in this interval (i.e., goethite, greigite, pyrrhotite, hematite). MDFNRM values ranging from ∼25–30 mT are found from 250 cm to the bottom of the core which again suggests the presence of low coercivity minerals such as magnetite and/or titanomagnetite in this interval [Dankers, 1981] (Figure 3). From 80 cm to the top of the core, MDFNRM values sharply increase with values up to 90 mT except very low values (close to 5 mT) within the 45–60 cm and 90–105 cm layers corresponding to larger magnetic grain size (MD grains, Figures 3 and 5) also associated with a gravel peak (Figure 2). These high MDFNRMvalues could be characteristic of the presence of high-coercivity minerals such as hematite within the mineralogical assemblage. Between 90 to 105 cm, low Pseudo-S ratio values of ∼0.7 suggest the apparent presence of higher coercivity minerals such as goethite or hematite. However, when looking at the same ratio but at 0 mT, the values are close to 0.9 (not shown), which are indicative of low coercivity minerals. The difference between the Pseudo-S ratio at 0 and 25 mT thus reflects changes in magnetic grain size and not mineralogy in this specific interval characterized by the presence of gravel. Altogether these results point to magnetite and/or titanomagnetite as being the dominant remanence carriers throughout the core, although iron sulfides, maghemite and hematite may be present within specific depth-intervals.