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Fig. 5. (A) Recovery during field operations of a Fasad point (indicated by the arrow) in the Unit C of GQ-13/23 site (note that it displays a planar orientation, according to the stratigraphy); (B) the drawing of the same item (by. G. Devilder, CNRS).

Figure 5 (A) Recovery during field operations of a Fasad point (indicated by the arrow) in the Unit C of GQ-13/23 site (note that it displays a planar orientation, according to the stratigraphy); (B) the drawing of the same item (by. G. Devilder, CNRS).

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Fig. 1. (A) Location of the study area in Oman. (B) Satellite imagery (Google Earth™) representing the main regions cited in the text; the dashed box indicates the position of Fig. 2. The region of Dhofar in south-western Oman, bordering the Hadramawt and Mahra regions of eastern Yemen, is a mountainous and plateau region, with one particular limestone massif (Fig. 1), which separates the coastal plain of Salalah from the Nejd Desert: the Jebel Qara (Cremaschi and Negrino, 2005), representing the continuation in Oman of the Yemeni Hadramawt plateau (Fig. 2). Jebel Qara's top is gently undulating and it reaches the maximum height of ~850 m above sea level. From the geological point of view, the massif consists of late Cretaceous to Tertiary limestone (Platel et al., 1992). Geological strata are gently tilted to the North and crossed by systems of faults in the area above the Salalah coastal plain and immediately south of the Nejd Desert. Loess deposits occur along the northern fringe of the jebel and are similar to de- posits described on the Yemeni Plateau and dated to the Early Holocene (Nettleton and Chadwick, 1996; Cremaschi and Negrino, 2005). A well developed karst net is present in the Jebel Qara massif and many rock shelters are located along the steep slopes in the southern part of the jebel (Platel, 1992; Hanna and Al-Belushi, 1996); many of them can be interpreted as inland notches (Shtober-Zisu et al., 2015). The southern margins of the Jebel Qara are connected to the present-day coastline of the Indian Ocean by an alluvial apron consisting of steep alluvial fans, composed of
Fig. 1. (A) Location of the study area in Oman. (B) Satellite imagery (Google Earth™) representing the main regions cited in the text; the dashed box indicates the position of Fig. 2. The region of Dhofar in south-western Oman, bordering the Hadramawt and Mahra regions of eastern Yemen, is a mountainous and plateau region, with one particular limestone massif (Fig. 1), which separates the coastal plain of Salalah from the Nejd Desert: the Jebel Qara (Cremaschi and Negrino, 2005), representing the continuation in Oman of the Yemeni Hadramawt plateau (Fig. 2). Jebel Qara's top is gently undulating and it reaches the maximum height of ~850 m above sea level. From the geological point of view, the massif consists of late Cretaceous to Tertiary limestone (Platel et al., 1992). Geological strata are gently tilted to the North and crossed by systems of faults in the area above the Salalah coastal plain and immediately south of the Nejd Desert. Loess deposits occur along the northern fringe of the jebel and are similar to de- posits described on the Yemeni Plateau and dated to the Early Holocene (Nettleton and Chadwick, 1996; Cremaschi and Negrino, 2005). A well developed karst net is present in the Jebel Qara massif and many rock shelters are located along the steep slopes in the southern part of the jebel (Platel, 1992; Hanna and Al-Belushi, 1996); many of them can be interpreted as inland notches (Shtober-Zisu et al., 2015). The southern margins of the Jebel Qara are connected to the present-day coastline of the Indian Ocean by an alluvial apron consisting of steep alluvial fans, composed of
Fig. 2. Geomorphology of the Jebel Qara region (modified from Cremaschi and Negrino, 2005); the position of the rockshelters whose Holocene infillings were studied is indicate: py labels. The location of the archaeological sites identified in the field work is also shown. Key: 1) pediment of the Nejd Desert and gravely wadi bed; 2) desert loess deposits; 3 Jeep-cut fluvial net; 4) main Holocene calcareous tufa deposits; 5) slope deposits and Holocene alluvial fans; 6) coastal deposits and marine erosion terrace; 7) main scarps; 8 possible Holocene front of the monsoon rain; 9) rock shelters or caves with shell accumulations (Unit C); 10) rock shelters or caves without shell accumulations; 11) open-air site ‘see Cremaschi and Negrino, 2005).
Fig. 2. Geomorphology of the Jebel Qara region (modified from Cremaschi and Negrino, 2005); the position of the rockshelters whose Holocene infillings were studied is indicate: py labels. The location of the archaeological sites identified in the field work is also shown. Key: 1) pediment of the Nejd Desert and gravely wadi bed; 2) desert loess deposits; 3 Jeep-cut fluvial net; 4) main Holocene calcareous tufa deposits; 5) slope deposits and Holocene alluvial fans; 6) coastal deposits and marine erosion terrace; 7) main scarps; 8 possible Holocene front of the monsoon rain; 9) rock shelters or caves with shell accumulations (Unit C); 10) rock shelters or caves without shell accumulations; 11) open-air site ‘see Cremaschi and Negrino, 2005).
* Radiocarbon dating from Cremaschi and Negrino (2005). years BC and BP. Calibration according to IntCal13 curve (Reimer et al., 2013).
* Radiocarbon dating from Cremaschi and Negrino (2005). years BC and BP. Calibration according to IntCal13 curve (Reimer et al., 2013).
Essential micromorphological descriptions of samples representative for the four stratigraphic units composing the infilling of the rock shelters. Table 2
Essential micromorphological descriptions of samples representative for the four stratigraphic units composing the infilling of the rock shelters. Table 2
Results of U/Th dating on calcareous tufa samples KR1 and KR3. The activity ratios [??°Th/??8U] and [734U/?38U] have been standardized to the HU-1 secular equilibrium standard. Ages were calculated using decay constants of 9.195 x 10-6 yr—! (?3°Th) and 2.835 x 10~§ yr! (734U), and an assumed initial [??°Th/???Th] of 1.5 + 1.5 except KK215- 3B, for which a value of 0.8 has been assumed. Depths are from the sample top, and numbers in brackets are the 95% uncertainties in the last digits given.
Results of U/Th dating on calcareous tufa samples KR1 and KR3. The activity ratios [??°Th/??8U] and [734U/?38U] have been standardized to the HU-1 secular equilibrium standard. Ages were calculated using decay constants of 9.195 x 10-6 yr—! (?3°Th) and 2.835 x 10~§ yr! (734U), and an assumed initial [??°Th/???Th] of 1.5 + 1.5 except KK215- 3B, for which a value of 0.8 has been assumed. Depths are from the sample top, and numbers in brackets are the 95% uncertainties in the last digits given.
Fig. 3. Field pictures of (A) a rock shelter in the Jebel Qara area; note the columnar calcareous tufa sectioning its entrance. (B) The sedimentary infilling of a rock shelter sealed by a thick calcareous tufa. Details of the stratigraphic sequence: (C) the lowermost part of the calcareous tufa sealing the sequence (Unit D); (D) the accumulation of land shells (Unit C); (E) the angular breccia with a loessic matrix (Unit B). A total of eight U-series dating have been performed on twc samples KR1 and KR3 collected from the same flowstone decora- tion sealing the base deposits of the KR-213 shelter. Unfortunately due to the low U content and high level of detrital (Th) contami- nation, only the results of five out of eight ages can be considered as reliable (Table 3). U/Th ages indicate that flowstone KR1 is basically Interesting information can be detected at the micro-scale; thin sections from the infilling of both caves display similar features (Table 2). Thin sections of the clast-supported breccia Units A and B highlight the presence of limestone angular clasts (breccia), prob- ably deriving from thermal degradation of the vault of the rock shelter. The matrix of the breccia consists of sand grains (Unit A) and loess-like (Unit B) sandy silt (increasing in percentage from Unit A to Unit B). The local origin of limestone clasts is confirmed by the occurrence of marine microfossils typical of the rock formations constituting the Jebel Qara (Fig. 6). On the contrary, the inter- granular sediments, rich in quartz, feldspar and heavy minerals
Fig. 3. Field pictures of (A) a rock shelter in the Jebel Qara area; note the columnar calcareous tufa sectioning its entrance. (B) The sedimentary infilling of a rock shelter sealed by a thick calcareous tufa. Details of the stratigraphic sequence: (C) the lowermost part of the calcareous tufa sealing the sequence (Unit D); (D) the accumulation of land shells (Unit C); (E) the angular breccia with a loessic matrix (Unit B). A total of eight U-series dating have been performed on twc samples KR1 and KR3 collected from the same flowstone decora- tion sealing the base deposits of the KR-213 shelter. Unfortunately due to the low U content and high level of detrital (Th) contami- nation, only the results of five out of eight ages can be considered as reliable (Table 3). U/Th ages indicate that flowstone KR1 is basically Interesting information can be detected at the micro-scale; thin sections from the infilling of both caves display similar features (Table 2). Thin sections of the clast-supported breccia Units A and B highlight the presence of limestone angular clasts (breccia), prob- ably deriving from thermal degradation of the vault of the rock shelter. The matrix of the breccia consists of sand grains (Unit A) and loess-like (Unit B) sandy silt (increasing in percentage from Unit A to Unit B). The local origin of limestone clasts is confirmed by the occurrence of marine microfossils typical of the rock formations constituting the Jebel Qara (Fig. 6). On the contrary, the inter- granular sediments, rich in quartz, feldspar and heavy minerals
Fig. 4. Sketches of the infillings of the rock shelters KR-213 (modified from Cremaschi and Negrino, 2005) and GQ-13/23 in the Jebel Qara; the description of each stratigraphic Unit is in the text. Vertical bars indicate the extension of each stratigraphic unit. Key: 1) bedrock (limestone); 2) clast-supported breccia (Unit A); 3) matrix-supported breccia and loess (Unit B); 4) organic matter-rich layers; 5) accumulations of land shells/escargotieres (Unit C); 6) calcareous tufa (Unit D); 7) fragments of charcoal; 8) lithic artefacts.
Fig. 4. Sketches of the infillings of the rock shelters KR-213 (modified from Cremaschi and Negrino, 2005) and GQ-13/23 in the Jebel Qara; the description of each stratigraphic Unit is in the text. Vertical bars indicate the extension of each stratigraphic unit. Key: 1) bedrock (limestone); 2) clast-supported breccia (Unit A); 3) matrix-supported breccia and loess (Unit B); 4) organic matter-rich layers; 5) accumulations of land shells/escargotieres (Unit C); 6) calcareous tufa (Unit D); 7) fragments of charcoal; 8) lithic artefacts.
Fig. 6. Photomicrographs of thin sections of the deposits of rock shelter GQ-13/23. (A) Lower part of Unit B, planar orientation of rock fragments forming a matrix-supported angular breccia (XPL). (B) Unit B, transition between a clast to matrix-supported breccia; note the occurrence of micrite pendents on rock fragments (PPL). (C) Unit B, brown silty fine matrix deeply cemented by calcium carbonate with common quartz grains; the arrows indicate small shell fragments (PPL). (D) Upper Unit B, strong redistribution of calcium carbonate cement forming crystalline pedofeatures and enclosing charcoal fragments (indicated by the arrows; XPL).
Fig. 6. Photomicrographs of thin sections of the deposits of rock shelter GQ-13/23. (A) Lower part of Unit B, planar orientation of rock fragments forming a matrix-supported angular breccia (XPL). (B) Unit B, transition between a clast to matrix-supported breccia; note the occurrence of micrite pendents on rock fragments (PPL). (C) Unit B, brown silty fine matrix deeply cemented by calcium carbonate with common quartz grains; the arrows indicate small shell fragments (PPL). (D) Upper Unit B, strong redistribution of calcium carbonate cement forming crystalline pedofeatures and enclosing charcoal fragments (indicated by the arrows; XPL).
Fig. 7. Photomicrographs of thin sections of the deposits of rock shelter GQ-13/23. (A) Unit C, deep concentration of mollusc fragments in the escargotieres; note the clast-supported structure and the presence of evidence of heating (see: Maritan et al., 2007) on several shell fragments (PPL). (B) Unit C, note the strong distribution of micrite on shell fragments and in the micromass (XPL). (C) Unit C, brown matrix between two large shell fragments; note the occurrence of charcoal fragments (c) and a fragment of bone (b) (PPL). (D) Lower part of Unit D, note the transition between the accumulation of land shells and the calcareous tufa (XPL). (E) Concentration of charcoal fragments cemented by micrite at the transition between Unit C and Unit D (PPL). (F) Laminated microstructure with common fenestral voids of the calcareous tufa at the basis of Unit D (PPL). found in relation to this point at GQ-13/23, making it difficult to propose a precise technological assessment of the complete lithic assemblage. Nevertheless, both type and technology observed on this single artefact at GQ-13/23, confirm the chronological and thus cultural affiliation of this industry to the Early Holocene. However, it is not firmly known, and still highly debated, if the makers of this kind of projectiles have a local origin related to autochthonous Late Palaeolithic groups. As well, it is not known if the occupants at GQ- 13/23, and their counterparts in the region who were making these Fasad points, are actually the direct ancestors of the Neolithic populations that rapidly spread inland and along the coasts about two millennia later. Only a complete stratigraphic sequence
Fig. 7. Photomicrographs of thin sections of the deposits of rock shelter GQ-13/23. (A) Unit C, deep concentration of mollusc fragments in the escargotieres; note the clast-supported structure and the presence of evidence of heating (see: Maritan et al., 2007) on several shell fragments (PPL). (B) Unit C, note the strong distribution of micrite on shell fragments and in the micromass (XPL). (C) Unit C, brown matrix between two large shell fragments; note the occurrence of charcoal fragments (c) and a fragment of bone (b) (PPL). (D) Lower part of Unit D, note the transition between the accumulation of land shells and the calcareous tufa (XPL). (E) Concentration of charcoal fragments cemented by micrite at the transition between Unit C and Unit D (PPL). (F) Laminated microstructure with common fenestral voids of the calcareous tufa at the basis of Unit D (PPL). found in relation to this point at GQ-13/23, making it difficult to propose a precise technological assessment of the complete lithic assemblage. Nevertheless, both type and technology observed on this single artefact at GQ-13/23, confirm the chronological and thus cultural affiliation of this industry to the Early Holocene. However, it is not firmly known, and still highly debated, if the makers of this kind of projectiles have a local origin related to autochthonous Late Palaeolithic groups. As well, it is not known if the occupants at GQ- 13/23, and their counterparts in the region who were making these Fasad points, are actually the direct ancestors of the Neolithic populations that rapidly spread inland and along the coasts about two millennia later. Only a complete stratigraphic sequence
Fig. 8. Isotopic profiles (C and O) of the considered samples of flowstones (KR1 and KR3) and position of U/Th dating results according to flowstones' depth
Fig. 8. Isotopic profiles (C and O) of the considered samples of flowstones (KR1 and KR3) and position of U/Th dating results according to flowstones' depth
Fig. 9. The cross plots of 5'°0 versus 3'°C for each sample (Hendy test); the correlation between C and O values are also reported.
Fig. 9. The cross plots of 5'°0 versus 3'°C for each sample (Hendy test); the correlation between C and O values are also reported.
Fig. 10. Composite oxygen isotope profiles of flowstones KR1 and KR3 compared with the oxygen curve of the Q5 site (Qunf cave, southern Oman) elaborated by Fleitmann et al. (2003). Changes in Holocene summer insolation (according to Berger and Loutre, 1991) are also reported.
Fig. 10. Composite oxygen isotope profiles of flowstones KR1 and KR3 compared with the oxygen curve of the Q5 site (Qunf cave, southern Oman) elaborated by Fleitmann et al. (2003). Changes in Holocene summer insolation (according to Berger and Loutre, 1991) are also reported.
Related topics:
Landscape EcologyHydrology/HydrographyPrehistoric ArchaeologyEnvironmental ScienceGeologyHydrogeologyStable isotope ecologyClimate ChangeStable Isotope AnalysisHydrology
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