Spectroscopy and Trace-Element Characteristics of Emeralds from Kamakanga, Zambia

: Currently, Zambia is the second largest source of emeralds, after Colombia. In this study, emerald samples from the Zambian Kamakanga deposit were examined by UV-Vis-NIR, Miro-FTIR, Diamond View TM , and LA-ICP-MS. Representative UV-Vis-NIR spectra showed a distinct Fe 3+ absorption peak, and the Fe-related absorption band was much stronger than that of the Cr-related absorption band. The infrared spectra showed that the absorption of type II H 2 O was much stronger than that of type I H 2 O. The results of LA-ICP-MS indicated that darker green, green, lighter green, and bluish-green emeralds had a clear separation of Cr/V (Cr/V > 15 for darker green, 10 < Cr/V < 15 for green, and Cr/V < 10 for lighter green and bluish green). In color zoning emerald, the contents of Cr, Sc, V, and Fe gradually increased with the intensity of the green color, while the opposite occurred for Cs. Cr is the main chromogenic element in Kamakanga emeralds. Additionally, Zambian Kamakanga emeralds contain high contents of total alkali metals (avg. 17,592 ppmw), Cs (avg. 1331 ppmw), Fe (avg. 8556 ppmw), Li (avg. 485 ppmw), Li + Cs (avg. 1816 ppmw), and Ga/Fe < 0.0025. Therefore, combined Fe versus Ga, Li versus Cs binary diagrams and K, Rb, and the Li + Cs ternary plot can distinguish Zambian emeralds from other important emerald origins.


Introduction
Emerald is known as the "King of Green Gemstones" and is loved for its vibrant and beautiful color, which represents hope and the arrival of spring.In recent years, the Zambian production of emeralds has gradually increased, and Zambia is now the second largest source of emeralds, after Colombia [1][2][3][4].However, compared those from Colombia, Zambian emeralds have not been systematically studied.Emerald deposits are found all over the world, and the main emerald sources are Colombia, Zambia, Brazil, Zimbabwe, Madagascar, and Afghanistan.The prices of emeralds with the same quality may differ, depending on their origins.Therefore, the market demand for identifying the origin of emeralds has gradually grown [5][6][7][8].Origin identification has become an important part of the emerald evaluation system, which includes spectroscopy and trace-element tests.
Kamakanga is an emerald deposit in the Zambian Kafubu emerald area.Although the Zambian Kafubu emerald area was discovered and mined as early as 1928, large-scale mining and systematic research did not begin until the 1970s [3,4,9,10].The deposits in this area were tentatively identified as schist-hosted, and the Zambian Kafubu area emeralds were similar to other schist-hosted emeralds around the world [11].Subsequently, a brief description of the geological setting of the Zambian Kafubu area was reported by Sliwa et al. [9].They concluded that the emerald deposits of this area are located in the ultramafic metamorphic rocks of the Muwa Supergroup, underlying the gneisses and granites of the basal mafic rocks and overlying the younger metamorphosed sedimentary rocks of the Katanga Supergroup [9].The first geochemical and mineralogical data from the Kafubu emerald area were reported by Seifert et al. [2].They concluded that mineralization of the Kamakanga emerald deposit occurred at 447 ± 8.6 Ma [2].
Emerald mineralization in the Kamakanga deposit is directly related to the metasomatic alteration of Cr-bearing metabasites by Be-bearing fluids in hydrothermal veins [3].The rock in the Kamakanga deposit experienced magmatic intrusion during the Pan-African orogeny and, subsequently, the Be-rich magma and its derived fluids interacted with the nearby Cr-and V-rich host rock.Ultimately, emeralds formed within phlogopite reaction zones between the quartz-tourmaline veins and the metabasites [12].Only 2% of the Zambian Kafubu emerald area is currently mined, and the Kamakanga emerald deposit is mined at the deepest depth (50-60 m).However, the results of a geological survey indicated that there are traces of emerald mineralization at a deeper level [2,4].Consequently, the Kamakanga deposit still has the potential for the discovery of large and high-quality emeralds.
In recent years, experts have collected emeralds from the Zambian Kafubu area for spectroscopy study and analysis of chemical composition [3,13], and they have compared emeralds from this area with emeralds of other origins [14][15][16][17][18][19].Actually, there are four mechanized mining deposits in the Zambian Kafubu emerald area-Kagem, Grizzly, Chantete, and Kamakanga.However, most of the research has been concentrated on the former three deposits, while few studies have been carried out on the Kamakanga deposit.
In this paper, we used an ultraviolet-visible near-infrared spectrophotometer (UV-Vis-NIR), Diamond View TM , micro-fourier-transform infrared (Micro-FTIR) spectroscopy, and a laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) to analyze emeralds from the Zambian Kamakanga deposit, so as to provide a more comprehensive scientific basis for identifying the origins of emeralds and to summarize and supplement the latest data.

Materials
Thirteen emerald samples (ZAKA-1 to ZAKA-13) were investigated from the Kamakanga deposit in Kafubu area, Zambia (Figure 1).Emerald samples were selected from more than 300 rough emeralds that were obtained from an owner of a local mine.Emerald samples were in the form of hexagonal columns, slabs, or fragments; they were slightly transparent to transparent, and green to bluish green in color.were reported by Seifert et al. [2].They concluded that mineralization of the Kamakanga emerald deposit occurred at 447 ± 8.6 Ma [2].Emerald mineralization in the Kamakanga deposit is directly related to the metasomatic alteration of Cr-bearing metabasites by Be-bearing fluids in hydrothermal veins [3].The rock in the Kamakanga deposit experienced magmatic intrusion during the Pan-African orogeny and, subsequently, the Be-rich magma and its derived fluids interacted with the nearby Cr-and V-rich host rock.Ultimately, emeralds formed within phlogopite reaction zones between the quartz-tourmaline veins and the metabasites [12].Only 2% of the Zambian Kafubu emerald area is currently mined, and the Kamakanga emerald deposit is mined at the deepest depth (50-60 m).However, the results of a geological survey indicated that there are traces of emerald mineralization at a deeper level [2,4].Consequently, the Kamakanga deposit still has the potential for the discovery of large and high-quality emeralds.
In recent years, experts have collected emeralds from the Zambian Kafubu area for spectroscopy study and analysis of chemical composition [3,13], and they have compared emeralds from this area with emeralds of other origins [14][15][16][17][18][19].Actually, there are four mechanized mining deposits in the Zambian Kafubu emerald area-Kagem, Grizzly, Chantete, and Kamakanga.However, most of the research has been concentrated on the former three deposits, while few studies have been carried out on the Kamakanga deposit.
In this paper, we used an ultraviolet-visible near-infrared spectrophotometer (UV-Vis-NIR), Diamond View TM , micro-fourier-transform infrared (Micro-FTIR) spectroscopy, and a laser ablation inductively coupled plasma mass spectrometer (LA-ICP-MS) to analyze emeralds from the Zambian Kamakanga deposit, so as to provide a more comprehensive scientific basis for identifying the origins of emeralds and to summarize and supplement the latest data.

Materials
Thirteen emerald samples (ZAKA-1 to ZAKA-13) were investigated from the Kamakanga deposit in Kafubu area, Zambia (Figure 1).Emerald samples were selected from more than 300 rough emeralds that were obtained from an owner of a local mine.Emerald samples were in the form of hexagonal columns, slabs, or fragments; they were slightly transparent to transparent, and green to bluish green in color.

Methods
The emerald samples were examined by UV-Vis-NIR spectra, color measuring, Miro-FTIR, Diamond View TM , and LA-ICP-MS testing.
The UV-Vis-NIR spectra were recorded using a QSPEC GEM-3000 spectrophotometer manufactured by Biaoqi (Guangzhou, China) in the Gemological Research Laboratory of the China University of Geosciences in Beijing (CUGB, Beijing, China) with the following specifications: between 360-1000 nm; spectral resolution, 0.5 nm; and integral time, 240-300 ms.
The color parameters were also collected by the QSPEC GEM-3000 spectrophotometer, with the following specifications: integral time, 242; scans to average, 10; boxcar width, 2; range of wavelength, 250-1000.
Micro-FTIR infrared spectroscopy was performed in reflection mode in the Gemological Research Laboratory of the China University of Geosciences in Beijing (CUGB, Beijing, China), between 4000-600 cm −1 .The micro-FTIR spectrometer model was a Bruker LUMOS (Ettlingen, Germany) with the following specifications: resolution, 4 cm −1 ; scan time of background: 256; scan time of samples, 256; integration time, 80 s.
Diamond View TM (Maidenhead, United Kingdom), utilized at the Gemological Research Laboratory of the China University of Geosciences in Beijing (CUGB, Beijing, China), illuminated samples with hexagonal color zones.
The analysis of the in situ trace-element chemistry in the samples was completed at the National Research Center for Geoanalysis, Chinese Academy of Geological Sciences (CAGS), Beijing.The LA-ICP-MS analysis equipment consisted of an Applied Spectra IncJ-100 femto-second laser ablation system (343 nm) and a Thermo X-Series ICP-MS: laser spot diameters, 20 µm; laser frequency, 8 Hz; laser energy density, 1.08 J/cm 2 ; calibration reference materials, NISTSRM 610 and NIST SRM 612 (the mass discrimination and the time-dependent drift of sensitivity were corrected 1 time per 11 samples with calibration reference material).Internal standard element: 29 Si.Each analysis consisted of ~15 s of background acquisition of a blank measurement of gas, followed by 30 s of data acquisition from the sample.Chemical element analysis and calibration were completed using ICPMS Data Cal 10.8 software.

Color Parameters
In gemology, the CIE 1976 LAB uniform color space is often used to represent the color of gemstones, and the color parameters include L* (lightness), C* (chroma value), h (hue angle), a*, and b*.All samples were tested with the GEM-3000 spectrophotometer.According to the results, the color parameters of the experimental samples were as follows: L* ∈ (33.76, 57.45), a* ∈ (−29.17,−1.36), b* ∈ (−1.50, 12.81), C* ∈ (1.36, 31.86), and h ∈ (144.6 • , 189.5 • ) (Figure 2).The colors of the samples were mainly green; some samples had a bluish tinge in the blue-green tone interval, with medium lightness and low chroma.

UV-Vis-NIR
Polarized spectra of the oriented samples were collected for obtaining the ordinary ray (o-ray) and the extraordinary ray (e-ray).All the emeralds showed similar bands for both the o-ray and e-ray.The representative UV-Vis-NIR spectra of Kamakanga emerald (ZAKA-7) are shown in Figure 3.The o-ray (E⊥C) showed absorption bands at 420, 610-680, and 855 nm, as well as absorption peaks at 375 nm.The e-ray (E∥C) showed absorption bands at 420, 610-680, and 850 nm, as well as absorption peaks at 371 nm.The absorption bands and peaks at 420, 610, 635 and 680 nm indicated the presence of Cr 3+ , which caused the green color [21].In addition, Kamakanga emeralds are also abundant in Fe.The absorption peaks at 371 and 375 nm indicated the presence of Fe 3+ , while the absorption bands at 850 and 855 nm indicated the presence of Fe 2+ [22].Kamakanga emeralds showed distinct absorption The o-ray (E⊥C) showed absorption bands at 420, 610-680, and 855 nm, as well as absorption peaks at 375 nm.The e-ray (E C) showed absorption bands at 420, 610-680, and 850 nm, as well as absorption peaks at 371 nm.The absorption bands and peaks at 420, 610, 635 and 680 nm indicated the presence of Cr 3+ , which caused the green color [21].In addition, Kamakanga emeralds are also abundant in Fe.The absorption peaks at 371 and 375 nm indicated the presence of Fe 3+ , while the absorption bands at 850 and 855 nm indicated the presence of Fe 2+ [22].Kamakanga emeralds showed distinct absorption peaks at 371 and 375 nm, which were characteristic of high-Fe emeralds.The wavelength of the lowest absorption in the o-ray and e-ray spectra were essentially overlapping (~512 nm), indicating that the dichroism of Kamakanga emeralds was not strong.

Infrared Spectroscopy
According to the attribution of absorption peaks, the absorption peaks in the range of 3800 to 1400 cm −1 of the emerald infrared spectrum can be divided into three parts: the absorption peaks at 3800-3500 cm −1 are caused by channel water stretching vibration (Figure 4a); the absorption peaks at 3000-2000 cm −1 are caused by CO 2 or cedarwood oil (Figure 4b); the absorption peaks at 1700-1500 cm −1 are caused by channel water bending vibration (Figure 4c) [23,24].
According to the attribution of absorption peaks, the absorption peaks in the range of 3800 to 1400 cm −1 of the emerald infrared spectrum can be divided into three parts: the absorption peaks at 3800-3500 cm −1 are caused by channel water stretching vibration (Figure 4a); the absorption peaks at 3000-2000 cm −1 are caused by CO2 or cedarwood oil (Figure 4b); the absorption peaks at 1700-1500 cm −1 are caused by channel water bending vibration (Figure 4c) [23,24].As shown in Figure 4, the peaks at 3590 cm −1 of type I H2O were sharp and strong, while the peaks at 3564 or 3566 cm −1 of type II H2O were sharp but weak.The peak at 2359 cm −1 was caused by CO2.The absorption peaks of cedarwood oil (2921 and 2851 cm −1 ) were also shown in the infrared spectrum of ZAKA-2.The peak at 1620 cm −1 was caused by type I H2O.

Trace-Element Analysis
Eleven regular emerald samples with different colors (ZAKA-1, 2, 4, 5, 6, 8, 9, 10, 11, 12, and 13) and one emerald sample with a multi-layered hexagonal color zoning (ZAKA-3) were selected and analyzed by LA-ICP-MS.The 11 regular samples were analyzed, and each sample was tested by two points.Color zoning sample appeared in varying shades of green in natural light, while under ultraviolet light excitation, the hexagonal growth color zoning also showed different shades of red fluorescence with clear boundaries (Figure 5).Consequently, seven separate tests (ZAKA-3-1 to ZAKA-3-7) (Table 1) were carried out at different color zones (nearly colorless, darker green, and lighter green).As shown in Figure 4, the peaks at 3590 cm −1 of type I H 2 O were sharp and strong, while the peaks at 3564 or 3566 cm −1 of type II H 2 O were sharp but weak.The peak at 2359 cm −1 was caused by CO 2 .The absorption peaks of cedarwood oil (2921 and 2851 cm −1 ) were also shown in the infrared spectrum of ZAKA-2.The peak at 1620 cm −1 was caused by type I H 2 O.

Spectroscopy Characteristics
Emerald deposits can be roughly classified into two main groups (hydrothermal/ metamorphic and schist-hosted/magmatic-related), according to their geological conditions of formation [12,25].The UV-Vis-NIR spectra of the Kamakanga emerald have two characteristics: they contain a significant Fe 3+ absorption peak (371 or 375 nm) and the Fe-related absorption band (850 or 855 nm) is much stronger than the Cr-related absorption band (420 nm and 610-680 nm).These two characteristics are typical of the UV-Vis-NIR spectra of schist-hosted emeralds, while the spectra of hydrothermal emeralds have no absorption peak at 371 or 375 nm and have no Fe-related absorption band at 850 or 855 nm (e.g., low-Fe Colombia emerald and low-Fe Afghanistan emerald) or Cr-related absorption band stronger than Fe-related absorption band at 850 or 855 nm (e.g., high-Fe China emerald, high-Fe Colombia emerald, high-Fe Afghanistan emerald) [26].Therefore, UV-Vis-NIR spectra can be used to narrow down the range of emerald origins and to distinguish schisthosted emeralds from hydrothermal emeralds.However, determining the geographic origin of schist-hosted emeralds requires the use of multiple lines of evidence, as well as the evidence provided bny UV-Vis-NIRspectra.
The peak positions and attributions of the Kamakanga emeralds in the infrared spectra are shown in Table 3.The absorption peaks of type II H 2 O in Kamakanga emeralds are much stronger than those of type I H 2 O, and some of the samples studied in this paper were filled with colorless oil.Infrared spectra showed that the channel water within the Kamakanga emeralds is mainly type II H 2 O, which indicated that Kamakanga emeralds have a high content of alkali metal ions (15,407 ppmw; avg.17,592 ppmw).

Trace-Element Characteristics
The LA-ICP-MS results of 11 regular samples with different colors showed a wide variation of Cr/V (0.70 to 34.35) and a clear division of Cr/V for darker green, green, lighter green, and bluish green emeralds: Cr/V > 15 for darker green (15.84-34.35), 10 < Cr/V < 15 for green (10.77-14.86),and Cr/V < 10 (0.7-9.54) for lighter green and bluish green.However, the content of Cr (avg.1435ppmw) was much higher than that of V (avg.128 ppmw).This analysis indicated that Cr was the major chromogenic element in Kamakanga emeralds.
In addition, the variation of trace elements in different color zones of the color zoning sample (ZAKA-3) is shown in Figure 6.With the variation of colors (darker green color zoning → lighter green core → darker green color zoning → nearly colorless rim), the contents of Cr, V, and Sc showed large variability (Cr: 1954 → 767 → 2000 → 85 ppmw, Sc: 227 → 35 → 181 → 9 ppmw, V: 156 → 57 → 143 → 85 ppmw) (Figure 7).The trend was that the darker the green color, the higher the contents of Cr, Sc, and V, and the lower the content of Cs.However, the content of Cr was much higher than those of Sc, V, and Cs.In addition, Fe may have had a change in valence, so its content did not vary greatly with color.According to previous studies, the darker the green color, the higher the content of Fe [27].Therefore, Cr is the main chromogenic element in Kamakanga emeralds, and Sc, V, Cs, and Fe may have some influence on the color of Kamakanga emeralds.Most trace-element contents were stable in the lighter green core and vary significantly in the darker green color zoning and nearly colorless rim.This indicated that Kamakanga emeralds were grown in a stable environment during the early stages of mineralization.content of Cs.However, the content of Cr was much higher than those of Sc, V, and addition, Fe may have had a change in valence, so its content did not vary greatl color.According to previous studies, the darker the green color, the higher the con Fe [27].Therefore, Cr is the main chromogenic element in Kamakanga emeralds, a V, Cs, and Fe may have some influence on the color of Kamakanga emeralds.Most element contents were stable in the lighter green core and vary significantly in the green color zoning and nearly colorless rim.This indicated that Kamakanga em were grown in a stable environment during the early stages of mineralization.Emerald deposits in different countries have different geological settings, so tracechemical-element characteristics are essential for origin identification [15].In order to distinguish the origin of emeralds further, by trace elements, the LA-ICP-MS data from this paper were analyzed and compared with data from other major emerald deposits in the world, and a series of binary diagrams and ternary plots of trace-element concentrations were constructed (Figures 8-10).The data for the comparison came from the top six emerald origins, in terms of production (Colombia [28,29], Brazil [30], Zambia [28][29][30], Zimbabwe [29,30], Madagascar [29,31], and Afghanistan [28,29,32]), and from three origins Emerald deposits in different countries have different geological settings, so tracechemical-element characteristics are essential for origin identification [15].In order to distinguish the origin of emeralds further, by trace elements, the LA-ICP-MS data from this paper were analyzed and compared with data from other major emerald deposits in the world, and a series of binary diagrams and ternary plots of trace-element concentrations were constructed (Figures 8-10).The data for the comparison came from the top six emerald origins, in terms of production (Colombia [28,29], Brazil [30], Zambia [28][29][30], Zimbabwe [29,30], Madagascar [29,31], and Afghanistan [28,29,32]), and from three origins with similar inclusion to that of Zambian Kamakanga emerald (India [18], Russia [29], Ethiopia [33]), and China [34], for a total of 139 sample data points.
scales for clearer display.
Emerald deposits in different countries have different geological settings, so tracechemical-element characteristics are essential for origin identification [15].In order to distinguish the origin of emeralds further, by trace elements, the LA-ICP-MS data from this paper were analyzed and compared with data from other major emerald deposits in the world, and a series of binary diagrams and ternary plots of trace-element concentrations were constructed (Figures 8-10).The data for the comparison came from the top six emerald origins, in terms of production (Colombia [28,29], Brazil [30], Zambia [28][29][30], Zimbabwe [29,30], Madagascar [29,31], and Afghanistan [28,29,32]), and from three origins with similar inclusion to that of Zambian Kamakanga emerald (India [18], Russia [29] Ethiopia [33]), and China [34], for a total of 139 sample data points.Although Zambia and Madagascar partially overlap in the Fe versus Ga binary diagram, the two sources can be easily distinguished by the Li versus Cs binary diagram (Figure 9).This is because the contents of Cs (avg.266 ppmw) and Li (avg.89 ppmw) in Madagascar are much lower than the contents of Cs (avg.1331 ppmw) and Li (avg.485 ppmw) in Zambia.
Although India, Russia, Ethiopia, and Brazil emeralds have brownish platelet phlogopite and rectangular fluid inclusions that are similar to those of the Zambia emeralds [19], the Fe content in Russia emeralds (avg.1618 ppmw) is much lower than that in Zambia emeralds (avg.8556 ppmw).The contents of Cs (avg.312 ppmw) and Li (avg.103 Although Zambia and Madagascar partially overlap in the Fe versus Ga binary diagram, the two sources can be easily distinguished by the Li versus Cs binary diagram (Figure 9).This is because the contents of Cs (avg.266 ppmw) and Li (avg.89 ppmw) in Madagascar are much lower than the contents of Cs (avg.1331 ppmw) and Li (avg.485 ppmw) in Zambia.
Although India, Russia, Ethiopia, and Brazil emeralds have brownish platelet phlogopite and rectangular fluid inclusions that are similar to those of the Zambia emeralds [19], the Fe content in Russia emeralds (avg.1618 ppmw) is much lower than that in Zambia emeralds (avg.8556 ppmw).The contents of Cs (avg.312 ppmw) and Li (avg.103 ppmw) in Brazil are much lower than that in Zambia.The content of Cs in India (avg.385 ppmw) is lower than that in Zambia.The content of Ga in Ethiopia (avg.22 ppmw) is higher than that in Zambia (avg.11 ppmw).
Zambia emerald can be easily distinguished from Madagascar, Brazil, and Afghanistan emerald by the ternary plot of relative abundance of K, Rb, and Li + Cs (Figure 10).Zambia emerald shows high content of Li + Cs (avg.1816 ppmw), while Brazil and Madagascar emeralds show moderate contents of K and Li + Cs and Afghanistan emeralds show a high content of K. Bakakin and Belov [35] argued that when emeralds are enriched by Li, they also contain a higher concentration of Cs.In general, highly fractionated rare-element granitic pegmatites of the LCT association (Li, Cs, and Ta) are enriched in Li and Cs [30].Zambia emeralds are, indeed, closely associated with highly fractionated pegmatites [2].This indicates that the conclusions in this paper confirm those of previous studies.

Conclusions
This paper provides new data on the spectroscopy characteristics and the trace-element characteristics of Zambian Kamakanga emeralds.These data provide additional support for the identification of the origins of emeralds.
The UV-Vis-NIR spectra showed a distinct Fe 3+ absorption peak, and the Fe-related absorption band was much stronger than the Cr-related absorption band.This confirmed that the Zambian Kamakanga emeralds are schist-hosted.The infrared spectra showed that the absorption peak of type II H 2 O in Zambian emeralds is much stronger than that of type I H 2 O, which indicated that the channel water in Zambian Kamakanga emeralds is mainly type II H 2 O and the content of alkali metal ions in the emeralds is high.
LA-ICP-MS analysis showed that darker green, green, lighter green and bluish green emeralds have a clear separation of Cr/V (Cr/V > 15 for darker green, 10 < Cr/V < 15 for green, and Cr/V < 10 for lighter green and bluish green).In color zoning the emerald

Figure 1 .
Figure 1.The 13 different samples of emeralds studied.Figure 1.The 13 different samples of emeralds studied.

Figure 1 .
Figure 1.The 13 different samples of emeralds studied.Figure 1.The 13 different samples of emeralds studied.

Crystals 2023 , 13 Figure 2 .
Figure 2. Color distribution of emerald samples in the CIELAB space.Modified from [20].3.1.2.UV-Vis-NIR Polarized spectra of the oriented samples were collected for obtaining the ordinary ray (o-ray) and the extraordinary ray (e-ray).All the emeralds showed similar bands for

Figure 2 .
Figure 2. Color distribution of emerald samples in the CIELAB space.Modified from [20].

Figure 2 .
Figure 2. Color distribution of emerald samples in the CIELAB space.Modified from [20].

Figure 6 .
Figure 6.Representative photomicrograph of color zoning emerald ZAKA-3 with darker gree zoning, lighter green core, and nearly colorless rim.The white circles indicate the positions ysis points corresponding to analyses of ZAKA-3-1 to ZAKA-3-7.

Figure 6 .
Figure 6.Representative photomicrograph of color zoning emerald ZAKA-3 with darker green color zoning, lighter green core, and nearly colorless rim.The white circles indicate the positions of analysis points corresponding to analyses of ZAKA-3-1 to ZAKA-3-7.Crystals 2023, 13, x FOR PEER REVIEW 9 of 13

Figure 7 .
Figure 7. LA-ICP-MS data for selected trace-element analysis from ZAKA-3-1 to ZAKA-3-7.Plots of V, Cr, Fe, Sc, Ga, Rb, and Cs are used to highlight compositional changes, with uneven ordinate scales for clearer display.

Figure 7 .
Figure 7. LA-ICP-MS data for selected trace-element analysis from ZAKA-3-1 to ZAKA-3-7.Plots of V, Cr, Fe, Sc, Ga, Rb, and Cs are used to highlight compositional changes, with uneven ordinate scales for clearer display.

Figure 10 .
Figure 10.Ternary plot of relative abundance of klium (K), rubidium (Rb), and lithium + cesium (Li + Cs) in emerald samples from LA-ICP-MS analyses.Data are expressed in ppmw.Other sources are from [18,28-34].As shown in the Fe versus Ga binary diagram (Figure 8), Zambian and Madagascan Ga/Fe < 0.0025, while the other origins are Ga/Fe > 0.0025.Zambian and Madagascan emeralds contain relatively high Fe (Zambian avg.8556 ppmw; Madagascan avg.9139 ppmw) and low Ga (Zambian avg.11 ppmw; Madagascan avg.7 ppmw).Consequently, Zambia emerald can be completely distinguished from other origins, except for Madagascar origins, by the Fe versus Ga binary diagram.Although Zambia and Madagascar partially overlap in the Fe versus Ga binary diagram, the two sources can be easily distinguished by the Li versus Cs binary diagram (Figure9).This is because the contents of Cs (avg.266 ppmw) and Li (avg.89 ppmw) in Madagascar are much lower than the contents of Cs (avg.1331 ppmw) and Li (avg.485 ppmw) in Zambia.Although India, Russia, Ethiopia, and Brazil emeralds have brownish platelet phlogopite and rectangular fluid inclusions that are similar to those of the Zambia emeralds[19], the Fe content in Russia emeralds (avg.1618 ppmw) is much lower than that in Zambia emeralds (avg.8556 ppmw).The contents of Cs (avg.312 ppmw) and Li (avg.103

Table 3 .
Peak positions and attribution of the Kamakanga emeralds in infrared spectra (cm −1 ).