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Article

Fossil Resins–Constraints from Portable and Laboratory Near-infrared Raman Spectrometers

by
Beata Naglik
1,*,
Maja Mroczkowska-Szerszeń
2,
Magdalena Dumańska-Słowik
3,
Lucyna Natkaniec-Nowak
3,
Przemysław Drzewicz
4,
Paweł Stach
3 and
Grażyna Żukowska
5
1
Polish Geological Institute-National Research Institute, Upper Silesian Branch, 1 Królowej Jadwigi Str., 41-200 Sosnowiec, Poland
2
Oil and Gas Institute-National Research Institute, 25A Lubicz Str., 31-503 Krakow, Poland
3
Faculty of Geology, Geophysics and Environmental Protection, AGH University of Science and Technology, 30 Mickiewicz Av., 30-059 Krakow, Poland
4
Polish Geological Institute-National Research Institute, 4 Rakowiecka Str., 00-975 Warsaw, Poland
5
Faculty of Chemistry, Warsaw University of Technology, 3 Noakowskiego Str., 00-664 Warsaw, Poland
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(2), 104; https://doi.org/10.3390/min10020104
Submission received: 6 December 2019 / Revised: 15 January 2020 / Accepted: 17 January 2020 / Published: 25 January 2020
(This article belongs to the Special Issue Modern Raman Spectroscopy of Minerals)
Browse Figures
Versions Notes

Abstract

:
Comparative studies of fossil resins of various ages, botanical sources, geological environments, and provenience were provided via a handheld portable Near-Infrared (NIR)-Raman spectrometer and benchtop instrument both working with laser line 1064 nm. The recorded Raman spectra of individual fossil resins were found to be sufficiently similar irrespective to the device type applied, i.e., handheld or benchtop. Thus, the portable equipment was found to be a sufficient tool for the preliminary identification of resins based on botanical and geographical origin criteria. The observed height ratio of 1640/1440 cm−1 Raman bands did not correlate well with the ages of fossil resins. Hence, it may be assumed that geological conditions such as volcanic activity and/or hydrothermal heating are plausible factors accelerating the maturation of resins and cross-linking processes.

1. Introduction

Fossil resins are sticky plant secretions that harden on atmospheric exposure over time, and have been found within coal or other sedimentary rocks. They were formed tens of millions of years ago through the diagenetic or catagenetic transformations of plant exudates induced by various geochemical processes. From a chemical point of view, they are water-insoluble complex mixtures of organic compounds such as terpenes, terpenoids and their derivatives [1,2,3,4,5]. Occurring in various worldwide localities, fossil resins are incorporated in geological layers spanning in age from the Triassic to Cenozoic [6,7]. They differ from one deposit to another in terms of physicochemical properties (appearance) as well as the presence of organic and inorganic inclusions. These differences reflect the evolutionary history of the resins from the initial botanical source to the present, fossil form. Besides that, the exudates from the same botanical source sometimes undergo different fossilization processes resulting in the formation of many varieties of fossil resins. Among the huge number of resin types, the succinite (Baltic amber), containing succinic acid, remains the most frequently studied [8,9,10,11,12,13].
Since the mid-twentieth century, Fourier Transform Infrared Spectroscopy (FT-IR) has become a fundamental method for classification and origin interpretation of fossil resins [14,15,16,17,18]. However, the diagnostic significance of the FT-IR technique became disputable since the characteristic spectral pattern within the diagnostic absorption range of 1250–1150 cm−1 (known as the “Baltic shoulder”) was also observed in samples other than Baltic ambers [19]. Lately, the comprehensive approach to the investigation of fossil resins has become more complex due to the availability of various advanced analytical methods adopted from chemical and physical sciences [17]. Although many instrumental techniques have become successfully employed in fossil resin studies, i.e., scanning electron microscopy with electron dispersive spectroscopy [12,20,21], Raman microspectroscopy [19,22,23,24,25,26,27,28,29,30,31,32,33,34,35,36,37], gas chromatography-mass spectrometry (GC-MS) [38,39], Nuclear Magnetic Resonance spectroscopy (NMR) [40,41,42], thermal analysis [43,44,45] and microhardness testing [46,47], the unambiguous identification and classification of fossil resins is still a very challenging task. Some doubts regarding fossil resin origin, their botanical affinities, alteration in the geological environment still exist, and some knowledge gaps require explanation, i.e., the fossilization mechanisms pathways. Therefore, the development and the application of various analytical methods in fossil resin investigation together with a geological, palaeogeographical and palaeoclimatic background is crucial for understanding fossilization processes as well as geological and environmental conditions associated with the transformation of resins from plant exudates to present, fossil forms.
Recently, Raman spectroscopy with an excitation wavelength of 1064 nm and using benchtop equipment [22,23,24,25,26,28,29,30,33,35,37], as well as a portable technique [33] was successfully applied in research of fossil resins. The main advantage of this method over FT-IR was the easy sample preparation and nearly non-destructive character of the measurements [22,36]. Moreover, Raman microspectroscopy is suitable for analysis of the aromatic or unsaturated compounds, characteristic bands such as C=C stretching, having weak intensity in FT-IR and being additionally overlapped by much stronger bands related to the C=O stretching vibrations [36].
The identification of molecular spectral features of resins, which might allow for discrimination between specimens coming from different geographical locations was undertaken by many authors [23,27,28,37]. It has still remained a challenging task since the fossil resins, in the course of their maturation process, are affected by degradation processes to various degrees, which in consequence leads to the resetting of their spectroscopic fingerprints [19]. However, some fossil resins could still be easily recognized using Raman spectroscopy, i.e., Borneo amber [19] or siegburgite [26]. Raman spectroscopy was found to provide information about the chemical structure of the resins, such as the presence of cyclohexane/cyclopentane derivatives, aromatic rings as well as exocyclic CH2 and CH3 groups [48]. As the process of fossil resins degradation might affect the shape of their Raman spectra [19], Raman spectroscopy has been commonly used for assessments of the maturation degree of fossil resins that, in turn, may be correlated with the age of the specimens [24,25], geological setting of the deposit as well as redox, temperature and pressure conditions during fossilization [25,28]. Additionally, Raman spectroscopy has already been reported as a successful technique for studies of amber-hosted animal inclusions [19], archaeological objects [27,29] as well as differentiation between amber, copal (immature resins) and colophony [34]. In many cases, preliminary gemmological analyses of fossil resins and their quick identification by the spectrometric method might be sufficient for their authenticity confirmation. Further possibilities result from the use of portable, handheld equipment, which could be very useful, especially in field works, out of a laboratory [26]. The applicability and limits of using a portable Raman spectrometer in mineralogical investigations were discussed recently by Jehlička et al. [31,32] who recommended portable Raman instruments for the fast and easy identification of minerals in the field. On the other hand, the unsatisfactory quality of Raman spectra (low resolution, high background noise and limited signal processing capabilities) is the main drawback that should be considered in choosing between application of the portable and laboratory equipment in the research. Jehlička et al. [31,32] performed an investigation using Raman spectrometers with 785 nm excitation laser line that frequently causes fluorescence interferences resulting in poor quality of obtained spectra of fossil resins. The problems associated with fluorescence of samples could be avoided by using Near-infrared Raman spectroscopy [22,33]. The laboratory Raman spectrometers with 1064 nm laser line have been available for a long time, but portable equipment has been introduced to the market only quite recently.
In our contribution, ten fossil resins (Figure 1) of various age (from Cretaceous to Miocene), worldwide localities (Ethiopia, Russia, Myanmar, Mexico, the Dominican Republic, Borneo, Sumatra), and botanical sources (Araucariaceae/Pinaceae/Cupressaceae, Cupressaceae/Taxodiaceae, Hymenaea, Dipteropcarpus, Dipterocarpacea) were investigated with both handheld and laboratory equipment using 1064 nm laser line excitation. Based on NIR-Raman spectral characteristics, the resins were grouped to compare their age, botanical and geographical origin as well as environmental and geological conditions occurring during their formation and alteration. Finally, the potential for portable NIR-Raman spectroscopy as a tool for rapid and non-destructive fossil resins identification and classification is discussed in detail.

2. Experimental

2.1. Sampling

The samples subjected to analysis came from a great collection of fossil resins of Günter Krumbiegel, who was a German geologist and palaeontologist [49]. The specimen’s characteristics containing the information on localities, botanical sources and geological environments of deposition as well as detailed data on alterations during diagenesis and/or catagenesis are summarized in Table 1. To provide a correlation between the resins NIR-Raman spectra and their geological backgrounds, only specimens that were not subjected to the redeposition or which provenience was known were used for the study. The oldest resins of the Cretaceous age were considered as non-redeposited.

2.2. Analytical Methods

NIR-Raman spectra of the resins were recorded with two different spectrometers, i.e., handheld and benchtop, to verify the results and indicate the most reliable and informative measuring ranges, especially for the portable Raman instrument. The handheld device was Rigaku Progeny ResQ model equipped with a InGaAs detector device. The tests were feasible thanks to the courtesy of Tusnovics Instruments Ltd., Krakow (Poland). Another instrument was a laboratory grade Thermo Fisher Scientific NXR 9650 FT-Raman module, (Thermo Fisher Scientific, Madison, WI, USA). Both spectrometers worked with 1064 nm laser line excitation and the same detector type.
The Rigaku dispersive spectrometer was equipped with Nd:YAG laser of maximum power value of 490 mW. The spectra were recorded in the range of 2000–200 cm−1. The results were collected from at least three different analytical points on flat clean surfaces of samples. The spectra obtained differed slightly only in signal intensity. In the case of a portable Raman spectrometer, the sample was held in the hand and short scanning time was needed to obtain undisturbed spectra. Therefore, spectra were obtained from 10 scans with the resolution 8–11 cm−1 as a compromise between scanning time and spectrum quality. Laser power was optimized for the samples and no burn and/or carbonization of the samples were observable under the microscope (MOTIC SNZ-168, Xiamen, China). Raman spectra were baseline corrected and normalized for ease of comparison purposes. The normalized procedure was performed with respect to the most intense band in the range (band with maximum ~1440 cm−1). The baseline correction was an automatic function of the portable device.
The Thermo Electron FT-Raman device uses Nd:YVO4 laser of a maximum power up to 2.5 W, and XT-KBr beam splitter, gold plated mirrors and 180 degrees reflective accessory for samples acquisition. Each spectrum was acquired in the same analytical conditions. 3200 scans were collected and averaged for each spectrum. Such a high number of repetitions is frequently chosen by spectrometrists in the case of weakly scattering samples measured by Fourier Transform Raman spectroscopy. The selected resolution was 4 cm−1 with a spectral range from 3700 cm−1 to 150 cm−1. The laser power on the sample was optimized and finally set below 300 mW, to avoid thermal effects on the sample.

3. Results and Discussion

3.1. Comparison between NIR-Raman Portable, Handheld vs. Laboratory Benchtop Device for Fossil Resins Characterization

The quality of the Raman spectra of fossil resins seems to depend on many parameters, i.e., number of scans, laser power, and signal processing. In the case of an organic material, application of the high energy laser used to obtain Raman spectra might result in thermal alteration of the investigated samples. Therefore, a compromise between laser power and several scan repetitions was reached to obtain a reasonable signal-to-noise ratio in the recorded Raman spectra. The collection and superposition of many scans is a very lengthy process and it can be done by laboratory-grade equipment. In portable, handheld, Raman spectrometers, the duration of the measurement is very limited thus the equipment is considered to be less sensitive than lab equipment. Despite these limitations, it was previously shown that the Baltic amber produces very similar NIR-Raman spectra, irrespective of spectrometer type, i.e., portable or lab instrument [33]. In our work, the compatibility of Raman spectra between a lab, and handheld equipment was also quite good; however, in the case of the portable spectrometer, only the most intense signals could be unambiguously assigned as characteristic Raman bands of functional chemical groups. The positions of the strongest peaks were almost identical on spectra collected from both instruments, as well as the bands shapes in this case. In consequence, despite the difference of the spectral resolution between these two devices, it was possible to distinguish the main amber types. However, differences were found in the relative band intensities, especially for ~1650 cm−1 and ~1450 cm−1 lines (Figure 2, Figure 3, Figure 4 and Figure 5). Moreover, the Raman spectra collected from the laboratory instrument was a little bit more detailed, and more reliable especially in the region <800 cm−1.

3.2. Fossil Resins Grouping Based on Criteria of Geographical Origin and Botanical Source

The wavenumber positions of the bands in NIR-Raman spectra of the fossil resins collected with a handheld device is listed in Table 2 with their tentative assignments. In general, spectral profiles depend mostly on geographical locations of the samples, their botanical sources as well as maturation grade and geological conditions of their alterations.
The most distinctive Raman spectra were obtained for resins from Sumatra and Borneo Islands. They differed from other resins due to the absence of the peak at 1200 cm−1 that is usually assigned to δCCH modes of terpenoids [28] or δCOH [23]. Moreover, the extra band at 800 cm−1 was only present in the spectra of resins from Sumatra and Borneo (Figure 6). It could be attributed to aromatic hydrocarbon deformations [27], where its presence would explain the strong luminescence properties of these resins. The Indonesian resins were associated with coal horizons (Table 1), and thus they were probably susceptible to aromatization processes during their fossilization [74]. The presence of the aromatic compounds in the chemical profile of Sumatran fossil resins was confirmed with use of the GC-MS technique. In addition to cyclic compounds from the sesquiterpenoids group, aromatics were present in the form of Cadina-1 (10),6,8-triene (α-Calamine) and Cadina-1,3,5-triene (L-calamenene). The results are planned to be published in the frame of another paper. On the other hand, specific Raman spectra of Indonesian resins could be explained by their different botanical precursors (Dipterocarpaceae family source) as previously concluded by Edwards et al. [19]. The presence of aromatic compounds has also been revealed for Russian resin from Sakhalin Island, which was altered under catagenetic conditions (Table 1). The presence of a band at 1610 cm−1, which could be attributed to ν(C=C) aromatic [24], suggests that aromatization was a significant part of the maturation process of this resin type. The presence of aromatic compounds in Sakhalin resin has been previously documented due to the GC-MS data by Bechtel et al. [75]. It stays in correlation with the fact that aromatization is one of the most important reactions occurring in organic matter during catagenesis [28].
Despite the similar botanical sources (Hymenaea) and age (Miocene), the resins from the Dominican Republic differ from Mexican specimens (Figure 6) mainly due to the presence of a characteristic triplet found at 747, 724 and 695 cm−1 maxima (Figure 3 and Figure 6). These bands have been previously observed by Brody et al. [24] with the use of a laboratory, benchtop device. Now, for the first time, their presence is also confirmed by means of the portable, handheld instrument. These spectral differences might reflect variations of resins source plants at the species level. Likely, the Mexican resins were produced by extinct H. Mexicana [76] and/or H. allendis species [77], while Dominican species were probably formed from exudates of H. verrucos [78] as evidenced from FT-IR and 13C NMR spectroscopic methods [78]. In turn, Mexican and Ethiopian resins exhibit a great similarity in their NIR-Raman spectra characteristics. Specimens from Ethiopia, that have been already discovered [50], remain one of the less known fossil resins of Cretaceous [50] or Miocene age [79]. The genus Hymenaea has been proposed as a botanical source of Ethiopian resins [79] based on the organic inclusions data as well as chemical composition revealed by the use of solid phase microextraction gas chromatography-mass spectrometry [80]. On the basis of Raman spectroscopy, the similarity between Ethiopian and Mexican fossil resins could be found. As a result, the origin of Ethiopian resin from Hymenaea could be concluded.
Although spectra obtained from the portable Raman spectrometer allowed for the observation of only the most intense bands, a preliminary identification of the botanical source and fossil resins grouping seemed to still be possible with the application of this technique. Such portable equipment might be therefore used for preliminary screening of the material and selection of more advanced techniques with the use of laboratory spectrometers or other instrumental methods (i.e., GC-MS, thermal analysis).

3.3. Fossil Resins Grouping Based on Age/Maturation Grade Criteria

The process of fossil resin maturation is initiated at the time of the exudation under hypergenic conditions influenced by sun heating, and the temperature of the surrounding environment [7]. Further alteration of fossil resins could be very slow and gradual; however, it might also be accelerated by forest fires or geological events, e.g., volcanic activity, an increase in temperature due to burial conditions or the development of orogens. During fossilization, the resins have undergone many chemical processes, such as aromatization, catenation, compound cross-linking and dehydrogenation induced by various environmental and geological conditions [7,28].
Along with the maturation process, penta- and hexacyclic rings in terpenoids undergo aromatization. The degradation of fossil resins results in loss of v(C=C) non-aromatic unsaturation, which is marked by the lower intensity of the band at 1640 cm−1 compared with 1440 cm−1 [25]. Thus, the intensity ratio bands I(1640/1440) has been proposed as an indicator of the maturation degree of organic matter, especially for fossil resins [25]. Although the assignment of these two bands is still disputable, one may assume, based on previous studies, that the 1440 cm−1 band is characteristic of vibration in CH2 groups, and the 1640 cm−1 band is due to C=C stretching vibration [25]. Additionally, the presence of a broad band at ~714 cm−1 was previously interpreted as an indicator of the resin’s maturation grade [28].
The application of an I(1640/1440) indicator for assessment of fossil resins age has been frequently carried out despite the fact that the maturation of fossil resins is not only a function of time but is strongly dependent on their burial history [e.g., 25,28]. The botanical source of the resins and their primary environment also play an important role in the maturation process pathways [28]. The presented results confirm that assessment of resin age based on the height ratio of 1640/1440 cm−1 is very difficult or even impossible, as any correlation between the resins characteristic and their calculated height ratio of 1640/1440 cm−1 was found in our research (Figure 6, Table 3). However, the maturation grade of the resins could be revealed when their geological background is taken into consideration. It was concluded that the temperature conditions of the resin burial had the greatest influence on fossilization processes, while volcanism seemed to be the most important geological factor that determined not only the production of resins [81] but also their alteration rate affected by heating. Fossil resins that underwent alteration controlled by the volcanic heating showed a lower height ratio of 1640/1440 cm−1 than expected from their geological age (i.e., resins from Sumatra and Myanmar, vide Table 1). Probably thermal or/and hydrothermal processes associated with the volcanic activity may cause partial oxidation or breaking of double bonds in compounds present in these resins. The pressure-temperature (p-T) conditions of diagenesis also influence the polymerization degree of the resins. The relatively young resin from Sakhalin Island (Russia), which showed a height ratio of 1640/1440 cm−1 close to the Cretaceous resins from Myanmar and Khatanga (Russia) (Figure 2, Figure 3, Figure 4, Figure 5 and Figure 6), occurring in quartzite layers (Table 1), was likely altered due to the catagenic or oxidation processes, which, in turn, diminished the number of unsaturated bonds. Those results stay in correlation with thermal analysis [82] performed on Sumatran and Russian specimens, which confirmed that those resins were subjected to elevated p-T conditions. Another unexpected result was obtained for Ethiopian fossil resins. Their height ratios of 1640/1440 cm−1, as being indicative for low polymerization degree, might confirm younger than the Cretaceous age of these specimens [51,80]; however, geological data also suggest low temperature conditions of their diagenesis.
Further problems with the application of the height ratio of 1640/1440 cm−1 for proper assessment of resins age/maturation grade arises from differences in bands intensity between handheld measurements and a laboratory grade Raman device, which might be explained by different spectral resolutions. As always in the case of the preparation of analytical methods, one needs to have very well-defined rules in order to prepare reproducible spectra. Otherwise, investigators would have a problem with interpretation and comparison of spectra reported in literature.
To sum up, the height ratio of 1640/1440 cm−1 cannot be used as a general approach to resins dating, however, it still might have application for comparison of the age of samples altered under the same or similar pressure-temperature conditions in host deposits and from the same kind of botanical sources. The combination of this index with other, independent analytical techniques might provide new indicators of resins age irrespective of their provenance and geological history. FT-Raman spectroscopy coupled with a chemometric analysis has been already performed by Peris-Diaz et al. [37] presenting quite a good result of PLS (partial least squares classification analysis) according to resins age (Cretaceous and Cenozoic periods). Beltran et al. [36] performed Raman and IR spectroscopic analysis of resin specimens coming from Pinus, and pointed out characteristic compounds of fresh and aged samples. However, further effort should be done to find indicators of fossil resins polymerization degree with respect to their burial conditions, not the ageing itself. Moreover, the height ratio of the bands with maxima near 1640 cm−1 and 1440 cm−1 cannot be considered as an indicator of resins maturation grade until restrictive rules regarding data collection and processing are defined.

4. Conclusions

  • The Raman spectra of fossil resins, coming from various worldwide localities, and differing in age, botanical source, history of evolution and geological background, obtained with handheld, portable NIR-Raman spectrometer were very similar to these collected with a more advanced, benchtop Raman instrument. The only differences were found in the spectral region <800 cm−1, and locally in the intensities of some Raman bands.
  • The differentiation of fossil resins of the same age and botanical source, coming from various geographical localities with Near infrared Raman spectroscopy is possible for samples coming from the Dominican Republic and Mexico (Miocene, Hymenae), but out of the question for specimens from Sumatra and Borneo (Miocene, Dipterocarpaceae). On the other hand, similar spectral features obtained for specimens of various ages and geographical localities may result from the same botanical source, as noted for resins coming from Ethiopia and Mexico. Hence, it was found that spectral features which reflect the chemical composition of fossil resins seem to depend mainly on their botanical source. Other factors affecting the features of Raman spectra are strongly connected with the alteration and maturation processes of the fossil resins.
  • There was no direct correlation between the height ratio of 1640/1440 cm−1, which is commonly regarded as indicator of maturation grade, and fossil resins age. Interestingly, specimens of the same age (e.g., Dominican and Sumatran resins both of Miocene age) showed a different 1640/1440 cm−1 height ratio index, caused probably by the alterations under various temperature and pressure conditions. Hence, it was concluded, this 1640/1440 cm−1 height ratio index can provide additional data on geological events proceeding from the time of exudation through transportation, deposition in sedimentary basin to exhumation and re-exposure to hypergenic conditions, and thus will reflect the evolutionary history of resins.

Author Contributions

B.N., M.M.-S., M.D.-S., L.N.-N. and P.D. designed the experiments, interpreted the data and wrote the paper. M.M.-S., P.S. and P.D. performed the experiments and prepared figures and photographs. G.Ż. substantively revised the first version of the manuscript. All authors have read and agreed to the published version of the manuscript.

Funding

The work was financially supported by AGH University of Science and Technology (Krakow Poland), grant No 16.16.140.315 and the Polish Geological Institute-National Research Institute, research project No. 61.9012.1908.00.0.

Acknowledgments

Anselm Krumbiegel is acknowledged for providing specimens of fossil resin for the research. Rastislav Milovsky is acknowledged for providing GC-MS data for the Sumatran resin. We thank the anonymous reviewers for their constructive comments and the editor for handling the paper.

Conflicts of Interest

The authors declare no conflicts of interest.

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Minerals 10 00104 g001a 550Minerals 10 00104 g001b 550
Figure 1. Macrophotos of fossil resins: (A)—Khatanga, Russia; (B)—Alem Ketema, Ethiopia; (C)—Hukawng valley, Myanmar; (D)—Sakhalin, Russia; (E)—Sumatra (Palembang Province), Indonesia; (F)—Sumatra (Jambi Province), Indonesia; (G)—Chiapas, Mexico; (H)—Santiago de los Caballeros, Dominican Republic; (I)—El Valle, Dominican Republic; (J)—Sarawak, Borneo, Malaysia.
Figure 1. Macrophotos of fossil resins: (A)—Khatanga, Russia; (B)—Alem Ketema, Ethiopia; (C)—Hukawng valley, Myanmar; (D)—Sakhalin, Russia; (E)—Sumatra (Palembang Province), Indonesia; (F)—Sumatra (Jambi Province), Indonesia; (G)—Chiapas, Mexico; (H)—Santiago de los Caballeros, Dominican Republic; (I)—El Valle, Dominican Republic; (J)—Sarawak, Borneo, Malaysia.
Minerals 10 00104 g001aMinerals 10 00104 g001b
Minerals 10 00104 g002 550
Figure 2. Comparison of Raman spectra of fossil resin from Sakhalin (Russia) collected with laboratory (A) and handheld (B) equipment.
Figure 2. Comparison of Raman spectra of fossil resin from Sakhalin (Russia) collected with laboratory (A) and handheld (B) equipment.
Minerals 10 00104 g002
Minerals 10 00104 g003 550
Figure 3. Comparison of Raman spectra of fossil resin from Dominican Republic (Santiago de los Caballeros) collected with laboratory (A) and handheld (B) equipment.
Figure 3. Comparison of Raman spectra of fossil resin from Dominican Republic (Santiago de los Caballeros) collected with laboratory (A) and handheld (B) equipment.
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Minerals 10 00104 g004 550
Figure 4. Comparison of Raman spectra of fossil resin from Myanmar collected with laboratory (A) and handheld (B) equipment.
Figure 4. Comparison of Raman spectra of fossil resin from Myanmar collected with laboratory (A) and handheld (B) equipment.
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Minerals 10 00104 g005 550
Figure 5. Comparison of Raman spectra of resin from Khatanga (Russia) collected with laboratory (A) and handheld (B) equipment.
Figure 5. Comparison of Raman spectra of resin from Khatanga (Russia) collected with laboratory (A) and handheld (B) equipment.
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Minerals 10 00104 g006 550
Figure 6. Raman spectra of fossil resins, arranged from the oldest to youngest, collected with hand-held equipment. Fossil resins of a similar botanical source have been underlined through the use of specific colour lines.
Figure 6. Raman spectra of fossil resins, arranged from the oldest to youngest, collected with hand-held equipment. Fossil resins of a similar botanical source have been underlined through the use of specific colour lines.
Minerals 10 00104 g006
Table
Table 1. Detailed characterization of investigated fossil resins.
Table 1. Detailed characterization of investigated fossil resins.
Sample LabelAgeBotanical OriginGeological SettingsSamples Description
Ethiopialate Cretaceous (late Cenomanian) 93–95 Ma [50
or
Cenozoic (likely Miocene?) [51]		Unknown [50]Resins occur within Debre Libanos Sandstone Unit (DLSU) from the northwestern Plateau [50]. DLSU represents continental, alluvial to fluvial depositional environment. It consists of medium to coarse grained sandstones showing dune-scale trough cross-bedding and horizontal stratifications. The DLSU unit was deposited during the NE–SW-directed extension related to Mesozoic rifting of Gondwana [52]. Those deposits are overlaid by Early-Late Oligocene volcanic rocks (basalts, trachytes, rhyolites).Black colour, opacity
Russia,
Khatanga		lower Cretaceous (Aptian-Albian) 125–100.5 Ma [53]/ upper Cretaceous (Santonian) 85.8 Ma [54,55]Unknown [54,56]Resins occur within Begichev Formation (Eastern Taymir) [57]. It consists of lagoon and coastal sediments of alluvial origin (sands) with interbeddings of clays, aleurites and coal horizons [53].Red to brown colour, transparency
Myanmar
(Burma)		upper Cretaceous (Cenomanian?/Turonian?)
93.5 Ma [58]		Araucariaceae/
Pinaceae/
Cupressaceae [59]		Amber-bearing sediments are clastic sedimentary rocks ranging from fine sandstones to shales. The amber discs lie parallel to the bedding planes of finer sediment [60]. Volcanic event dated on Cenomanian is reflected in the presence of volcanic clasts.Red to brown colour, transparency
Russia,
Sakhalin Island		middle Eocene 43–47 Ma [61]; Paleocene–65.5 Ma [53]Ancient species of the gymnosperm families Cupressaceae/
Taxodiaceae [53]		Quartzite altered at the p-T conditions of catagenesis [53]Red to brown colour, transparency, shape of flat discs
Mexico,
Chiapas		lower Miocene–middle Miocene
22.5–26 Ma [62]		Extinct Hymenaea mexicana [62]Resins occur within three lithostratigraphic formations: Marine calcareous sandstones and silt with beds of lignite–the Early Miocene Quinta or Simojovel Fm, the Lower Middle Miocene dark-grey shales of the Mazantic Shale, Lower Miocene grey-blue to grey-green sandstones of the Balumtun Fm [62]Yellow to brown colour, transparency
Dominican Republic (Cordillera Oriental)
El Valle 		lower Miocene–middle Miocene
15–20 Ma [63]		Hymenaea [64,65]The Yanigua Formation is the amber-bearing unit of the eastern area of the Dominican Republic. Formation consists of conglomerates, dark clays, laminated sandy clays, lignite and carbonaceous clays and sandstones. These beds contain flattened and irregular inclusions of amber, usually as pockets or lenses ranging from a few millimeters to several centimeters in size, and may also contain freshto brackish water ostracods and molluscs [64,66]Yellow to brown colour, transparency, visible strong blue fluorescence
Dominican Republic (Cordillera Septentrional
Santiago de los Caballeros)		late Oligocene-early Miocene
20–25 Ma
[64,65]		Hymenaea [64,65]The La Toca Formation is the second amber-bearing unit of the northern part of the Dominican Republic. Its thickness is estimated at ca. 1200 m. There are mainly clastic (conglomerates and sandstones) rocks cutting by thin lignite beds with fragments of carbonized wood. This is probably an accumulation of deposits in different environments from deltaic to deepwater [64,66,67]Yellow to brown colour, transparency, visible strong blue fluorescence
Borneo,
Sarawak,
Malaysia		Neogene/ Miocene;
middle Miocene
15–17 Ma [55]		Dipterocarpus [55]During the earliest Middle Miocene volcanic activity increased.
Merit Pila amber was formed together within a layer of brown coal in the Nyalau Formation (NF). The unit consists of sandstones, coal layers and conglomerates. These sediments were deposited under humid tropical conditions. Amber was formed in a damp swamp surrounded by mountainous terrain. Deposition occurred in the lake and wetland flooded by sea water [68,69]		Yellow to brown colour, transparency, visible blue fluorescence
Sumatra, Jambi,
Indonesia		lower Miocene-middle Miocene
15–23 Ma [70,71]		Dipterocarpaceae family belonging to angiosperms group [70,71]Resins occur in coal layers (lignite beds) within middle Miocene sediments representing the transgressive depositional system of Talang Akar Formation (TAF). Sediments were uplifted, folded and faulted due to the Pliocene-Pleistocene orogeny associated with volcanic activity [72,73]Yellow to brown colour, transparency, visible strong blue fluorescence
Sumatra, Palembang, Indonesialower Miocene −23 Ma [70,71]Dipterocarpaceae [70,71]Yellow to brown colour, very strong blue fluorescence
Table
Table 2. NIR-Raman bands (cm−1) for the analysed resins and their tentative assignment.
Table 2. NIR-Raman bands (cm−1) for the analysed resins and their tentative assignment.
EthiopiaRussia (Khatanga)MyanmarRussia (Sakhalin Island)Mexico (Chiapas)Dominican Republic
(El Valle)		Dominican Republic
(Santiago de los Caballeros)		Borneo
(Sarawak)		Sumatra
(Jambi) 		Sumatra
(Palembang)		Proposed Band Assignment
-----371----δ(CCC) [24]
444---445439----unknown
-497503-------ν(COC) [24]
555---554-----δ(CCO) [24]
-----695695---ν(CC)isolated [24]
720720723708718720724732731733νC-C [25]
-----744747---ν(CC)isolated [24]
-------800799800aromatic hydrocarbonsdeformations [27]
1201120212031205120312021201---δ(CCH) [24]
12991292129912951296--131513161316δ(CH2), δ(CH3) [24]
---1349-----1330δ(CH2), δ(CH3) [24]
13601354135113721357--13601360-δ(CH2), δ(CH3) [24]
1443145014491443144214421462/1438144914421442δ(CH2), δ(CH3) [24]
---1610------ν(C=C)aromatic [24]
1652164916561649165316581642165716571657ν(C=C) non conj. [24]
Table
Table 3. Comparison of bands height ratios I(1640/1440) calculated on the basis of portable spectrometer results.
Table 3. Comparison of bands height ratios I(1640/1440) calculated on the basis of portable spectrometer results.
AgeSample labelHeight Ratio of 1640/1440 cm−1
CretaceousEthiopia0.51 ± 0.01
CretaceousRussia (Khatanga)0.40 ± 0.06
CretaceousMyanmar0.33 ± 0.02
EoceneRussia (Sakhalin Island)0.36 ± 0.01
MioceneMexico (Chiapas)0.52 ± 0.01
MioceneDominican Republic (El Valle)0.79 ± 0.02
MioceneDominican Republic (Santiago de los Caballeros)0.66 ± 0.12
MioceneBorneo (Sarawak)0.60 ± 0.03
MioceneSumatra (Jambi)0.44 ± 0.06
MioceneSumatra (Palembang)0.46 ± 0.02

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Naglik, B.; Mroczkowska-Szerszeń, M.; Dumańska-Słowik, M.; Natkaniec-Nowak, L.; Drzewicz, P.; Stach, P.; Żukowska, G. Fossil Resins–Constraints from Portable and Laboratory Near-infrared Raman Spectrometers. Minerals 2020, 10, 104. https://doi.org/10.3390/min10020104

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Naglik B, Mroczkowska-Szerszeń M, Dumańska-Słowik M, Natkaniec-Nowak L, Drzewicz P, Stach P, Żukowska G. Fossil Resins–Constraints from Portable and Laboratory Near-infrared Raman Spectrometers. Minerals. 2020; 10(2):104. https://doi.org/10.3390/min10020104

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Naglik, Beata, Maja Mroczkowska-Szerszeń, Magdalena Dumańska-Słowik, Lucyna Natkaniec-Nowak, Przemysław Drzewicz, Paweł Stach, and Grażyna Żukowska. 2020. "Fossil Resins–Constraints from Portable and Laboratory Near-infrared Raman Spectrometers" Minerals 10, no. 2: 104. https://doi.org/10.3390/min10020104

APA Style

Naglik, B., Mroczkowska-Szerszeń, M., Dumańska-Słowik, M., Natkaniec-Nowak, L., Drzewicz, P., Stach, P., & Żukowska, G. (2020). Fossil Resins–Constraints from Portable and Laboratory Near-infrared Raman Spectrometers. Minerals, 10(2), 104. https://doi.org/10.3390/min10020104

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