Rock Magnetism / Paleomagnetism
The laboratory protocol for both sites was an initial alternating field (AF)
demagnetization to diminish the viscous remanence (up to 15 mT), followed by thermal
demagnetization to randomize the remanence from the weathering mineral goethite (~95°,
135°C) (Table S1). Higher temperatures were then used to isolate the primary remanence,
with as many as 11 progressive heating steps, up to 600°C (Fig. S1).
The heterogeneous fluvial deposits at Solana del Zamborino (La Solana del
Zamborino) have a similarly wide range of magnetic properties (Fig. S2) owing to the
general presence of iron oxides, and in some layers iron sulphides. We restricted our
sampling to siltstones and claystones in a sequence dominated by coarse sandstones
(medium sand to gravel). The remanence recorded by goethite (normal polarity) comprises
about 10% of the magnetization. The other secondary remanences (also normal polarity),
probably recorded by multi-domain magnetite, are a large part of the magnetization. In
general, the strength of the viscous (secondary) component correlates well with the lowfield
magnetic susceptibility and is generally removed by AF demagnetization (Fig. S2).
The remaining remanences (normal or reverse polarity) are the primary characteristic
remanence, which is probably recorded by hematite. These more stable components (with
higher coercivity and unblocking temperature) are clustered stratigraphically into
magnetozones: reverse polarity in a lower sequence [14 m, n=7], and normal polarity in an
upper sequence [12 m, n=6]. The two lowest samples in the normal polarity magnetozone
(from the fossil quarry) are greenish-gray claystones that have unusual magnetic behavior
during thermal demagnetization. Laboratory heating between 240° and 300°C causes
random dispersal of the remanence directions and/or the susceptibility to dramatically
increase. These observations appear to result from thermal alteration of iron sulphides such
as greigite and pyriteS1. We base our polarity determination for these 2 claystone layers
only on their response during the initial demagnetization phases, where the remanence
vectors behave similarly to the other normal polarity specimens. If these layers have reverse
polarity, then the age of Solana del Zamborino would be slightly older (~800 kyr).
The homogeneous, fine-grained deposits at Estrecho del Quípar (Cueva Negra del
Estrecho del Río Quípar) have a two-fold subdivision of their magnetic properties, Firstly,
the characteristic (primary) remanence has: 1) reverse polarity, 2) higher un-blocking
temperatures (>240°C), 3) higher coercivity (>40 mT), and 4) vector intensity that is
independent of low-field susceptibility or secondary vector intensity (Fig. S3). Secondly,
the secondary remanence has: 1) normal polarity, 2) low unblocking temperatures (mostly
<220°C), 3) low coercivity (<20 mT), and 4) vector intensity that directly correlates to lowfield
susceptibility, while being independent of the strength of the characteristic reverse
polarity component. We interpret the stable recorder of reverse polarity remanence to be
hematite, complexed with pedogenically-modified clays. In general, demagnetization
isolates this reverse polarity component (Fig. S1). We interpret the modern normal polarity
remanences to be recorded by multi-domain magnetite and the weathering mineral goethite.
Goethite accounts for a small portion (~10%) of the secondary remanence throughout the
deposit. Multi-domain magnetite accounts for the majority of the secondary remanence,
that average ~5X the intensity of the primary remanence for samples with unambiguous
reverse polarity (Δ>135°). However, these secondary remanences are ~12X the intensity of
the primary remanence for samples with mixed polarity components (Δ<135°), which
apparently reflects the combined effects of decreased intensity of the primary component
and the increased intensity of the secondary component (Fig. S3). Reverse polarity was
found at all 15 levels, in 40 out of 45 specimens. The other 5 specimens (from 3 levels)
have mixed component remanences with a weak reverse magnetization relative to a
dominant normal secondary overprint. The broad range of unblocking temperatures for all
minerals reflects the range of grain sizes and domain states in the iron oxides (magnetite,
hematite, and goethite).