Abstract
The type-section of the Blackwater Draw Formation (BDF) consists of a series of five paleosol horizons developed on eolian deposits and an overlying surficial soil. Previous work has shown that magnetic properties (e.g., χ, ARM, and IRM) as a function of depth in this type-section, display both magnetically enhanced and magnetically depleted signals for different paleosols. To better understand the magnetic mineralogy responsible for these varying responses, various rock-magnetic experiments, scanning electron microscopy, and Mössbauer spectroscopy were conducted on representative samples from the six soil units which constitute the BDF type-section. Our results show that sub-micron hematite [with a minor contribution from single-domain sized hematite (Hc = ∼500 mT) dominates all the soils in terms of weight percent concentration. Whereas, low coercivity (Hc = ∼35 mT or less) magnetite/maghemitized-magnetite grains, largely in the PSD state (Mr/Ms=∼0.14 +/– 0.03588, Hcr/Hc=∼2.68 +/– 0.298789), dominate the magnetic signal. Magnetically depleted soils show a relatively higher proportion of goethite, while magnetically enhanced soils show an increased contribution from SP/SSD magnetite/maghemite phases.By combining our data-set with geochemically-derived climofunctions, we have correlated the magnetically preserved, depleted, and enhanced sections of the type-section to three distinct environmental phases (I-III). The basal sediments of Phase I displays relatively homogenous (neither enhanced nor depleted) magnetic properties due to relatively arid conditions and minimal alteration of southerly derive eolian sands. Conversely, Phase II-III represents a change in weathering intensities and provenance, resulting in a mix of southerly derived sands and northerly derived silts. Phase II, experienced greater precipitation levels, resulting in the dissolution of Fe-oxide phases and thus magnetic depletion. The uppermost Phase III experienced intermediate precipitation intensities resulting in magnetic enhancement.Using previously published age models we tentatively interpret these changing environmental conditions to be influenced by the Middle-Pleistocene Transition (1.2-0.7 Ma), where the Earth’s climatic cycles shifted from a ∼41 kyr to ∼100 kyr cycles. However, ambiguities persist due to uncertainties in the currently published age model. Due to the complexity of the magnetic signal, we recommend future studies utilize a holistic approach, incorporating rock-magnetic, geochemical, and microscopy observations for more accurate reconstruction of regional paleoenvironments.
Highlights
Iron is the fourth most common element forming the planet (Lepp, 1975; Thompson and Oldfield, 1986; Frey and Reed, 2012) iron bearing minerals, including magnetic iron oxides, are a common constituent in most rocks in the Earth’s crust. Thompson and Oldfield (1986) recognized that environmentally influenced changes in iron oxide-bearing sediments correspond to changes in the magnetic properties of the bulk sediment material
Exposures of Blackwater Draw Formation (BDF) deposits are rare on the Southern High Plains (SHP) but here a gulley that first acted as an anthropogenic thoroughfare has incised down to the Caprock Caliche on top of the Ogallala Formation; this provides a complete section of the formation
Representative samples from all paleosols and the overlying Surficial Soil from the type-site of the BDF subjected to a range of both non-magnetic and magnetic experiments provide an improved understanding of the magnetic mineralogic cause of magnetic enhancement and magnetic depletion within the formation profile, observations which might be applied to similar sites
Summary
Iron is the fourth most common element forming the planet (Lepp, 1975; Thompson and Oldfield, 1986; Frey and Reed, 2012) iron bearing minerals, including magnetic iron oxides (i.e. magnetite, maghemite, hematite, and others), are a common constituent in most rocks in the Earth’s crust. Thompson and Oldfield (1986) recognized that environmentally influenced changes in iron oxide-bearing sediments correspond to changes in the magnetic properties of the bulk sediment material. It is often the case that fine-grained magnetite/maghemite particles form from the alteration of parent material (Thompson and Oldfield, 1986; Maher et al, 2003a, 2003b; Jordanova, 2016). These pedogenic magnetite/ maghemite particles include superparamagnetic (SP; grain size typically
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