Diagenetic Processes in the Fossilized Carapace of Neosclerocalyptus sp. from the Paraguayan Chaco

Abstract

Paleometry is essential in analyzing fossil remains, revealing diagenetic processes through physicochemical characterization techniques that identify crystalline and chemical structures, as well as elemental composition and changes observed via electron microscopy. This study examines the fossilized carapace of Neosclerocalyptus sp. from the Paraguayan Chaco, employing these methodologies to understand its diagenetic transformation. Fourier transform infrared (FT-IR) spectra identified phosphate, carbonate, and amide I and II groups. The Gaussian deconvolution model applied to the FT-IR spectra distinguished individual bands within overlapping vibrational modes, providing insights into the presence of stoichiometric and non-stoichiometric calcium phosphates. X-ray diffraction patterns confirmed the crystallinity and apatite nature of the sample, while energy dispersive X-ray fluorescence and scanning electron microscopy energy-dispersive spectroscopy assessed its elemental composition and microstructural characteristics. The results indicated the inclusion of new crystalline phases (quartz) and changes in mineralogy and crystallinity due to environmental interactions. A diagenetic pathway model is proposed, involving initial development, exposure to calcium carbonate-rich water, hydroxyapatite recrystallization, calcite infiltration in pores, and incorporation of new elements. This study enhances the understanding of fossil preservation and environmental influences on diagenetic processes at a regional level as well as being one of the first works on glyptodont carapace characterizations in South America.

Graphical abstract

This is a visual representation of the abstract.

Keywords

Diagenesis process hydroxyapatite‌spectroscopic analysis Fourier transform infrared FT-IR‌X-ray fluorescence XRF X-ray diffraction XRD‌scanning electron microscopy energy-dispersive spectroscopy SEM-XRD‌paleometry‌

Introduction

Paleometry is crucial for understanding fossil remains, integrating geology, biology, chemistry, and physics to reveal the origins and evolution of life on Earth and beyond.^1,2 Using techniques such as spectroscopy, it preserves rare fossils while deducing how they and their surrounding sediments change over time.^1,3–5 Paleometry helps reconstruct ancient ecosystems, providing insights into past climates, habitats, and biodiversity, which are key to interpreting evolutionary processes. It also clarifies how environmental factors affect fossil preservation, ensuring a more accurate interpretation of the fossil record.^2,6 Techniques such as Fourier transform infrared (FT-IR) spectroscopy, X-ray diffraction (XRD), X-ray fluorescence (XRF) spectrometry, and scanning electron microscopy energy-dispersive spectroscopy (SEM-EDS) are integral to this research. These advanced methodologies facilitate in-depth molecular-level analyses of fossils and their environmental interactions, providing critical insights into their formation and preservation. Specifically, the rapid identification of phosphate groups associated with apatite materials uncovers the complex interplay between groundwater chemistry and diagenetic transformations in biogenic materials.^1,3–5,7,8

When analyzing bones, the primary focus is on apatite, predominantly in the form of calcium phosphate, which serves as the principal inorganic component of bone, vertebrate teeth, and certain carapaces or shells.^9,10 Bone mineral composition is approximately 60–70% inorganic material, mainly hydroxyapatite (Ca₁₀(PO₄)₆(OH)₂), which provides structural rigidity and strength.¹¹ The remaining 25% consists of organic material, largely type I collagen, along with non-collagenous proteins and lipids. Besides hydroxyapatite, the inorganic phase contains minor calcium phosphates such as brushite and tricalcium phosphate, as well as trace elements like magnesium and sodium, which can substitute for calcium within the hydroxyapatite lattice.⁷

Natural variations in bone composition can arise from factors such as diet and metabolism, leading to ionic substitutions at both calcium and phosphate sites. In contrast, changes during fossilization are indicated by the presence of increased carbonate ions, which can substitute for phosphate in the apatite structure, as well as alterations in crystallinity and the introduction of foreign minerals due to groundwater infiltration.^2,11 These substitutions create atomic-level disruptions that can notably alter the physical properties of bone crystals following burial.^12–14

These changes involve the degradation of the bone's organic matrix by microorganisms, happening both before and during transport and sedimentary events, recrystallization and ion absorption. Subsequent processes after deposition depend on site conditions such as the mineralogical composition of the sediment, pH, temperature, and water characteristics.^2,9,15,16

The diagenesis process encompasses the physical and chemical transformations that carbonate hydroxyapatite experiences in sediments due to groundwater exposure. Key processes include dissolution and recrystallization, where minerals are leached and then re-precipitated into more stable forms, as well as crystal growth, which alters structural integrity without necessarily dissolving the original material.^2,7,17,18

In 2020, a carapace of a Neosclerocalyptus sp. was collected outside Neuland, Boquerón Department, near the center of the Paraguayan Chaco. This study focuses on conducting a rigorous characterization of the fossil remain. A potential model of diagenetic pathways was proposed based on the geological conditions surrounding the fossil as well as its alterations.

We hypothesize that the partial preservation of organic materials within the osteoderms may have been influenced either by an early interruption in the fossilization process or by more recent contamination. This preservation might have been facilitated by the osteoderms’ isolation and protection within an inorganic matrix, where cementation occurred, preventing complete permineralization. Alternatively, it may result from the deposition of organic material from the surrounding environment.^19,20

Geological Environment

The Cenozoic sedimentary system which occurs in the central portion of South America, known as Chaco, spans around 840 000 km² and extends from the Sub-Andean Sierras to the Paraná basin, covering parts of northeastern Argentina, southern Bolivia and western Paraguay. Shaped by six major river systems, including the Pilcomayo and Bermejo rivers, which flow eastward from the Andes towards the Paraguay and Paraná rivers, the region is characterized by large alluvial fans, creating a landscape of ancient channels, meandering lakes, and swampy areas.^21–33 It is essential to understand the sedimentary context of the Paraguayan Chaco, a region whose geological evolution reveals that it is largely composed of transported soils, ranging from sandy loam to clay.³⁴

Sedimentation in the Chaco began in the Oligocene period and continues to this day. These sediments, carried from the Andes, have deposited thick layers across the plains, shaped by two key phases of river activity: one during the late Pleistocene and another after the Ice Age.^21–24,35 Wet climates stabilized the river systems, leading to finer sediment deposits, while dry periods led channels to shift and increased sedimentation. Evidence of old riverbeds are still visible, especially in the Pilcomayo system, one of the most sediment-rich rivers in the world, transporting around 140 million tons of sediment annually.^24,28

Fossil remains of Neosclerocalyptus sp. were found about 3 m deep in Neuland, a part of the Boquerón District, seen in Figure 1a. This place is within the central area of the Pilcomayo River's alluvial fan that spans over 210 000 km² and extends more than 1000 km from its starting point to the Paraguay River.^24,28 The region's depositional environments have evolved: it began with short-lived braided streams and hardened soils in the late Oligocene, transitioning to large riverbanks that created thick deposits on the floodplain, pushing sediment progressively eastward.²³

Figure 1.

(a) Location map of the glyptodont's carapace fossil discovery site. (b) Excavation site of the fossil carapace. (c) Analyzed fragments of the glyptodont's carapace fossil of Neosclerocalyptus sp., coded as FACEN-PVert-0064.

The Chaco's geological history has a significant impact on bone preservation. As sediments accumulate, minerals can leach into buried bones, altering their chemical composition and potentially modifying isotopic ratios. Climatic fluctuations, alternating between wet and dry periods, further influence sedimentation, which directly affects bone chemistry. During diagenesis, interactions like groundwater movement through sediments can further modify the bones. In the Chaco, where river activity drives significant sediment transport, these processes are particularly important to consider during fossil analysis.^22,34,36

Experimental

Materials and Methods

The carapace presented in this manuscript was discovered and collected in September 2020 from the plains near Neuland Town (latitude: 22°38′53.61'S; longitude: 60°4′38.77″W), in the Boquerón Department of Western Paraguay,³⁷ as seen in Figure 1b. The partial carapace is deposited at the Laboratorio de Paleontología, Facultad de Ciencias Exactas y Naturales, Universidad Nacional de Asunción, under the collection number FACEN-PVert-0064.

The fossil remains were assigned to the genus Neosclerocalyptus based on certain diagnostic characteristics, including a reduced size compared to other taxa, a low and elongated subcylindrical dorsal carapace, and elongated rectangular lateral plates that are relatively thin with a central figure larger than the peripheral ones.^38,39 Although the genus Neosclerocalyptus is represented by five recognized species: N. castellanosi, N. ornatus, N. pseudornatus, N. gouldi, and N. paskoensis,⁴⁰ one of the diagnostic features for species assignment is the development and pneumatization of the frontonasal sinuses, as well as their extensively studied and recognized biostratigraphical distribution.⁴¹

Nevertheless, the absence of the skull and other diagnostic aspects of the skeleton, along with the uncertainty about the age of the sediments in which the specimen was found, prevent us from assigning the materials to one of the recognized species of the Neosclerocalyptus genera.

Two small peripheric osteoderm fragments from the edge of the dorsal carapace were selected for this study, presented in Figure 1c. These fragments were chosen due to their relatively protected location, being less exposed to surrounding sediments. After careful cleaning, the samples were placed in sterile bags to prevent any contamination, either during field collection or later in the laboratory.

FT-IR spectroscopy measurements were conducted using an IRAffinity-1 Infrared Spectrometer (Shimadzu) configured with a spectral resolution of 0.5 cm⁻¹ and set to 4 cm⁻¹. The instrument performed 128 scans over a spectral range of 400 to 4000 cm⁻¹. The sample preparation involved pulverizing a small fragment of the fossil with a mortar and pestle, followed by the addition of potassium bromide (KBr) powder as a binding agent. The mixture was then pressed to form a pellet, which was then measured in transmission mode.

For spectral processing, the FT-IR spectra underwent baseline corrections, smoothing, and second derivative calculations,^42,43 performed three times using the Spectragryph software.⁴⁴ Among the three collected FT-IR spectra, the most representative one was selected for detailed analysis. The deconvolution of IR spectra utilized a model of N coupled Gaussian oscillators adopted for calcium phosphates,^45–47 identifying regions of interest (ROI) where these compounds exhibited a response. The second derivative of the spectra was calculated to locate the minima. Deconvolution was carried out using the Gaussian deconvolution model (GDM) via the open-source software Fityk,⁴⁸ where each curve's centroid corresponds to an active band, and intensity relates to the number of oscillators, considering common active modes in IR and the second derivative minima.⁴⁹

The XRD analyses were performed using a PANalytical X’Pert Pro MRD diffractometer (Malvern Panalytical), featuring a spectral resolution of approximately 5 arcseconds.³ The analysis employed a Cu Kα radiation source with a wavelength of λ = 1.54060 Å and a powdered FACEN-PVert-0064 sample. The angular measurement range spanned from 5° to 60° at a step size of 0.025 degrees and an accumulation time of 3 seconds for each angular position, aiming to optimize the signal-to-noise ratio. The analysis involved comparing the crystalline phase pattern with the experimental X-ray diffractogram.

The elemental composition of FACEN-PVert-0064 was qualitatively assessed using the EDX-7000 energy dispersive X-ray fluorescence system (Shimadzu), achieving an energy resolution of less than 140 eV for the Mn Kα line, equipped with a Rh anode and a solid-state-type detector. All EDXRF spectra analyses were done using the PCEDX Pro software by fundamentals parameters methods for semiquantitative analysis.

The microstructure was examined through scanning electron microscopy (SEM). Prior to the SEM analysis, the fossil remains underwent a standardized carbon-coating process to mitigate electron accumulation effects on irregular surfaces, executed at a 4 V for 8 seconds of carbon deposition time. The samples were subsequently examined using secondary electron imaging with a CX-200 Plus scanning electron microscope (COXEM Co., Ltd.), which boasts a spectral resolution of less than 3 nm at an acceleration voltage of 30 kV. For this study, however, the SEM operated at a voltage of 20 kV to optimize imaging conditions.

Finally, for enhanced characterization, a specific zone of the sample was subjected to elemental mapping with an energy dispersive X-ray spectrometer (EDS) equipped with an EDS Xplore30 Detector (Oxford Instruments), noted for its spectral resolution of approximately 129 eV for the Mn Kα peak at a count rate of 100 000 counts per second.

To ensure a comprehensive characterization, sediment samples were collected from an area in proximity to the fossil fragments. These sediments underwent the same analytical procedures, including FT-IR, XRD, EDXRF, and SEM-EDS analyses (Supplemental Material), thus maintaining consistency in the evaluation process.

Results

The FT-IR analysis revealed key functional groups characteristic of apatitic structures, including phosphates (PO₄³⁻), carbonates (CO₃²⁻), hydroxyl (OH⁻), and organic components. Figure 2a illustrates the specific absorption bands, while Table I details these spectral features, following a conventional FT-IR analysis approach for fossil samples. Phosphate groups exhibited O–P–O bond bending modes, and P–O bonds showed symmetric and asymmetric stretching modes.^{42,45,50–59} A potential vibrational signal for hydrogen phosphate (HPO₄²⁻) was also noted.⁵⁰

Figure 2.

(a) FT-IR spectra of FACEN-PVert-0064. (b) Gaussian deconvolution of the ROI (700–400 cm⁻¹). (c) Gaussian deconvolution of the ROI (1300–800 cm⁻¹).

Table I.

Assigned bands from the FT-IR spectrum of FACEN-PVert-0064.

Wavenumber (cm⁻¹)	Assignation	References
467	Double degenerated bending mode (ν₂) of the phosphate group PO₄ (O−P−O bond)	^50,56,59
562	Triply degenerated bending mode (ν₄) of the phosphate group PO₄ (O−P−O bond)	^{45,50,56–58}
602	Triply degenerated bending mode (ν₄) of the phosphate group PO₄ (O−P−O bond)	^45,50,56,58
875	Characteristic peak of hydrogen phosphate group (nondistinguishable peak) or a possible bending mode (ν₄ or ν₃) of carbonate group CO₃ in carbonated apatites	^45,50,56,60
960	Nondegenerated symmetric stretching mode (ν₁) of the phosphate group PO₄ (P−O bond)	^50–52
1029	Triply degenerated asymmetric stretching mode (ν₃) of the phosphate group PO₄ (P−O bond)	^42,54,58
1097	Triply degenerated asymmetric stretching mode (ν₃) of the phosphate group PO₄ (P−O bond)	^53,55
1453	Amide II or a doublet band (ν₃) of the carbonate group CO₃	^19,53,61
1628	Amide I (β-sheets) or a possible adsorbed water band	^{45,52,61–63}
3455	Stretching mode (ν_s) of the hydroxyl group OH or a possible adsorbed water band	^53,54,63,64

Table I further identifies the carbonate group, indicating possible ionic substitutions within the apatitic structure.^45,50,56,60 Additionally, the amide I group and overlapped signals from adsorbed water on clay were observed,^{45,52,61–63} along with stretching modes of hydroxyl groups and a broad peak attributed to adsorbed water.^53,54,63,64 Finally, the amide II group or a doublet band (ν₃) of the carbonate group was detected.^19,53,61

Given the broad FT-IR spectrum, it is crucial to focus on the overlapping bands in the ranges of 700–400 cm⁻¹ and 1300–800 cm⁻¹, as they reveal multiple absorption bands related to carbonate ionic substitutions and phosphate groups. Although these overlaps complicate precise identification, this complexity is effectively addressed through the deconvolutions shown in Figure 2b and 2c, and summarized in Tables II and III.

Table II.

FT-IR band assignments of the GDM from the ROI, 700–400 cm⁻¹.

Band	Center	Area	Full width half-maximum (FWHM)	Assignation	References
A	540.78	1.19225	21.1635	Bending modes of the phosphate group PO₄ (O−P−O bond)	⁶⁵
B	563.883	7.20892	23.3731	Triply degenerated bending modes (ν₄) of the phosphate group PO₄ (O−P−O bond)	^45,50,58
C	582.437	3.16674	19.1294	Triply degenerated bending modes (ν₄) of the phosphate group PO₄ (O−P−O bond)	^45,50,58
D	605.257	6.188	23.6065	Triply degenerated bending modes (ν₄) of the phosphate group PO₄ (O−P−O bond)	^45,50,58
E	630.45	1.54041	26.357	Librational mode (ν_L) of the hydroxyl group	⁵⁰

Table III.

FT-IR band assignments of the GDM from the ROI, 1300 to 800 cm⁻¹.

Band	Center	Area	FWHM	Assignation	References
A	873.225	1.58788	18.3809	Non-apatitic stretching mode (ν₂) of the carbonate group CO₃	⁴⁵
B	912.806	1.58248	37.1082	Stretching mode (ν₁) of the phosphate group PO₄	⁵⁵
C	958.498	8.75716	44.8985	Non-degenerate symmetric stretching mode (ν₁) of the phosphate PO₄ (P–O bond)	^50,66
D	998.484	12.1656	43.9676	PO₄ in an apatitic environment	⁶⁶
E	1031.53	33.764	54.9225	Triply degenerate asymmetric stretching mode (ν₃) of the phosphate PO₄ (P–O bond)	^50,58
F	1080.91	33.6672	76.2595	Triply degenerate asymmetric stretching mode (ν₃) of the phosphate PO₄ (P–O bond)	⁵⁰
G	1125.63	19.1723	97.2591	Due to the presence of HPO₄	⁶⁶

Table IV.

Estimation of the percentage weight composition of FACEN-PVert-0064 using the fundamental parameter method in EDXRF.

Element	Result (%wt)	Standard error (3σ)	Intensity
Si	41.37	0.128	2.9672
Ca	20.927	0.023	25.1892
Al	16.032	0.137	0.2544
P	12.128	0.049	1.3526
Fe	4.739	0.007	97.3695
K	3.57	0.01	2.9936
Traces	1.234

Table II presents the deconvolution of the first ROI from 700 to 400 cm⁻¹, where the phosphate group exhibits O–P–O bond bending modes and triply degenerated bending modes (ν₄).^45,50,58,65 Additionally, a librational mode (ν_L) of the hydroxyl group is observed at 630.45 cm⁻¹.⁵⁰

In the ROI of 1300–800 cm⁻¹, detailed in Table III, several P–O bond vibrational modes of the phosphate group are identified, include a stretching mode (ν₁), a non-degenerate symmetric stretching mode (ν₁), and a triply degenerate asymmetric stretching mode (ν₃). The PO₄ in an apatitic environment appears at 998.484 cm⁻¹, while a band at 1125.63 cm⁻¹ is attributed to the presence of hydrogen phosphate.^50,55,58,66 Additionally, a non-apatitic stretching mode (ν₂) of the carbonate group is detected at 873.225 cm⁻¹.⁴⁵

Figure 3a presents the XRD results for FACEN-PVert-0064, confirming the apatitic nature of the sample. The analysis identifies common crystalline phases, including hydroxyapatite, which is prevalent in fossil structures, along with quartz (a silicate) and illite phases. In terms of elemental composition, the XRF results indicate the presence of Ca, P, and Si, consistent with the crystalline phases identified in the XRD analysis, as well as other secondary elements. Additionally, the Kα and Kβ emission lines for Mn and Cr are relatively close in energy, leading to overlapping peaks in the XRF spectrum. This overlap complicates the distinction between these elements, as illustrated in Figure 3b.

Figure 3.

(a) X-ray diffractogram and (b) EDXRF spectrum of FACEN-PVert-0064.

The EDXRF results show in Table IV a predominant presence of Si at 41.37% by weight (%wt). Ca and P were also detected, with a Ca/P ratio of approximately 1.72,^50,67 a value close to that of stoichiometric apatites. This ratio is comparable to those found in living organisms, highlighting the preservation of the original chemical composition throughout the fossilization process. Additionally, Al and Fe were identified at 16.032% and 4.739 %wt, respectively, along with 1.234% of traces of Ti, Mn, Sr, Cu, Zn, Cr, Rb, and Ni.

The FACEN-PVert-0064 SEM-EDS results are shown in Figure 4. In Figure 4a, a magenta outline highlighting the zone of interest, accompanied with its magnified SEM image in Figure 4b. EDS results are shown in Figure 4c. The elemental mapping reveals a uniform distribution of constituent elements, particularly notable on the main surface characterized by high porosity and voids.⁶⁸ The chemical composition in this area includes Ca, Si, P, Al, Fe, and K.

Figure 4.

(a) Low magnification and recognition of the area for examination; (b) SEM image of the zone to analyze; (c) EDS elemental mapping analysis.

Discussion

The FT-IR analysis reveals that the apatitic structure of bones contains carbonate ions, which partially overlap with phosphate ions. The deviations observed in the phosphate group bands are correlated with the presence of carbonate ions.^69,70 When comparing the experimental bands to those assigned in the literature, noticeable deviations were observed. The symmetric stretching of the PO₄³⁻ group is particularly sensitive to ionic impurities, especially substitution by CO₃²⁻. Any alterations in its ionic constituents can significantly affect the characteristics of the band.

Moreover, changes in the full width half-maximum (FWHM) parameters of the performed GDM curves were noted, with values being relatively higher than those reported for synthetic hydroxyapatites. This observation aligns with the inversely proportional relationship between FWHM values and their crystallite size; a narrower FWHM indicates higher crystallinity, while broader peaks suggest an increase in amorphous content.²

Considering the XRD pattern, it confirms the apatitic nature of the material and indicates the presence of silicates. The phase similar to hydroxyapatite is the most abundant, accompanied by quartz and illite. The crystallinity of illite is a crucial indicator of metamorphic grade in clay-rich rocks that have transformed between diagenesis and low-grade metamorphism,⁷¹ which coincides with the soil condition of the Paraguayan Chaco.⁷² In the EDXRF analysis, for the elemental composition, prominent peaks of phosphorus and calcium are visible, which makes sense considering the apatitic structure of bones. The silicon peak is also noteworthy, emphasizing the quartz phase found in the XRD analysis.

Trace elements like Sr, Cu, Zn, and Ni accumulate in bones, reflecting possible environmental conditions and diet during life. Metals such as Mn and Zn are influenced by both environmental factors and postmortem chemical changes.^73,74 After burial, bones undergo chemical changes, increasing metal concentrations like Mn and Ni through sediment interactions.⁷³ On the other hand, sediment concentration of Mn, Cr, Ti, Cu, Zn, and Rb vary by location and environmental conditions, often impacted by human activities or natural geological processes.^74–76

The high percentage of Si, along with the trace elements could be due to the inclusion, surface deposition, and penetration through the pores of the fossil material, originating from the sediment (Figure S1, Figure S2, and Table S1, Supplemental Material) incorporated into the analyzed material as well as biogenic changes due to the diagenesis process.

As a pioneering study on glyptodont carapace characterization, drawing parallels with modern relatives like armadillos helps shed light on the incorporation of various elements. A comparison between the modern armadillo and Neosclerocalyptus sp. armor reveals that both are primarily composed of hydroxyapatite, with collagen also present for this modern relative and potentially preserved in the case of the glyptodont carapace. The similarities in elemental composition and chemical structure suggest a shared fundamental framework, with any observed differences likely attributable to diagenetic processes during fossilization. The glyptodont osteoderms show evidence of mineralization influenced by elements such as Si, Ca, and Fe, which reflects postmortem alterations rather than intrinsic differences in their original composition. In contrast, the armadillo osteoderms retain their well-organized hydroxyapatite structure, reinforced by collagen fibers for flexibility.⁷⁷

Similarly, concerning the morphological structure revealed through SEM analysis, the identified elements might be associated with enrichment or supergene processes subsequent to the burial of the material. Additionally, the fossil exhibits an amorphous and perforated surface, attributed to bioerosion and an extensive diagenesis process. It is plausible that these minerals constituted a significant component of the sedimentary layer at the extraction site of Neosclerocalyptus sp. in Neuland town, suggesting a combination of the apatitic nature of the osseous shell and silicates.

The identification of functional groups, crystalline phases, element characterization, morphological structure and knowledge of the extraction site of the fossil remains of the Neosclerocalyptus sp. suggest a possible diagenetic pathway. Considering the sedimentary rocks of the Paraguayan Chaco, the sediment can experience significant changes from the moment of deposition until its transformation into sedimentary rock.⁷⁸

The theoretical process of fossilization explains how bone remains are preserved in sediments through permineralization, where water enriched with various compounds (Si, Fe, and Ca, among others) infiltrates and penetrate through the pores of the material, allowing for precipitation. This process strengthens the remains while preserving their original structure. Therefore, diagenesis is influenced by the characteristics of the sedimentary environment, which control the geochemical conditions during fossilization.^79–82 For the osteoderm under study in this manuscript, we have considered two possible diagenetic pathways A and B (Figure 5), inspired by the work of de Sousa et al.,² that could, to some extent, explain the process by which carbonate phases were incorporated into the osteoderm.

Figure 5.

Model of possible diagenetic pathways according to the geological conditions of the fossil FACEN-PVert-0064.

In the first pathway, Route A (leaching), moisture from the surface infiltrates through the soil, incorporating phases from carbonate-rich layers, such as calcite, which are pedogenetically incorporated in the more superficial layers. This process is influenced by relative humidity and biological activity, which facilitate the formation of pedogenic carbonates. Accumulation typically occurs in water-deficient areas, where climatic conditions favor carbonate precipitation.⁸³

Route B (capillarity) suggests that carbonates form from deeper layers below the Neosclerocalyptus sp. site, unrelated to biological activity. Instead, this process is linked to water table fluctuations over long geological periods. The unsaturated zone above the phreatic level has negative pressure relative to local atmospheric pressure, causing moisture to rise via capillarity. Water molecules move upward due to surface tension and mineral attraction. When the capillary fringe reaches the evapotranspiration zone, up to about 375 m, depending on sediment, moisture loss leads to compound precipitation, enriching surface zones with materials from deeper layers.⁸⁴

The incorporation of carbonate ions into the bone matrix is crucial for bone mineralization, particularly during recrystallization. During diagenesis, carbonate ions from surrounding sediments infiltrate the porous bone matrix, often substituting for phosphate groups in hydroxyapatite crystals. Osteoblasts transport calcium and phosphate into the extracellular matrix to form hydroxyapatite crystals. During recrystallization, carbonate ions help transform amorphous calcium phosphate into stable crystals, improving the resilience of the bone matrix. Carbonates influence hydroxyapatite's solubility, stability, and the pH needed for effective mineralization.^85–88

The results indicate vibrational modes corresponding to carbonate groups, specifically large-sized crystal B-type carbonate, presumably formed by partial or total substitution of CO₃ for PO₄,^89,90 and the organic amide group, which may be responsible for the organic and collagen fractions. These processes possibly lead to the formation of both stoichiometric and non-stoichiometric calcium phosphates.

Finally, it is suggested that the recrystallization process may have begun in the early stages of diagenesis, and that during this process, up until late diagenesis, the total or partial incorporation of other trace elements identified in both the fossil and sediment may have occurred within the apatite structure of the fossil, influenced by the surrounding environmental conditions.^91,92

Conclusion

Through FT-IR analyses, vibration modes corresponding to phosphate, carbonate, hydroxyl, carboxyl, methyl, and amide groups were identified, along with the presence of crystalline phases and various elements.

The GDM allowed for the identification of individual bands within overlapped vibration modes, providing detailed bond information. Additionally, diffraction patterns confirmed the crystallinity and apatitic nature of the samples, while fluorescence spectra assessed the integration of new elements. SEM-EDS analysis provided a microstructural display of the surface and examined the elements present.

Notably, the appearance of a new crystalline phase (quartz), along with changes in peak positions and FWHM values, indicated alterations in mineral purity and crystallinity due to environmental interactions. This suggests a diagenetic pathway involving initial amorphous development followed by exposure to calcium carbonate-rich water, leading to recrystallization of hydroxyapatite, filtration of calcite into pores, and the total or partial incorporation of other elements identified in both the fossil remains and the surrounding sediment.

Supplemental Material

sj-docx-1-app-10.1177_27551857251327408 - Supplemental material for Diagenetic Processes in the Fossilized Carapace of Neosclerocalyptus sp. from the Paraguayan Chaco

Supplemental material, sj-docx-1-app-10.1177_27551857251327408 for Diagenetic Processes in the Fossilized Carapace of Neosclerocalyptus sp. from the Paraguayan Chaco by Deyne SM Buzarquis Arias, Edher Herrera, Christian F Colman, Yennifer Sarubbi Jacks, Sergio D Ríos, Ricardo Souberlich, Christian J Sánchez Gonzales and Alex Matos da Silva Costa in Applied Spectroscopy Practica

Footnotes

Acknowledgments

This work was supported by the Consejo Nacional de Ciencia y Tecnología (CONACYT) of Paraguay, finance code PINV15-120. This research is part of the IAEA-funded Technical Cooperation Project: “Strengthening Capabilities for the Utilization of Nuclear and Radiation Technology to Characterize, Conserve, and Preserve Cultural Heritage,” project code RLA1019. Thanks to the University Research Scholarship Program «Andrés Borgognon Montero» (PUBIABM) and Ganadera 13 de Mayo S.A., for the technical, scientific, and financial support in developing and concluding this study. Thanks to the Scientific Initiation Program (PIC) of FACEN–UNA for providing the necessary resources and infrastructure.

Declaration of Conflicting Interests

The authors declared no potential conflicts of interest with respect to the research, authorship, and/or publication of this article.

Funding

The authors received no financial support for the research, authorship, and/or publication of this article.

ORCID iDs

Deyne SM Buzarquis Arias

Edher Herrera

Christian F Colman

Yennifer Sarubbi Jacks

Sergio D Ríos

Ricardo Souberlich

Christian J Sánchez Gonzales

Alex Matos da Silva Costa

Supplemental Materials

All supplemental material mentioned in the text is available in the online version of the journal.

References

Gomes

Becker Kerber

Osés

Prado

, et al. “Paleometry as a Key Tool to Deal with Paleobiological and Astrobiological Issues: Some Contributions and Reflections on the Brazilian Fossil Record”. Int. J. Astrobiol. 2019. 18(6): 1–15. https://doi.org/10.1017/S1473550418000538

de Sousa

D.V.

Eltink

Oliveira

R.A.P.

Félix

J.F.

Guimarães

L.M.

. “Diagenetic Processes in Quaternary Fossil Bones from Tropical Limestone Caves”. Sci. Rep. 2020. 10(1): 21425. https://doi.org/10.1038/s41598-020-78482-0

Boaz

N.T.

Hampel

. “Strontium Content of Fossil Tooth Enamel and Diet of Early Hominids”. J. Paleontol. 1978. 52(4): 928–933. https://www.jstor.org/stable/1303911

de Queiroz

L.C.

Carlisbino

Agressott

E.V.H.

Paschoal

A.R.

, et al. “Paleoenvironmental Interpretations of Irati and Mangrullo Formations (Permian of Paraná Basin) Based on Rocks and Fossil Bones Through Spectroscopy Techniques”. Vib Spectrosc. 2020. 110: 103110. https://doi.org/10.1016/j.vibspec.2020.103110

Delgado

A.O.

Buck

P.V.

Osés

G.L.

Ghilardi

R.P.

, et al. “Paleometry: A Brand New Area in Brazilian Science”. Mat Res. 2014. 17(6): 1434–1441. https://doi.org/10.1590/1516-1439.288514

Peppe

D.J.

Baumgartner

Flynn

Blonder

. “Reconstructing Paleoclimate and Paleoecology Using Fossil Leaves”. In: Croft

D.A.

D.F.

Simpson

S.W.

, editors. Methods in Paleoecology: Reconstructing Cenozoic Terrestrial Environments and Ecological Communities. Cham, Switzerland: Springer, 2018. Pp. 289–317.

Falgayrac

Vitale

Delannoy

Behal

, et al. “Bone Molecular Modifications Induced by Diagenesis Followed-Up for 12 Months”. Biology (Basel). 2022. 11(10): 1542. https://doi.org/10.3390/biology11101542

Rengger

J.R.

. Reise nach Paraguay in den Jahren 1818 bis 1826. Aarau: Saeurlaender, 1835.

Pasteris

Wopenka

Valsami-Jones

. “Bone and Tooth Mineralization: Why Apatite?”. Elements. 2008. 4(2): 97–104. https://doi.org/10.2113/GSELEMENTS.4.2.97

10.

Kallaste

Nemliher

. “Apatite Varieties in Extant and Fossil Vertebrate Mineralized Tissues”. J. Appl. Crystallogr. 2005. 38(4): 587–594. https://doi.org/10.1107/S0021889805011404

11.

Von Euw

Wang

Laurent

Drouet

, et al. “Bone Mineral: New Insights into Its Chemical Composition”. Sci. Rep. 2019. 9: 8456. https://doi.org/10.1038/s41598-019-44620-6

12.

Brown

P.W.

Constantz

. Hydroxyapatite and Related Materials. Boca Raton, Florida: CRC Press, 2017.

13.

de la Puerta

. Química Orgánica General y Aplicada a la Farmacia, Medicina, Industria, Agricultura y Artes. Galiciana: Imp. de T. Fortanet, 1872.

14.

Asscher

Regev

Weiner

Boaretto

. “Atomic Disorder in Fossil Tooth and Bone Mineral: An FT-IR Study Using the Grinding Curve Method”. Archeo Sci Revue d’Archéométrie. 2011. 35: 135–141. https://doi.org/10.4000/archeosciences.3062

15.

Anné

Wogelius

R.A.

Edwards

N.P.

Van Veelen

, et al. “Chemistry of Bone Remodelling Preserved in Extant and Fossil Sirenia”. Metallomics. 2016. 8(5): 508–513. https://doi.org/10.1039/c5mt00311c

16.

Newesely

“Fossil Bone Apatite”. Appl. Geochem. 1989. 4(3): 233–245. https://doi.org/10.1016/0883-2927(89)90023-1

17.

Sillen

. “Diagenesis of the Inorganic Phase of Cortical Bone”. In: Price

T.D.

, editor. The Chemistry of Prehistoric Human Bone. Cambridge: University of Cambridge Press, 1989. Pp. 221–229.

18.

Thomas

D.B.

McGoverin

C.M.

Fordyce

R.E.

Frew

R.D.

Gordon

K.C.

. “Raman Spectroscopy of Fossil Bioapatite: A Proxy for Diagenetic Alteration of the Oxygen Isotope Composition”. Palaeogeogr, Palaeoclimatol, Palaeoecol. 2011. 310(1–2): 62–70. https://doi.org/10.1016/j.palaeo.2011.06.016

19.

Lee

Y.C.

Chiang

C.C.

Huang

P.Y.

Chung

C.Y.

, et al. “Evidence of Preserved Collagen in an Early Jurassic Sauropodomorph Dinosaur Revealed by Synchrotron FT-IR Microspectroscopy”. Nat. Commun. 2017. 8(1): 14220. https://doi.org/10.1038/ncomms14220

20.

Saitta

E.T.

Liang

Lau

M.C.

Brown

C.M.

, et al. “Cretaceous Dinosaur Bone Contains Recent Organic Material and Provides an Environment Conducive to Microbial Communities”. Elife. 8: e46205. https://doi.org/10.7554/eLife.46205

21.

Cafaro

E.D.

Latrubesse

E.M.

Ramonell

C.G.

. “Distribución Espacial de Patrones de Cauce en Abanicos Aluviales Chaqueños”. Cuarto Simposio Regional Sobre Hidráulica de Ríos. 2009. 9–10.

22.

Uba

C.E.

Heubeck

Hulka

. “Evolution of the Late Cenozoic Chaco Foreland Basin, Southern Bolivia”. Basin Res. 2006. 18(2): 145–70. https://doi.org/10.1111/j.1365-2117.2006.00291.x

23.

Uba

C.E.

Heubeck

Hulka

. “Facies Analysis and Basin Architecture of the Neogene Subandean Synorogenic Wedge, Southern Bolivia”. Sediment Geol. 2005. 180(3–4): 91–123. https://doi.org/10.1016/j.sedgeo.2005.06.013

24.

Iriondo

. “Geomorphology and Late Quaternary of the Chaco (South America)”. Geomorphology. 1993. 7(4): 289–303. https://doi.org/10.1016/0169-555X(93)90059-B

25.

Kruck

Helms

Geyh

Suriano

, et al. “Late Pleistocene–Holocene History of Chaco–Pampa Sediments in Argentina and Paraguay”. Quat. Sci. J. 2011. 60(1): 188–202. https://doi.org/10.3285/eg.60.1.13

26.

Latrubesse

E.M.

Stevaux

Cremon

May

J.H.

, et al. “Late Quaternary Megafans, Fans, and Fluvio–Aeolian Interactions in the Bolivian Chaco, Tropical South America”. Palaeogeogr, Palaeoclimatol, Palaeoecol. 2012. 356–357: 75–88. https://doi.org/10.1016/j.palaeo.2012.04.003

27.

Latrubesse

E.M.

. “Large Rivers, Megafans and Other Quaternary Avulsive Fluvial Systems: A Potential ‘Who’s Who’ in the Geological Record”. Earth Sci. Rev. 2015. 146: 1–30. https://doi.org/10.1016/j.earscirev.2015.03.004

28.

Martín-Vide

J.P.

Amarilla

Zárate

F.J.

. “Collapse of the Pilcomayo River”. Geomorphology. 2014. 205: 155–163. https://doi.org/10.1016/j.geomorph.2012.12.007

29.

May

J.H.

Argollo

Veit

. “Holocene Landscape Evolution along the Andean Piedmont, Bolivian Chaco”. Palaeogeogr, Palaeoclimatol, Palaeoecol. 2008. 260(3–4): 505–520. https://doi.org/10.1016/j.palaeo.2007.12.009

30.

McGlue

M.M.

Smith

P.H.

Zani

Silva

, et al. “An Integrated Sedimentary Systems Analysis of the Río Bermejo (Argentina): Megafauna Character in the Overfilled Southern Chaco Foreland Basin”. J. Sediment. Res. 2016. 86(12): 1359–1377. https://doi.org/10.2110/jsr.2016.82

31.

Sambrook Smith

G.H.

Best

J.L.

LeRoy

J.Z.

Orfeo

. “The Alluvial Architecture of a Suspended Sediment Dominated Meandering River: The Río Bermejo, Argentina”. Sedimentology. 2015. 63(5): 1187–1208. https://doi.org/10.1111/sed.12256

32.

Suárez

P.A.

Sartirana

M.C.

Orfeo

. “Caracteres Sedimentológicos de Ambientes Fluviales de La Llanura Subtropical Chaqueña (Argentina)”. Acta Geológica Lilloana. 2010. 22(1–2): 34–45.

33.

Thalmeier

Kröhling

Brunetto

. “The Geomorphology and Late Quaternary Sedimentary Record of the Salado/Juramento Fluvial Megafan, Central Andes Foreland Basin (Chaco Plain, Argentina)”. Geomorphology. 2020. 373: 107495. https://doi.org/10.1016/j.geomorph.2020.107495

34.

Kuhn

C.A.C.

. The Geological Evolution of the Paraguayan Chaco. [Doctor of Philosophy in Geoscience Dissertation]. Lubbock, Texas: Texas Tech University, 1991.

35.

Argollo Bautista

Iriondo

M.H.

. El Cuaternario de Bolivia y Regiones Vecinas. Santa Fe: Museo Provincial de Ciencias Naturales Florentino Ameghino, 2017.

36.

Eckel

E.B.

. Geology and Mineral Resources of Paraguay: A Reconnaissance. Washington, DC: U.S. Department of the Interior, U.S. Government Printing Office, 1959.

37.

Government of Paraguay. Hallan fósil de más de 9 mil años en Presidente Hayes.2020. https://cultura.gov.py/2020/08/hallan-fosil-de-mas-de-9-mil-anos-en-presidente-hayes/ [accessed Feb 27 2025].

38.

A.E.

Zurita

Scillato

G.J.

Carlini

A.A.

. “Paleozoogeographic, Biostratigraphic, and Systematic Aspects of the Genus Sclerocalyptus Ameghino, 1891 (Xenarthra, Glyptodontidae) of Argentina”. 2005. 20(1–2): 121–129. https://doi.org/10.1016/j.jsames.2005.06.013

39.

Zurita

A.E.

. Sistemática y Evolución de los Hoplophorini (Xenarthra: Glyptodontidae: Hoplophorinae. Mioceno Tardío-Holoceno Temprano. [Doctoral Thesis]. Argentina: Universidad Nacional de La Plata, 2007.

40.

Quiñones

S.I.

De los Reyes

Zurita

A.E.

Cuadrelli

, et al. “Neosclerocalyptus Paula Couto (Xenarthra, Glyptodontidae) in the Late Pliocene–Earliest Pleistocene of the Pampean Region (Argentina): Its Contribution to the Understanding of Evolutionary History of Pleistocene Glyptodonts”. J. South Am. Earth Sci. 2020. 103: 102701. https://doi.org/10.1016/j.jsames.2020.102701

41.

Zurita

A.E.

Scarano

Carlini

Scillato-Yané

G.J.

Soibelzon

. “Neosclerocalyptus spp. (Cingulata: Glyptodontidae: Hoplophorini): Cranial Morphology and Palaeoenvironments Along the Changing Quaternary”. J. Nat. History. 2011. 45(15–16): 893–914. https://doi.org/10.1080/00222933.2010.536917

42.

Pleshko

Boskey

Mendelsohn

. “Novel Infrared Spectroscopic Method for the Determination of Crystallinity of Hydroxyapatite Minerals”. Biophys. J. 1991. 60(4): 786–793. https://doi.org/10.1016/S0006-3495(91)82113-0

43.

Stuart

B.H.

. Infrared Spectroscopy: Fundamentals and Applications. Chichester, UK: J. Wiley, 2004.

44.

Menges

. “Spectragryph: Optical Spectroscopy Software”. Spectroscopy. 2024. https://www.effemm2.de/spectragryph/index.html

45.

Brangule

Gross

. “Importance of FT-IR Spectra Deconvolution for the Analysis of Amorphous Calcium Phosphates”. IOP Conf Ser: Mater. Sci. Eng. 2015. 77: 012027. https://doi.org/10.1088/1757-899X/77/1/012027

46.

Rey

Shimizu

Collins

Glimcher

M.J.

. “Resolution-Enhanced Fourier Transform Infrared Spectroscopy Study of the Environment of Phosphate Ion in the Early Deposits of a Solid Phase of Calcium Phosphate in Bone and Enamel and their Evolution with Age: 2. Investigations in the v3 PO₄ Domain”. Calcif. Tissue Int. 1991. 49(6): 383–388. https://doi.org/10.1007/BF02555847

47.

Boldeskul

I.E.

Sukhodub

L.F.

Kalinkevich

A.N.

Khavryutchenko

V.D.

. “Ab Initio Modelling of Calcium Phosphate Clusters and Their Vibrational Spectra”. Cond. Matter Phys. 2006. 9(4): 669–679. https://doi.org/10.5488/CMP.9.4.669

48.

Wojdyr

. “Fityk: A General-Purpose Peak Fitting Program”. J. Appl. Crystallogr. 2010. 43(5–1): 1126–1128. https://doi.org/10.1107/S0021889810030499

49.

Britton

Liaaen-Jensen

Pfander

. Carotenoids. Basel: Springer AG, 2008.

50.

Koutsopoulos

. “Synthesis and Characterization of Hydroxyapatite Crystals: A Review Study on the Analytical Methods”. J. Biomed. Mater. Res. 2002. 62(4): 600–612. https://doi.org/10.1002/jbm.10280

51.

Joris

S.J.

Amberg

C.H.

. “The Nature of Deficiency in Nonstoichiometric Hydroxyapatites. II. Spectroscopic Studies of Calcium and Strontium Hydroxyapatites”. J. Phys. Chem. 1971. 75(20): 3172–3178. https://doi.org/10.1021/j100689a025

52.

Paschalis

E.P.

DiCarlo

Betts

Sherman

, et al. “FT-IR Microspectroscopic Analysis of Human Osteonal Bone”. Calcif Tissue Int. 1996. 59(6): 480–487. https://doi.org/10.1007/BF00369214

53.

Herrera

Ríos

Aquino

Colman

, et al. “Characterization of Dental Fragments of Toxodon sp. (Mammalia, Notoungulata) by Multiple Physical and Chemical Techniques”. Vib Spectrosc. 2021. 114: 103248. https://doi.org/10.1016/j.vibspec.2021.103248

54.

Antonakos

Liarokapis

Leventouri

. “Micro-Raman and FT-IR Studies of Synthetic and Natural Apatites”. Biomaterials. 2007. 28(19): 3043–3054. https://doi.org/10.1016/j.biomaterials.2007.02.028

55.

Fowler

B.O.

. “Infrared Studies of Apatites. I. Vibrational Assignments for Calcium, Strontium, and Barium Hydroxyapatites Utilizing Isotopic Substitution”. Inorg. Chem. 1974. 13(1): 194–207. https://doi.org/10.1021/ic50131a039

56.

Mamede

A.P.

Gonçalves

Marques

M.P.M.

Batista de Carvalho

L.A.E.

. “Burned Bones Tell Their Own Stories: A Review of Methodological Approaches to Assess Heat-Induced Diagenesis”. Appl. Spectrosc. Rev. 2018. 53(8): 603–635. https://doi.org/10.1080/05704928.2017.1400442

57.

Piga

Santos-Cubedo

Moya Solà

Brunetti

, et al. “An X-Ray Diffraction (XRD) and X-Ray Fluorescence (XRF) Investigation in Human and Animal Fossil Bones from Holocene to Middle Triassic”. J. Archaeol. Sci. 2009. 36(9): 1857–1868. https://doi.org/10.1016/j.jas.2009.04.013

58.

Wright

L.E.

Schwarcz

H.P.

. “Infrared and Isotopic Evidence for Diagenesis of Bone Apatite at Dos Pilas, Guatemala: Palaeodietary Implications”. J. Archaeol. Sci. 1996. 23(6): 933–944. https://doi.org/10.1006/jasc.1996.0087

59.

Eichert

Drouet

Sfihi

. “Nanocrystalline Apatite Based Biomaterials: Synthesis, Processing, and Characterization”. In: Kendall

J.B.

, editor. Biomaterials Research Advances. New York: Nova Science Publishers, 2008. Pp. 93–143.

60.

Beasley

M.M.

Bartelink

E.J.

Taylor

Miller

R.M.

. “Comparison of Transmission FT-IR, ATR, and DRIFT Spectra: Implications for Assessment of Bone Bioapatite Diagenesis”. J. Archaeol. Sci. 2014. 46: 16–22. https://doi.org/10.1016/j.jas.2014.03.008

61.

Barraza-Garza

de la Rosa

L.A.

Martínez-Martínez

Castillo-Michel

, et al. “La Microespectroscopía de Infrarrojo con Transformada de Fourier (FT-IRM) en El Estudio de Sistemas Biológicos”. Rev Latinoam de Quimica. 2013. 41(3): 125–148.

62.

Chadefaux

Le Hô

A.S.

Bellot-Gurlet

Reiche

. “Curve-Fitting Micro-ATR-FT-IR Studies of the Amide I and II Bands of Type I Collagen in Archaeological Bone Materials”. e-Preserv Sci 2009. 6: 129–137.

63.

Rytwo

Zakai

Wicklein

. “The Use of ATR-FT-IR Spectroscopy for Quantification of Adsorbed Compounds”. J. Spectrosc. 2015. 1: 1–8. https://doi.org/10.1155/2015/727595

64.

Olcott Marshall

Marshall

C.P.

. “Vibrational Spectroscopy of Fossils”. Palaeontology. 2015. 58(2): 201–211. https://doi.org/10.1111/pala.12144

65.

Chapman

A.C.

Long

D.A.

Jones

D.T.L.

. “Spectra of Phosphorous Compounds: II. The Force Constants of Orthophosphates”. Spectrochim. Acta. 1965. 21(4): 633–640. https://doi.org/10.1016/0371-1951(65)80019-4

66.

Paschalis

E.P.

Mendelsohn

Boskey

A.L.

. “Infrared Assessment of Bone Quality: A Review”. Clin Orthop Relat Res. 2011. 469(8): 2170–2178. https://doi.org/10.1007/s11999-010-1751-4

67.

Elliott

J.C.

Wilson

Dowker

S.E.P.

. “Apatite Structures”. Adv. X-ray Anal. 2002. 45: 172–181.

68.

Fleet

M.E.

Liu

King

P.L.

. “Accommodation of the Carbonate Ion in Apatite: An FTIR and X-Ray Structure Study of Crystals Synthesized at 2–4 GPa”. Am. Mineral. 2004. 89(10): 1422–1432. https://doi.org/10.2138/am-2004-1009/html

69.

Jurašeková

Fabriciová

Silveira

L.F.

Lee

Y.N.

, et al. “Raman Spectra and Ancient Life: Vibrational ID Profiles of Fossilized (Bone) Tissues”. Int. J. Mol. Sci. 2022. 23(18): 10689. https://doi.org/10.3390/ijms231810689

70.

Otto

de Grauw

C.J.

Duindam

J.J.

Sijtsema

N.M.

Greve

. “Applications of Micro-Raman Imaging in Biomedical Research”. J. Raman. Spectrosc. 1997. 28(2–3): 143–150. https://doi.org/10.1002/%28SICI%291097-4555%28199702%2928%3A2/3%3C143%3A%3AAID-JRS70%3E3.0.CO%3B2-9

71.

Merriman

R.J.

Frey

. “Patterns of Very Low-Grade Metamorphism in Metapelitic Rocks. En: Low-Grade Metamorphism”. In: Frey

Robinson

, editors. Low-Grade Metomorphism. Chichester, UK: John Wiley and Sons, Ltd., 1998. Pp. 61–107.

72.

Armengol

Ayora

Manzano

Bea

S.A.

Martínez

. “The Role of Loess Weathering in the Groundwater Chemistry of the Chaco–Pampean Plain (Argentina)”. J. Hydrol. 2020. 587: 124984. https://doi.org/10.1016/j.jhydrol.2020.124984

73.

Krajcarz

M.T.

. “Alteration of the Metal Content in Animal Bones after 2.5-Year Experimental Exposure to Sediments”. Archaeol. Anthropol. Sci. 2019. 11(1): 361–372. https://doi.org/10.1007/s12520-017-0533-2

74.

Tanjin

Rahman

M.M.

Jolly

Y.N.

Riya

K.K.

, et al. “Accumulation and Phytoremediation Potentiality of Trace and Heavy Metals in Some Selected Aquatic Plants from a Highly Urbanized Subtropical Estuary”. J. Marine Sci Eng. 2024. 12(7): 1131. https://doi.org/10.3390/jmse12071131

75.

Ediagbonya

R.F.

Balogun

O.T.

. “Potential Risk Assessment and Spatial Distribution of Elemental Concentrations in Sediment”. Appl. Water Sci. 2020. 10(7): 176. https://doi.org/10.1007/s13201-020-01260-w

76.

García-López

Cortizas

A.M.

Álvarez-Fernández

López-Costas

. “Understanding Necrosol Pedogenetical Processes in Post-Roman Burials Developed on Dunes Sands”. Sci. Rep. 2022. 12(1): 10619. https://doi.org/10.1038/s41598-022-14750-5

77.

Chen

I.H.

Kiang

J.H.

Correa

Lopez

M.I.

, et al. “Armadillo Armor: Mechanical Testing and Micro-Structural Evaluation”. J. Mech. Behav. Biomed. Mater. 2011. 4(5): 713–722. https://doi.org/10.1016/j.jmbbm.2010.12.013

78.

Tarbuck

E.J.

Lutgens

F.K.

. Ciencias de la Tierra: Una Introducción a la Geología Física. Madrid: Pearson Educación, 2005.

79.

Mayer

E.L.

Hubbe

Botha-Brink

Ribeiro

A.M.

, et al. “Diagenetic Changes on Bone Histology of Quaternary Mammals from a Tropical Cave Deposit in Southeastern Brazil”. Palaeogeogr, Palaeoclimatol, Palaeoecol. 2020. 537: 109372. https://doi.org/10.1016/j.palaeo.2019.109372

80.

Nielsen-Marsh

C.M.

Hedges

R.E.M.

. “Patterns of Diagenesis in Bone I: The Effects of Site Environments”. J. Archaeol. Sci. 2000. 27(12): 1139–1150. https://doi.org/10.1006/jasc.1999.0537

81.

Hedges

R.E.M.

Millard

A.R.

. “Bones and Groundwater: Towards the Modelling of Diagenetic Processes”. J. Archaeol. Sci. Rep. 1995. 22(2): 155–164. https://doi.org/10.1006/jasc.1995.0017

82.

Saitta

E.T.

Kaye

T.G.

Vinther

. “Sediment-Encased Maturation: A Novel Method for Simulating Diagenesis in Organic Fossil Preservation”. Palaeontology. 2019. 62(1): 135–150. https://doi.org/10.1111/pala.12386

83.

Ovalle

Seguel

Pfeiffer

. “Genesis y Ocurrencia de Carbonatos en los Suelos”. Agro. Sur. 2023. 51(1): 1–17. https://doi.org/10.4206/agrosur.2023.v51n1-01

84.

Keeling

J.L.

. “Metal Ion Dispersion Through Transported Cover at Moonta, South Australia”. In: Proceedings of the CRC LEME Regional Regolith Symposia. Adelaide, Australia. 10–26 November 2004. Pp. 161–165.

85.

Berna

Matthews

Weiner

. “Solubilities of Bone Mineral from Archaeological Sites: The Recrystallization Window”. J. Archaeol. Sci. 2004. 31(7): 867–882. https://doi.org/10.1016/j.jas.2003.12.003

86.

Schlesinger

P.H.

Blair

H.C.

Stolz

D.B.

Riazanski

, et al. “Cellular and Extracellular Matrix of Bone, with Principles of Synthesis and Dependency of Mineral Deposition on Cell Membrane Transport”. Am. J. Physiol. Cell Physiol. 2019. 318(1): C111–C124. https://doi.org/10.1152/ajpcell.00120.2019

87.

Šromová

Sobola

Kaspar

. “A Brief Review of Bone Cell Function and Importance”. Cells. 2023. 12(21): 2576. https://doi.org/10.3390/cells12212576

88.

Feng

. “Chemical and Biochemical Basis of Cell–Bone Matrix Interaction in Health and Disease”. Curr Chem Biol. 2009. 3(2): 189–196. https://doi.org/10.2174/187231309788166398

89.

Ren

Leng

. “Carbonated Apatite, Type-A or Type-B?”. Key Eng. Mater. 2011. 493–494: 293–297. https://doi.org/10.4028/www.scientific.net/KEM.493-494.293

90.

Fleet

M.E.

Liu

. “Coupled Substitution of Type A and B Carbonate in Sodium-Bearing Apatite”. Biomaterials. 2007. 28(6): 916–926. https://doi.org/10.1016/j.biomaterials.2006.11.003

91.

Gueriau

Jauvion

Mocuta

. “Show Me Your Yttrium, and I Will Tell You Who You Are: Implications for Fossil Imaging”. Palaeontology. 2018. 61(6): 981–990. https://doi.org/10.1111/pala.12377

92.

Marchetti

Ricardi-Branco

Callefo

Delcourt

, et al. “Fossil Diagenesis and Ontogenetic Insights of Crocodyliform Bones from the Adamantina Formation, Bauru Basin, Brazil”. J. South Am. Earth Sci. 2019. 96: 102327. https://doi.org/10.1016/j.jsames.2019.102327

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