Spectroscopic Characterization of Eoholocene Bones Found in a Cave in Northeast Brazil.
The hard parts (skeletons) which usually undergo fossilization keep valuable information of biogenic processes, and the taphonomic characteristics supply data on the postmortem changes . Geochemical investigations and physical characterizations were performed to determine the composition of a fossil provide both taphonomic and ecologic data. Mineralogical composition of fossils can be adequately studied using physicochemical and mineralogical techniques such as X-ray fluorescence, X-ray diffraction, and infrared spectroscopy [2-4].
In northeastern Brazil, there are very important cenozoic continental deposits (especially caves) showing remains of organisms, valuable in the reconstruction of the paleoenviroment. The Ubajara National Park, in northeast Ceara State (Figure 1), is a karstic region where rocks suffered corrosion processes, subsequently creating caves and valleys. This region is part of a Spelean province composed by Neoproterozoic carbonatic rocks known as Serra da Ibiapaba, originating in the Upper Neogene-Quaternary according to Auler et al. [5, 6].
Of the 14 caves of the park, the most important is the Gruta do Urso Fossil (GUF) which lies at 03[degrees]49'58"S/ 40[degrees]53'34,4"W. The GUF was discovered in 1978 in Morro do Pendurado, and a fossilized skull of Arctotherium wingei was found . At GUF, several Early Eoholocene fragments of bones and teeth from small fauna, as well as gastropod shells, have been collected and reported in the specialized literature by Hsiou et al. , Oliveira et al. [9-11], and Viana . Additionally, these authors assigned an approximate age of 8,000 years BP based on the thermoluminescence measurements of local sediments .
The main goal of this work is to present the qualitative, quantitative, and semiquantitative physicochemical composition of fossils from a cave in the Ubajara National Park (Ceara State), in order to obtain taphonomic information. Unidentified long bone fragments were selected and analyzed using X-ray fluorescence spectroscopy (XRF), X-ray diffraction (XRD), and infrared spectroscopy (IR).
2. Materials and Methods
This research was carried out in two stages: (1) the fieldwork for the stratigraphic analysis and collection of samples, and (2) the laboratory work to obtain data on the physicochemical and mineralogical composition of the samples, diagenetic transformation, and taphonomic analysis.
2.1. Fieldwork. A 90 cm deep excavation was carried out in the GUF's entrance chamber. A stratigraphic study was performed and divided into 8 layers of 10 cm depth, named from C1 to C8. The material of each layer was sieved in situ to collect mineralized organic samples, such as bones and teeth. In all, seven fragments of bones from the layers C1 to C6 and C8, were selected for X-ray diffraction, X-ray fluorescence, and infrared spectroscopy measurements. Due to the scarcity of bone samples, layer C7 was not analyzed.
2.2. Laboratorial Work. X-Ray diffraction is used to determine the atomic and molecular nature of a crystalline structure. X-ray fluorescence spectroscopy was used to analyse both major and trace chemical elements from a sample. Infrared spectroscopy was useful to identify chemical compounds and molecular compositions, including amorphous samples.
At the laboratory, the selected samples were crushed in a porcelain mortar with pestle for the following analysis.
2.2.1. X-Ray Diffraction (XRD). The X-ray diffraction patterns were obtained using a Rigaku powder diffractometer with the Bragg-Brentano geometry. The Co-K[alpha] radiation was used and operated at 40 kV and 25 mA. The XRD measurements were taken in the 29 range of 3-45[degrees], using step scan procedures (0.02[degrees]) at counting times of 5 s.
2.2.2. X-Ray Fluorescence Spectroscopy (XRF). The X-ray fluorescence spectroscopy was performed using a ZSX Mini II equipment from Rigaku, operating with a Pb tube, using a power of 40 kV x 1.2 mA.
2.2.3. Infrared Spectroscopy. The infrared spectra were measured using the absorbance mode of transmittance measurement, and KBr pellets were used to dilute the samples. The samples were mixed with KBr powder in the proportion 1:100 from each sample (at about 5-10 mg). The pellet thickness varied from 0.5 to 0.6 mm, and they were measured in the spectral range from 400 to 4000 [cm.sup.-1] using a Vertex 70 spectrometer from Bruker.
3. Results and Discussion
The excavation resulted in the schematic section represented below, which demonstrates the stratigraphic distribution of the fossils in all layers found of unconsolidated sediments composed of both cave carbonate and siliciclastic material carried into the cave (Figure 2). The siliciclastic material was determined by microscopic analysis (not shown here), revealing the presence of small crystalline grains.
Table 1 summarizes the XRF analyses from seven small species of bone samples collected during the excavation at GUF. From this analysis, the main chemical elements were detected: Ca and P, which are the mineral components of the bones, and trace elements such as Zn, Sr, Si, S, Mn, K, Fe, Cl, and Al. The elements K, Si, Al, Fe, and Cl are basic constituents from the soil formation . The amount of Zn in bones is an indicator of meat food, and the amount of Sr and Mn is an indicator of plant food, suggesting different species of animals were found . Observing Ca/P amount relationship, it is possible to infer about similar groups C1, C3, and C4 (9.3-8.2) and C5, C6, and C8 (6.2-5.5). However, C2 (7.6) can not be related with any group cited above.
The XRD diffractograms indexed hydroxyapatite ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]) as the majority phase in all samples, which were identified using the ICDD Reference code: 00001-1008, PDF index name: calcium hydroxide phosphate. These results suggest that the biomineralization of the bones is preserved (Figures 3 and 4). Other phases of the diffractograms include crystalline calcium carbonate as calcite (CaC[O.sub.3]). The elemental analysis (XRF) was not able to identify C and O because of the limitation of equipment. However, Ca and P are the majority elements identified by XRF, and the measurements are agreeing with XRD. These chemical characteristics and the incrustation observed from fossil analyses suggest that in all layers, there has been an incrustation of calcium carbonate from the dissolution and reprecipitation of the cave's carbonatic rocks.
XRD diffractograms indexed the (002) plane related to the crystalline hydroxyapatite phase. The Debye-Scherrer equation (Equation (1)) was used to calculate the crystallite size  (Table 2):
[tau] = k[lambda]/[beta] cos ([theta]), (1)
where [tau] is the size of crystallite (nm), k is the shape constant, k = 0.9, corresponding to the spherical shape, [lambda] is the Co-K[alpha] radiation wavelength (1.7928 [Angstrom]), [beta] is the full-width half maximum (FWHM) of the XRD peak plane (hkl), and [theta] is the diffraction angle (degrees) in accordance with Bragg's law and the (002) plane of crystalline hydroxyapatite ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]).
The results listed in Table 2 show that the sizes of crystallites were heterogeneous. Some groups presented similar crystallite sizes, C3 with C4, C2 with C5, and C6 with C8. The more crystalline samples showed larger crystallite sizes (C2 and C5).
The IR spectra (Figures 5 and 6) showed characteristic bands of hydroxyapatite [2-4]. Specifically, the bands centered at 467 and 557 [cm.sup.-1] are associated with antisymmetric deformation of P[O.sup.3-.sub.4] ion, while the bands around 1020 [cm.sup.-1] are related to the antisymmetric stretching of P[O.sup.3-.sub.4]. Furthermore, calcite bands at 875 [cm.sup.-1] correspond to symmetric deformations of C[O.sup.3-.sub.4], and bands at 1419 and 1460 [cm.sup.-1] due to symmetric stretchings of C[O.sup.3-.sub.4] were observed [2-4]. IR results were synergistic with the XRF and XRD analysis, suggesting together the presences of crystalline calcium, carbonate, and phosphate phases.
From the IR spectra, it is possible to estimate the relative amount of apatite and carbonate phases (Table 3). For this, the intensities of the two strongest peaks of both carbonate and phosphate phases were used. The base line was subtracted between 400 [cm.sup.-1] and 1600 [cm.sup.-1]. The relative amount of carbonate/phosphate was calculated according to the following expression:
carbonate/phosphate = AA' + BB'/CC' + DD', (2)
where [AA' + BB'] is the intensity of the carbonite bands (1447 [cm.sup.-1] and 1413 [cm.sup.-1], respectively) and [CC' + DD1] is the intensity of the phosphate bands (599 [cm.sup.-1] and 561 [cm.sup.-1], respectively).
The IR spectra also afforded the estimation of the amount of carbonate ions (% y) in the nanohydroxyapatite (nHAp) lattice (Table 3) by calculating the ratio of intensity between the carbonate at 1420 [cm.sup.-1] ([I.sub.c]) and the phosphate at 598 [cm.sup.-1] ([I.sub.p]) bands using the following equation :
[mathematical expression not reproducible]. (3)
The use of XRD to address the crystallographic changes in ancient bones has often been documented [13-20]. The crystallinity Index (CI) and carbonate/phosphate ratio (C/P) are extremely useful for the determination of the mineral alteration in both diagenetic and postdiagenetic bone. Here, we interpreted the CI as a representative of common diagenetic effects. Thus, we consider that the diagenesis in general sense, e.g., a decrease in histological preservation, increased with an increase in bone porosity and mineral crystallinity. Lee-Thorp and Sponheimer  discussed that the relationship between crystallinity and elemental alteration is not clear. Previous studies [16, 17] have suggested that an increase in CI values is not directly correlated with the age of the bones, i.e., CI does not increase with increasing age. Furthermore, the CI range is not uniform between different chemical environments. Puceat et al. , compared various CIs using Raman and FT-IR spectroscopy and X-ray diffractometry.
Early diagenetic factors (e.g., microbial attacks and hydrolysis) are associated with an increase of bone porosity [22, 23]. According to Smith et al. , the increase of bone porosity can coincide with a decrease in CI values. The porosity may increase the interaction between bone and soil water, thereby causing a loss of organic content. Thus, exogenous minerals may be deposited within bone at any time postmortem. According to Table 3, the samples C2, C5, C6, and C8 present a small range of CI values. Although samples C3 and C6 exhibited slightly different values, the only significantly different value was that of C1 (0.25). The C1 sample results suggest the presence of calcite as an exogenous mineral, which is expected once the fossil is placed in a karst environment. In C1, there is a clear correlation between the increase of C/P ratio with decreasing CI (Table 3). These results support the literature; for example, Astibia et al.  reported that the degree of crystallinity increased during fossilization.
The sample fossils from GUF are the same age; therefore, the most important parameter responsible for the observed range of CI and C/P ratio values are local taphonomical conditions. The bone from C1 layer, at the top of the section, is most susceptible to interaction with pore-water and microorganisms accelerating the rate of dissolution, which facilitate exogenous and secondary minerals precipitation inside of the fossil. Indeed, the fact that the CI analyses do not differ significantly (barring sample C1) is not surprising because all samples come from the same locality. Therefore, this relative homogeneity can be explained by the fact that the remains have been deposited as individual bone fragments in the cave bottom. Person et al.  suggested that cave deposits offer the most favorable conditions for the preservation of original crystallinity. These facts suggest that the local conditions were key postdiagenesis parameters for the changes in the CI and C/P ratio.
It has described here a bone assembly excavated from an Eoholocene deposit in northeast Brazil. The excavation at the GUF entrance cave allowed distinguishing eight layers composed of nonconsolidated sediments and very fossiliferous, especially with bones of small to medium size individuals, whose estimated age is approximately 8,200 years BP.
The biostratinomic characteristics observed in the field and in laboratory include the disarticulation and fragmentation of carcasses. The low concentrations of Fe and S indicated by the XRF analyses also demonstrated a very low degree of decomposition of the bones. The fossil diagenesis is represented by the following characteristics: (i) preservation of the biomineralization and (ii) a high incidence of incrustation (both analyzed by XRD and IR).
The Crystallinity and C/P ratio seem to be related to the local taphonomical conditions. The C1 sample clearly shows a correlation between the increase in C/P ratio and the decrease of crystallinity indices; however, there are no great disparities among the other samples, which suggests that the bones remained in a closed system for long time, and it was not possible to confirm the number of different species.
The data used to support the findings of this study are available from the corresponding author upon request.
Conflicts of Interest
The authors declare that they have no conflicts of interest.
The authors are grateful to D. Lima (COOPTUR), G. C. Oliveira (UFPE), T. A. Lima (UVA), and A. D. A. Sousa (UFCE) for their support during fieldwork, and this work received support from CNPq (#142942/2010-3) for Doctoral Fellowship (PVO). J. H. Silva acknowledges the support from the BPI-Notice no. 09/2015 and the CHAMADA UNIVERSAL MCTI/CNPq no. 014/2015. The authors would also like to thank Ms. Jessica Fitzgerald, Chemical Engineering Writing Consultant at Northeastern University, and Professor Anderson Lobo for providing English language corrections.
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P. V. Oliveira, (1) M. S. S. Viana, (2) O. A. Barros, (3) P. T. C. Freire, (4) F. I. Bezerra, (3) S. B. S. Gusmao, (5) B. C. Viana (iD), (5,6) and J. H. Silva (iD) (7)
(1) Universidade Federal do Piaui, Campus Senador Helvidio Nunes de Barros, 64607-670 Picos, PI, Brazil
(2) Universidade Estadual Vale do AcaraU (UVA), 62010-290 Sobral, CE, Brazil
(3) Pas-Graduagao em Geologia (PPGG), Universidade Federal do Ceara (UFC), 60455-760 Fortaleza, CE, Brazil
(4) Departamento de Fisica, Universidade Federal do Ceara, 60455-970 Fortaleza, CE, Brazil
(5) Pos Graduagao em Ciencias e Engenharia dos Materiais (LIMAV), Universidade Federal do Piaui, 64049-550 Teresina, PI, Brazil
(6) Departamento de Fisica, Universidade Federal do Piaui, 64049-550 Teresina, PI, Brazil
(7) Centro de Ciencias e Tecnologia-CCT, Universidade Federal do Cariri, 63048-080 Juazeiro do Norte, CE, Brazil
Correspondence should be addressed to B. C. Viana; firstname.lastname@example.org and J. H. Silva; email@example.com
Received 21 May 2018; Revised 21 August 2018; Accepted 28 August 2018; Published 3 October 2018
Academic Editor: Vincenza Crupi
Caption: Figure 1: Map of South America, showing the Ceara state and the Ubajara town. Modified from Oliveira et al. .
Caption: Figure 2: Schematic section showing the stratigraphic distribution of fossils in the GUF's entrance chamber .
Caption: Figure 3: XRD diffractograms of the bone samples from the layers C1, C2, C3, and C4 analyzed, where peaks of hydroxyapatite (*) ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]) and calcite (#) (CaC[O.sub.3]) are assigned.
Caption: Figure 4: XRD diffractograms of bone samples analyzed. Results of the samples from the layers C5, C6, and C8, where peaks of hydroxyapatite (*) ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]) and calcite (#) (CaC[O.sub.3]) are observed.
Caption: Figure 5: Infrared spectra of bone samples analyzed. Results of the samples from the layers C1, C2, C3, and C4, where peaks of hydroxyapatite (*) ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]) and calcite (#) (CaC[O.sub.3]) are observed.
Caption: Figure 6: Infrared spectra of bone samples analyzed. Results of the samples from the layers C5, C6, and C8, where peaks of hydroxyapatite (*) ([Ca.sub.10][(OH).sub.2][(P[O.sub.4]).sub.6]) and calcite (#) (CaC[O.sub.3]) are observed.
Table 1: Chemical elemental percentage of the C1, C2, C3, C4, C5, C6, and C8 samples measured by XRF. Chemical C1 C2 C3 C4 C5 C6 C8 elements (%) Ca 69.45 82.20 86.67 83.80 82.03 83.17 82.13 P 8.39 10.76 9.33 10.00 13.34 13.56 14.82 Fe 0.43 0.35 0.00 0.54 0.68 0.35 0.27 S 0.12 0.09 0.19 0.14 0.42 0.67 0.31 Al 0.15 -- 0.09 0.17 0.59 -- -- Cl 0.48 0.27 0.44 0.24 0.13 0.26 0.45 K 0.47 0.54 0.21 0.28 0.27 0.26 0.46 Mn -- 0.13 -- 0.24 0.21 -- 0.16 Si 0.36 0.46 -- 0.62 1.93 1.30 1.01 Sr 2.31 4.58 2.34 2.24 0.19 0.18 0.18 Zn 0.49 0.21 -- 0.41 0.10 0.12 0.10 Table 2: Size of the crystallite obtained in accordance with to the Scherrer equation, using the (002) diffraction plane of hydroxiapatite. Samples 2[theta] ([degrees]) (2[theta]) Crystallite Peak (002) FWHM size (nm) C1 30.34 0.526 14 C2 30.30 0.222 40 C3 30.30 0.396 20 C4 30.36 0.357 23 C5 30.25 0.193 48 C6 30.26 0.282 30 C8 30.27 0.254 34 Table 3: Average crystallinity index ([CI.sub.X-ray]) and relative carbonate/phosphate relative amount. Samples [CI.sub.X-ray] Carbonate/phosphate (%) (average) C1 0.25 32.87 C2 0.87 11.42 C3 0.47 16.50 C4 0.68 12.47 C5 0.82 18.39 C6 0.79 14.87 C8 0.78 14.85
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|Title Annotation:||Research Article|
|Author:||Oliveira, P.V.; Viana, M.S.S.; Barros, O.A.; Freire, P.T.C.; Bezerra, F.I.; Gusmao, S.B.S.; Viana, B|
|Publication:||Journal of Spectroscopy|
|Date:||Jan 1, 2018|
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