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Mineralogy, geochemistry, petrography, and depositional environment of Gebel El-Qurn, Early Eocene, West Luxor, South Egypt

Bulletin of the National Research Centre201842:7

https://doi.org/10.1186/s42269-018-0008-3

  • Received: 10 July 2018
  • Accepted: 27 August 2018
  • Published:

Abstract

Background

Luxor represented the modern Egyptian city that occupies the site of ancient Thebes. Thebes Mountain on the West Bank of the Nile, opposite the town of Luxor, is among the most famous historical sites of the world. Carbonate rocks exposed at Gebel El-Qurn, west Luxor, south Egypt has been investigated for mineralogical, petrographical, and geochemical studies to illustrate its depositional environments.

Results

We revealed that the carbonate rocks in the Gebel El-Qurn, west Luxor, are mainly of Lower Eocene age. The carbonate rocks that belong to the Thebes Formation were deposited under shallow, warm, oxidizing, open marine environment. Petrographically, they are differentiated into five microfacies: (1) nummulitic bioclastic wackestone/mudstone, (2) nummulitic biosparite grainstone, (3) nummulitic rudstone microfacies, (4) pelecypod biomicrite wacke/packstone, and (5) biomicrite dolomitic lime-mudstone. Diagenetically, carbonate rocks were subjected to cementation, compaction, neomorphism, dissolution, and dolomitization processes. Mineralogically, XRD revealed that the studied carbonate samples consist mainly of calcite as well as dolomite, quartz, halite, pyrite, and clay minerals. EDX data indicated that the dolomite of the Gebel El-Qurn is non-stoichiometric in composition, and the size of crystals is up to 80 μm.

Geochemically, the carbonate rocks of the Gebel El-Qurn are impoverished in Sr and Na content. This may be attributed to the diagenetic processes, which took place under less saline environment than seawater. Dolomite crystals were formed by re-crystallization under mixed marine-meteoric environment. The positive correlation between Sr and Fe2O3 indicates that the studied carbonates were deposited under control of bacterial activity. The studied carbonate rocks are characterized by light REE (LREE) enrichment with respect to heavy REE (HREE). The total radioactivity measurements are ranging from 4 to 5.9 ppm for U and from 5.5 to 6.6 ppm for Th. The radioactivity measurements are less than the background level of carbonates, and they are in the permissible limits for carbonates used in cement industries and as building stones.

Conclusions

The petrographical and geochemical observations, as well as mineralogical investigation, indicate that the carbonate rocks in the Gebel El-Qurn were deposited in a shallow, warm open marine environment.

Keywords

  • Gebel El-Qurn
  • Thebes Formation
  • Petrography
  • Geochemistry
  • Rare earth elements

Background

Luxor, the modern Egyptian city that occupies the site of ancient Thebes, is famed for its magnificent ancient monuments. The Thebes Mountain on the West Bank of the Nile, opposite the town of Luxor, is among the most famous historical sites of the world. The Thebes Mountains are sedimentary rocks that are composed mainly of shales, marls, chalk, and limestones. They consist of three important formations, from base to top, the Paleocene Tarawan Chalk, the Paleocene/Eocene Esna Shale, and the Lower Eocene Thebes Formation which were unconformably overlain by the Plio-Pleistocene conglomerate (Said 1962). Generally, they were mainly deposited through the Paleocene–Lower Eocene age in a pelagic and shallow environment under and above the phototropic zone (Said 1990). Thebes Mountains in Luxor were studied by many authors: biostratigraphy (Perch-Nielsen et al. 1978; Strougo and Hassaan 1984), sedimentology, and structural geology (Yehia 1986; El-Kammar et al. 1991; Elwaseif et al. 2012), in addition, recently, the environmental studies (El-Bayomi 2007; Leisen et al. 2008).

The stratigraphic succession of Gebel El-Qurn, west Luxor, is represented as a type-section of the Thebes Formation (Said 1962). The succession belongs to the Thebes Mountains that extend for several hundred kilometers toward the west of the western side of the Nile River. These mountains consist of craggy limestone hills which have been deeply incised by a series of dendritic wadis that mainly controlled by gravity, structure, and/or lithology (Yehia 1973). The maximum elevation is more than 400 m from the Nile River to the top of Gebel El-Qurn.

The present study uses incorporated petrographical, geochemical, and mineralogical studies in order to decide the origin and the depositional environments of the carbonate rocks of Member IV, Lower Eocene, Thebes Formation of Gebel El-Qurn in west Luxor, south Egypt (Fig. 1).
Fig. 1
Fig. 1

Location and geological map of the studied area (after, Said 1962)

Methods

Twenty representative samples were collected from the carbonate beds of Gebel El-Qurn in west Luxor, in the south part of Egypt. Mineralogically, four selected samples were investigated by the X-ray technique at the Egyptian Mineral Resources Authority (Dokki, Egypt) using a PAN analytical X-ray diffraction equipment model X′Pert PRO with Secondary Monochromator, Cu-radiation (λ = 1.542 Å) at 45 K.V., 35 M.A., and a scanning speed of 0.02°/s were used. The diffraction charts and relative intensities are compared with ICDD files. The morphology and the size of the synthesized samples were examined using scanning electron microscope carried out in the nuclear materials as well as the thin sections under microscope. Ten samples were selected to determine the chemical composition by using Axios Sequential WD_XRF Spectrometer, Analytical 2005 in the National Research Center laboratories, ASTM E 1621 standard guide for elemental analysis by wavelength dispersive X-Ray Fluorescence Spectrometer, and ASTM D 7348 standard test methods for loss of ignition (LOI) of solid combustion. The fabric and the size of the synthesized samples were characterized via SEM coupled with energy-dispersive spectroscopy EDAX (SEM Model Quanta FEG 250), carried out in the National Research Center laboratories.

Geologic setting

The stratigraphic succession at Gebel El-Qurn, west Luxor, comprising the Esna Shale and Thebes Formations, reaches about 400 m thick (Fig. 2), which ranges from the upper Paleocene to the lower Eocene.
Fig. 2
Fig. 2

Lithostratigraphic succession of Gebel El-Qurn, west Luxor, southern Egypt (after Said 1962)

The Thebes Formation is about 350 m thick and commences with fine-grained micritic limestone and marl rich in bands and nodules of chert, probably deposited at bathyal depths (Snavely et al. 1978), and ends with repetitive skeletal limestones and oyster banks formed in a shallow water setting. Said (1962) classified the Thebes Formation into four members according to variations in lithology and weathering characteristics (Fig. 2).

Member IV was composed of about 250 m of an alternating series of dolomitic limestones, marls, shales, and nodular limestones with interbedded chert nodules and chert bands.

They are regarded as individual shallowing upward cycles of deposition. In addition, they are richly fossiliferous, with cephalopods (Nautilus sp.), gastropods (Turritella sp.), pelecypods (Ostrea sp.), and anodont bivalves (Lucina thebaica), and various nummulites and Operculina sp. They were deposited in shallow water (10–100 m) on an extensive carbonate platform (Wüst 1995).

Results

Mineralogically, the studied carbonate rocks consist of six minerals, mainly of calcite as well as dolomite, quartz, halite, pyrite, and clay minerals. Petrographically, five major microfacies were encountered in the studied section. Five main diagenetic features encountered in the carbonate rocks of Geble El Gurna. Chemical analysis data for major, trace, and rare earth elements of the studied carbonate rocks are listed in Table 1 and the relation between them in Table 2.
Table 1

Chemical analysis data of major oxides (%) and trace rare earth elements (ppm), of the studied rocks

 

1

2

3

4

5

6

7

8

9

10

Mim.

Max.

Average

CaO

50.84

32.21

48.21

51.36

50.84

48.27

51.21

49.51

50.41

38.44

32.21

51.36

47.13

MgO

3.26

1.01

2.11

0.8

3.51

3.85

2.57

1.92

2.1

2.04

0.8

3.85

2.317

SiO2

2.33

23.74

5.34

3.25

1.25

3.45

4.52

3.55

3.24

18.75

1.25

23.74

6.942

Al2O3

0.63

0.81

1.95

0.98

0.51

1.97

1.92

0.95

0.92

0.8

0.51

1.97

1.144

Fe2O3

0.76

0.64

0.84

0.78

0.82

0.89

0.74

0.81

0.91

0.85

0.64

0.91

0.804

Na2O

0.11

0.1

0.21

0.12

0.11

0.15

0.16

0.19

0.18

0.12

0.1

0.21

0.145

K2O

0.03

0.03

0.02

0.03

0.03

0.03

0.02

0.03

0.02

0.03

0.02

0.03

0.027

P2O5

0.22

0.25

0.24

0.26

0.27

0.25

0.3

0.22

0.24

0.25

0.22

0.3

0.25

Cl

0.08

0.09

0.11

0.01

0.09

0.14

0.2

0.15

0.15

0.11

0.01

0.2

0.113

LOI

41.6

41.02

41.11

41.91

41.82

40.97

38.74

42.51

41.65

38.57

38.57

42.51

40.99

Ti

60

77

65

70

62

75

55

88

50

80

50

88

68

Sr

445

510

400

470

520

490

460

510

500

520

400

520

483

Sc

30

35

25

24

20

19

29

28

32

22

19

35

26.4

V

24.5

29

35

28

26

30

19

22.5

23.4

24.3

19

35

26.17

Cr

34.6

35

38

37

36.4

40

23.8

37

34.5

33.8

23.8

40

35.01

Mn

50.2

52

48

55

59

58

60

55.4

36.5

49.7

36.5

60

52.38

Co

0.4

0.5

0.3

0.6

0.4

0.8

0.7

0.5

0.4

0.3

0.3

0.8

0.49

Ni

10.8

11.5

12

14.2

11.5

15.1

14.2

13.4

12.7

13.7

10.8

15.1

12.91

Cu

5.8

6.1

6.5

5.8

5.9

4.9

6.2

7.1

6.8

6.9

4.9

7.1

6.2

Zn

54.4

57.4

55.3

60.2

62.3

59

58.1

57.5

61.5

62.4

54.4

62.4

58.81

Ga

0.5

0.4

0.4

0.3

0.5

0.5

0.06

0.03

0.04

0.05

0.03

0.5

0.278

As

0.8

0.7

0.6

0.5

0.5

0.6

0.3

0.4

0.7

0.8

0.3

0.8

0.59

Se

0.6

0.04

0.05

0.06

0.06

0.08

0.07

0.06

0.05

0.06

0.04

0.6

0.113

Br

1.5

1.3

1.5

2.1

2.4

1.9

1.6

1.5

2.2

1.8

1.3

2.4

1.78

Mo

2

3

2.4

1.8

2.5

2.7

3

3.5

3.8

3.8

1.8

3.8

2.85

Y

0.8

0.9

0.7

0.8

0.6

0.9

0.8

0.6

0.8

0.8

0.6

0.9

0.77

Zr

5.5

7.4

6.8

5.9

5.8

6.5

7

7.5

6.4

5.9

5.5

7.5

6.47

Ag

0.1

0.1

0.1

0.1

0.2

0.1

0.1

0.2

0.1

0.1

0.1

0.2

0.12

As

0.8

0.9

1.1

0.9

0.7

0.8

0.7

1.2

1.3

0.9

0.7

1.3

0.93

Sn

0.4

0.4

0.3

0.5

0.3

0.4

0.4

0.5

0.5

0.3

0.3

0.5

0.4

Sb

1.5

1.3

1.3

1.5

2.1

1.9

1.8

1.7

1.8

1.9

1.3

2.1

1.68

I

11.8

12.5

12

13.1

11.8

12.8

13.1

12.7

11.9

11.5

11.5

13.1

12.32

Cs

16.8

17.3

17.5

15.4

16.8

18.1

17.3

19.1

16.7

16.5

15.4

19.1

17.15

Ba

70.2

75

78

80

79

82

75.4

77.3

78.6

75.2

70.2

82

77.07

La

11.2

12

11.7

12.4

13.1

12.3

14.2

12.5

12.7

11.4

11.2

14.2

12.35

Nd

4.3

4.1

5.2

5.3

4.9

4.3

3.9

3.7

4.6

4.9

3.7

5.3

4.52

Sm

5.4

5.9

5.7

5.2

6.7

4.9

5.6

6.5

4.8

5.6

4.8

6.7

5.63

Hf

1.9

1.1

1.8

2.1

1.9

1.9

1.5

2.4

2.4

2.3

1.1

2.4

1.93

W

2.2

2.5

3.1

2.4

1.9

3.2

2.8

2.7

2.5

2.8

1.9

3.2

2.61

Bi

0.8

0.8

0.6

0.7

0.5

0.9

0.4

0.4

0.6

0.8

0.4

0.9

0.65

U

4

4

5

4.5

5.2

4.9

5.9

4.8

4.5

5

4

5.9

4.78

Th

5.8

5.9

6.5

6.1

5.8

5.5

6.3

6.4

6.6

6.2

5.5

6.6

6.11

ΣREE

870.00

977.14

853.95

933.56

972.56

964.38

894.93

992.2

926.19

975.61

764.3

1050.5

936.35

Nor. Calc.

90.74

57.49

86.05

91.67

90.74

86.15

91.40

88.37

89.97

68.61

57.49

91.67

84.12

Nor.Dolo.

6.82

2.11

4.41

1.67

7.34

8.05

5.37

4.02

4.39

4.27

1.67

8.05

4.85

LREEs

21.4

22.4

23

23.2

25.2

22

23.76

22.73

22.14

21.95

19.73

26.7

22.78

HREEs

6.2

7

7.2

7.9

6.4

6.3

7.5

7.7

5.6

4.7

4.5

8

6.65

REE/HREES

3.45

3.20

3.19

2.94

3.94

3.49

3.17

2.95

3.95

4.67

4.38

3.34

3.43

Sr/Ca

0.00098

0.00155

0.00104

0.00019

0.00098

0.00104

0.00088

0.00101

0.00099

0.00117

0.00031

0.00097

0.00098

Table 2

Correlation coefficients of the major oxides, trace, and rare earth elements in the studied carbonate rocks

 

CaO

MgO

SiO2

Al2O3

Fe2O3

Na2O

Ti

Sr

V

Cr

Mn

Co

Ni

Cu

Zn

Ga

As

Se

Br

Mo

Y

Zr

Ag

As

Sn

I

Ba

La

Nd

Sm

Hf

W

Bi

U

Th

CaO

1.00

                                  

MgO

0.41

1.00

                                 

SiO2

− 0.98

− 0.49

1.00

                                

Al2O3

0.20

0.19

− 0.19

1.00

                               

Fe2O3

0.45

0.42

− 0.48

0.20

1.00

                              

Na2O

0.39

0.00

− 0.39

0.60

0.50

1.00

                             

P2O5

0.07

0.04

0.01

0.33

− 0.20

− 0.18

                             

Ti

− 0.49

− 0.27

0.44

− 0.10

− 0.14

− 0.08

1.00

                            

Sr

− 0.37

− 0.03

0.34

− 0.56

0.03

− 0.42

0.38

1.00

                           

V

− 0.22

− 0.08

0.13

0.28

0.08

0.10

0.19

− 0.41

1.00

                          

Cr

− 0.04

0.05

− 0.09

− 0.13

0.37

0.05

0.44

0.06

0.71

1.00

                         

Mn

0.11

0.27

− 0.12

0.21

− 0.36

− 0.29

0.33

0.09

− 0.10

− 0.14

1.00

                        

Co

0.21

0.18

− 0.22

0.50

− 0.12

− 0.04

0.06

0.06

− 0.15

− 0.15

0.58

1.00

                       

Ni

0.17

− 0.02

− 0.12

0.54

0.36

0.24

0.26

0.15

− 0.16

− 0.08

0.31

0.68

1.00

                      

Cu

− 0.15

− 0.46

0.23

− 0.26

0.08

0.42

0.13

0.14

− 0.33

− 0.23

− 0.48

− 0.63

− 0.16

1.00

                     

Zn

− 0.05

− 0.02

0.08

− 0.31

0.42

− 0.24

− 0.02

0.71

− 0.26

0.00

− 0.05

− 0.03

0.35

0.12

1.00

                    

Ga

0.00

0.40

− 0.12

− 0.01

− 0.18

− 0.41

− 0.06

− 0.27

0.64

0.50

0.28

0.08

− 0.40

− 0.77

− 0.32

1.00

                   

As

− 0.48

0.01

0.44

− 0.40

0.11

− 0.35

0.01

0.06

0.30

0.34

− 0.62

− 0.53

− 0.42

0.00

− 0.01

0.25

1.00

                  

Se

0.23

0.37

− 0.24

− 0.29

− 0.17

− 0.31

− 0.24

− 0.34

− 0.15

− 0.04

− 0.07

− 0.15

− 0.47

− 0.25

− 0.54

0.37

0.42

1.00

                 

Br

0.45

0.25

− 0.45

− 0.24

0.58

− 0.14

− 0.36

0.36

− 0.09

0.18

− 0.06

0.01

0.19

− 0.18

0.79

0.03

− 0.08

− 0.26

1.00

                

Mo

− 0.36

− 0.10

0.38

− 0.07

0.29

0.30

0.18

0.57

− 0.44

− 0.23

− 0.38

− 0.19

0.21

0.66

0.42

− 0.75

0.09

− 0.43

− 0.03

1.00

               

Y

− 0.44

− 0.12

0.45

0.25

− 0.21

− 0.34

− 0.07

− 0.03

0.13

− 0.11

− 0.15

0.42

0.26

− 0.46

− 0.08

0.14

0.42

0.10

− 0.22

− 0.02

1.00

              

Zr

− 0.31

− 0.35

0.29

0.40

− 0.31

0.49

0.35

0.04

0.00

− 0.14

0.10

0.27

0.16

0.31

− 0.30

− 0.34

− 0.44

− 0.50

− 0.57

0.41

− 0.01

1.00

             

Ag

0.25

0.21

− 0.31

− 0.38

0.07

0.07

0.30

0.44

− 0.22

0.20

0.37

− 0.13

− 0.17

0.24

0.21

− 0.03

− 0.44

− 0.16

0.25

0.11

− 0.85

0.14

1.00

            

As

0.02

− 0.42

− 0.03

− 0.04

0.39

0.66

0.09

− 0.02

0.10

0.31

− 0.74

− 0.38

− 0.04

0.66

− 0.03

− 0.49

0.14

− 0.25

− 0.07

0.48

− 0.21

0.36

0.05

1.00

           

Sn

0.29

− 0.39

− 0.27

− 0.10

− 0.02

0.18

0.01

0.14

− 0.34

0.01

− 0.19

0.41

0.30

0.08

− 0.04

− 0.38

− 0.25

0.00

0.04

0.08

0.13

0.25

0.00

0.46

1.00

          

I

0.20

− 0.26

− 0.17

0.48

− 0.32

0.12

0.16

− 0.10

− 0.10

− 0.19

0.54

0.85

0.60

− 0.34

− 0.18

− 0.09

− 0.71

− 0.29

− 0.16

− 0.24

0.22

0.48

− 0.06

− 0.15

0.56

1.00

         

Ba

0.24

0.04

− 0.30

0.37

0.53

0.32

0.11

0.17

0.36

0.46

0.14

0.40

0.58

− 0.26

0.48

0.05

− 0.37

− 0.71

0.58

0.01

− 0.08

0.12

0.17

0.17

0.15

0.36

1.00

        

La

0.40

0.11

− 0.35

0.29

− 0.05

0.19

− 0.38

0.15

− 0.51

− 0.58

0.40

0.52

0.36

− 0.04

0.30

− 0.32

− 0.83

− 0.44

0.32

0.13

− 0.19

0.31

0.27

− 0.21

0.22

0.54

0.33

1.00

       

Nd

0.10

− 0.17

− 0.08

− 0.08

0.34

− 0.08

− 0.20

− 0.26

0.55

0.37

− 0.25

− 0.42

− 0.07

− 0.07

0.34

0.26

0.28

− 0.15

0.51

− 0.37

− 0.08

− 0.60

− 0.21

0.01

− 0.35

− 0.35

0.32

− 0.30

1.00

      

Sm

− 0.11

0.01

0.08

− 0.35

− 0.34

− 0.09

0.36

0.27

− 0.10

− 0.01

0.46

− 0.30

− 0.39

0.32

0.00

0.04

− 0.36

− 0.14

− 0.12

0.03

− 0.75

0.25

0.83

− 0.15

− 0.33

− 0.13

− 0.15

0.15

− 0.18

1.00

     

Hf

0.44

0.07

− 0.42

− 0.24

0.77

0.34

0.10

0.21

− 0.23

0.30

− 0.36

− 0.27

0.27

0.42

0.41

− 0.46

0.09

− 0.01

0.47

0.32

− 0.41

− 0.33

0.28

0.53

0.30

− 0.28

0.24

− 0.16

0.23

− 0.13

1.00

    

W

− 0.14

0.00

0.14

0.84

0.30

0.60

0.29

− 0.32

0.31

0.07

− 0.01

0.31

0.60

0.00

− 0.23

− 0.21

− 0.08

− 0.34

− 0.39

0.26

0.33

0.47

− 0.41

0.23

− 0.07

0.29

0.31

− 0.08

− 0.11

− 0.38

− 0.01

1.00

   

U

0.34

0.32

− 0.27

0.54

0.25

0.36

− 0.17

− 0.06

− 0.30

− 0.49

0.46

0.24

0.49

0.09

0.29

− 0.34

− 0.67

− 0.45

0.21

0.19

− 0.32

0.14

0.20

− 0.29

− 0.33

0.21

0.30

0.69

− 0.03

0.21

0.03

0.31

− 0.58

1.00

 

Th

0.14

− 0.50

− 0.04

0.10

0.20

0.69

− 0.20

− 0.22

− 0.20

− 0.30

− 0.55

− 0.43

0.01

0.85

0.02

− 0.75

− 0.19

− 0.33

− 0.09

0.46

− 0.35

0.33

− 0.01

0.73

0.23

− 0.09

− 0.04

0.16

0.08

0.00

0.37

0.18

− 0.59

0.22

1.00

Discussion

Mineralogy

X-ray patterns revealed that the dominating minerals in the studied samples are mainly calcite as well as dolomite, quartz, halite, pyrite, and clay minerals. The EDX analysis data for the bulk samples show that this phase of dolomite is nearly stoichiometry (Mg: Ca ≈ 1:1) and the size of the dolomite crystals is up to 80 μm without any zoning. Also, present of halite which conformed with the X-ray analysis. Dolomite crystals are unimodal and polymodal; planar-e and planar-s as well as some are interlocked (Fig. 3). Also, the photo is showing patches from disorder from halite crystals, which is conformed with X-ray results.
Fig. 3
Fig. 3

BSE image and EDX analysis data showing the dolomite crystals is up to 80 μm and patches of halite

Petrography

The faunal assemblage that characterizes the studied succession consists of forminifera, Nummulites, pelecypods, miliolids as well as echinods fragments, and others. Petrographically, five major microfacies were encountered in the studied section:

Nummulitic biomicrite wackestone/mudstone microfacies

This microfacies is the most prevailing microfacies in the studied section of Gebel El-Qurn. It consists mainly of 35% fossils and 4% quartz grains embedded in micrite and microsparite matrix. Some of the microcrystalline matrix is stained by iron oxy-hydroxides and exhibits re-crystallization to microsparite. Allochems are mainly represented by abundant nummulites species, Nummulite gizehensis and Nummulite discorbinus, as well as amounts of gastropods, pelecypods, miliolids, bryozoa, and others (Figs. 4 and 5). This microfacies shows considerable variation in the size of the allochems. The large nummulite size possibly indicates higher salinity and adequate paleoecologic conditions (Plumley et al. 1962) and presumably characteristic of warm open marine condition (Wilson 1975). The sand content is monocrystalline, fine to medium, subangular to subrounded quartz grains scattered in the matrix.
Fig. 4
Fig. 4

Nummulitic biomicrite (wackestone/mudstone) microfacies showing Nummulite gizehensis, as well as amounts of gastropods and others scattered in micritic matrix, PPL

Fig. 5
Fig. 5

Nummulitic biomicrite (wackestone/mudstone) microfacies showing Nummulite discorbinus embedded in sparite matrix and dissolution, PPL

Nummulitic biosparite (grainstone) microfacies

The allochems content are represented by nummulites (50–70%), and other fossils are embedded in sparite matrix (grainstone). Nummulites vary from 10 to 25 mm in diameter (Fig. 6). The nummulites are leached and later on filled with sparry calcite or micrite, and some are stained with iron oxy-hydroxides. Those retaining their original fibrous structure are occasionally present.
Fig. 6
Fig. 6

Nummulitic biosparite (grainstone) showing Nummulite gizehensis are embedded in sparite matrix (grainstone) as well as compaction and dissolution. Note: Nummulite gizehensis filled with sparry calcite and micrite, PPL

Nummulitic rudstone

The rudstone microfacies is made up of nummulites (30 to 40%), foraminifera (3%), and quartz grains (5 to 6%). Allochems are embedded and cemented with sparry calcite (Fig. 7). Nummulites reach up to 35 mm in diameter. Some foraminifera and miliolids are enclosed in microsparite cement. The allochems (fossils) are mostly filled with sparry calcite, but a few miliolids and algae are micritized and have a micritic envelope (Fig. 8). Monocrystalline and polycrystalline, medium to coarse, subangular to rounded quartz grains are embedded in the matrix.
Fig. 7
Fig. 7

Nummulitic rudstone microfacies showing Nummulite gizehensis embedded in sparry calcite matrix, PPL

Fig. 8
Fig. 8

Nummulitic rudstone microfacies showing the fossils are mostly filled with sparry calcite, but a few miliolids and algae are micritized and have a micritic envelope. Note: Compaction and the micritic envelope, PPL

Pelecypod biomicrite (wacke/packstone) microfacies

This microfacies is present in the upper part of the studied section in Thebes Formation. The allochems are represented mainly by pelecypod shells (35%), and few algae and micritic peloids are present. This association is texturally considered as a biomicrite (wacke to packstone) in a matrix (Fig. 9). The sediments are loosely packed inferring that cementation occurred before significant compaction. Micrite envelope outlined the skeletal grains of pelecypods, with microsparite pore-filling.
Fig. 9
Fig. 9

Pelecypod biomicrite (wacke/packstone) microfacies showing a mega-sized pelecypod embedded in micritic matrix as well as a compaction effect, PPL

Biomicrite dolomitic lime-mudstone microfacies

The fossils are only allochems in this microfacies (20%). They are mainly of nummulites species, miliolids, and other shell fragments scattered in the micritic matrix (Fig. 10). This microfacies is characterized with fine anhedral crystals, closed packing, and intercrystalline porosity.
Fig. 10
Fig. 10

Biomicrite dolomitic lime-mudstone microfacies showing of nummulites species, miliolids, and others shell fragments scattered in the micritic matrix. Note: Compaction and the micritic envelope, PPL

Diagenesis

Carbonate rocks are particularly susceptible to diagenesis partly because minerals are more soluble in water and so are subject to dissolution and re-precipitation. The main diagenetic features encountered in the carbonate rocks of Geble El Gurna are described below:

Cementation

Two types of micrite and microsparite cementation are recorded in the studied samples. Micrite and sparite cemented the allochems together, (Figs. 4 and 5), which indicated that it had taken place when the pore-fluid becomes supersaturated with respect to cement phase (Tucker and Wright 1990). Micrite and microsparite are also observed to be filling the intergranular pores and lining the chambers of bioclastics (Figs. 4, 6, and 8). Micrite is of early diagenetic marine origin (Longman 1980). The original micrites were occasionally replaced by coarser mosaics of microspar through aggrading neomorphism. This cement is early diagenetic formed in the phreatic zone.

Neomorphism

Neomorphism is demonstrated where former aragonite bioclasts have been calcitised-retaining elements of the original structure (Figs. 5 and 6). The nummulite, foraminiferal, and pelecypoda shells were re-crystallized to unequigranular microspar crystals before leaching. While some algae and millolids were re-crystallized to equigranular microspar, also some other shell fragments were re-crystallized to sparry calcite. The re-crystallization is typically associated with crystal growth and transformation of the metastable Mg-calcite and aragonite to calcite under meteoric and burial diagenetic environments (Tucker and Wright 1990). Thus, the original micrites were transformed to coarser mosaics of microspar through aggrading neomorphism.

Bioclastics which are made originally of aragonite may be dissolve in most cases during diagenesis and are filled with micrite (Figs. 8 and 10). This micritization process took place at or just below the sediment-water interface (Tucker and Wright 1990). Margins of some nummulites, millolids, and pelecypods become completely micritized forming a micrite envelope (Fig. 8), which points to deposition under a shallow water regime at an early stage of diagenesis (Bathurst 1975).

Compaction

The effect of mechanical compaction on carbonate sediments was decreased by early cementation either in the marine environment or during meteoric diagenesis (Tucker and Wright 1990) Mechanical compaction is clearly observed in the closer packing of bioclastics, also showing penetration and reduction of shell fossil fragments (Figs. 8, 9, and 10). It is suggested that the compaction has initiated at an early stage before complete cementation (cf. Adams and Mackenzie 1998).

Dissolution

Under the effect of the meteoric waters, the unstable mineral suite consisting of aragonite and magnesian calcite (metastable phases) changes to stable phase and re-precipitated by the dissolution process. Dissolution plays a little role in the diagenesis of the carbonate rocks of Geble El Gurna. This process involves partial or, rarely, completes leaching of some fossils and shell fragments as well as some vugs and micro-channels in the matrix due to tectonic effect (Figs. 5 and 6). Dissolution takes place mostly in the near-surface meteoric condition (Tucker and Wright 1990). The dissolution processes and secondary porosity indicate early diagenetic stage. Selective destruction and void formation are due to the solubility of the shells. Generally, this rock type indicates shallow marine subtidal environment.

Dolomitization

Magnesium is pronounced in the succession in all samples. The neomorphism of high magnesian-calcite foraminiferal tests, algae, and miliolids to calcite evolves Mg2+, which plays a significant role in the dolomitization process (Maliva and Dickson 1994). The possible sources of Mg ions required to initiate dolomitization could be transformations of metastable Mg-calcite and aragonite to calcite upon deep burial seawater and/or connate Mg-bearing water circulating through sediments. The dolomite rhombs are unimodal and polymodal, idiomorphic to hypidiomorphic, and equigranular in texture with crystal size ranging from 10 to 80 μm (Fig. 3). The dolomite rhombs are fine crystalline and unzoned, and the author suggests that dolomitization of the studied carbonate rocks is most probably post-depositional and took place in the mixing zone between meteoric and marine phreatic zones.

Geochemistry

Chemical analysis data of major, trace, and rare earth elements are listed in Table 1. Normative calcite content varies from 57.49 to 91.76%, averaging 84.12%, while the normative dolomite content ranges from 1.67 to 8.05%, averaging 4.85%. Calcite precipitated from seawater would contain from 5.9 to 27.1% MgCO3 by weight. While calcite exposed to meteoric water diagenesis will lose most of its magnesium content (Moore 1989; Morse and Mackenzie 1990). The studied rocks contain 4.76% MgCO3, in average, indicating that the studied calcite subjected to progressive diagenesis, which led to loose most of its magnesium content under meteoric water. MgO content ranges from 0.8 to 3.85%. It seems more eligible that the dolomitization process is controlled by the fracture and joint systems in the area, which maintain access to the dolomitizing fluids. Positive correlation (r = 0.41) between Ca and Mg indicated calcite is present as calcite and dolomite (Table 2), which agrees with X-ray results.

SiO2 content in the studied samples ranges from 1.25 to 5.33% expected samples number 2 and 10, which represented limestones with nodular flint. The highest SiO2 value is detected at the top bed of the succession indicating an upward increase in the influx of terrigenous constituent of the depositional basin.

The carbonate rocks of the studied succession record a low content of Al2O3 and K2O (average 1.64 and 0.03%; respectively). The low content of both Al2O3 and K2O can mainly be attributed to the low clay content. Si/Al ratio is about 3 (without S. Nos. 2 and 10), suggesting a three-layer clay structure. Moreover, the preponderance of K indicates possible smectite-illite mixed layer.

Fe2O3 content of the studied carbonate rocks ranges from 0.64 to 0.91%, averaging 0.81% (Table 1). The low values for the Geble El Gurna carbonate rocks indicate the formation of dolomite in the near-surface oxidizing environment (Choquette and James 1990). Positive correlation (r = 0.42, Table 2) between Fe2O3 and MgO indicates that iron may be associated with dolomite. Also, the positive correlation between Fe2O3 and Sr (r = 0.38) indicates that iron oxy-hydroxides may be scavenge and uptake Sr, which is an essential function of many microbes. This is in agreement with Krumbein (1983), Abou El-Anwar (2005, 2011, 2014, and 2016), and Abou El-Anwar et al. (2017, 2018).

Trace element data of sedimentary carbonate rock can be used to constrain the chemical composition of ancient seawater (Veizer and Mackenzie 2014; Kamber et al. 2014). Sodium is present in the carbonate rocks sodium co-precipitated with the carbonate minerals, which gives an indication of salinity of water from which the original carbonates were deposited (Moore 1989; Morse and Mackenzie 1990). Na2O content of the studied samples ranges from 0.1 to 0.12%, averaging 0.15%. Na content may be attributed to the presence of halite which is conformed with the X-ray results. There are positive correlation between Na and Cl (r = 0.55, Table 2), which indicate high salinity during precipitation, so the studied area effected by dry climate, in agreement with the petrographic study. Sodium occurs in modern carbonate sediments to levels of about 3000 ppm and progressively drops with diagenesis to 200 ppm in ancient limestone (Scoffin 1987). The sodium content of the studied carbonates ranges from 800 to 1394 ppm, averaging 1100 ppm. This means that there is loss in Na content during diagenesis of the studied carbonate rocks. Therefore, the diagenesis processes may have taken place in an environment less saline than seawater (Loukina and Abou El-Anwar 1994; Loukina et al. 2001; Abou El-Anwar 2006; Abou El-Anwar 2011). This agrees with the environments of dolomitization in mixed marine/meteoric water (Badiozamani 1973).

The strontium content for the majority of the ancient carbonate is less than 500 ppm (Bathurst 1975). The Sr-contents of Geble El Gurna ranges from 400 to 520 ppm, averaging 483 ppm, which indicated that the dolomite crystals deposited in mixing zone of marine and meteoric water (Table 1). The depletion in Sr content can be attributed to the long diagenetic history particularly the dolomitization stages. This agrees with the findings of Brand and Veizer (1980); Loukina and Abou El-Anwar (1994). Strontium concentrations can be utilized for understanding the nature of the dolomitize fluid. Remnant inclusions of precursor carbonate (calcite or aragonite) and distribution coefficient of Sr (Dsr) between dolomite and diagenetic fluids are generally the major factors controlling the Sr concentrations in dolomite (Budd 1997). Therefore, the dolomites reflect mostly the nature of the dolomitize fluid. Estimates of Sr distribution coefficient (Dsr) for dolomite vary from 0.015 to 0.06 (Vahrenkamp and Stewart 1990; Banner 1995; Budd 1997). If the Sr content were mainly due to Dsr and Sr/Ca of the dolomitize fluid, the latter can be calculated from equation (Sr/Ca) dolomite = Dsr (Sr/Ca) fluid. Such calculations yield molar Sr/Ca for the Geble El Gurn dolomitization fluid of 0.00031 to 0.000974 with average 0.000984. These values are significantly less than the Sr/Ca ratio of present day seawater (0.0086; Drever 1988). Thus, the average Sr value suggesting that we are dealing with Sr-depleted dolomitizing fluids, likely due to partial or full meteoric water contributions (Abou El-Anwar 2010, 2012; Abou El-Anwar and Mekky 2013).

However, post-depositional diagenetic and metamorphic processes may modify the mineralogical compositions, concentrations of mobile trace elements (Webb et al. 2009). The fluid-immobile elements, such as the rare earth elements (REEs) and high-field strength elements (HFSE), remain largely unaffected by diagenesis (Webb et al. 2009); thus, they are useful for recognize the ancient environmental conditions. The mean values of the ΣREEs for the studied samples are 936 ppm. The studied carbonate rocks showed significant enrichment of LREEs and a well-depleted pattern of HREEs (Table 1). The total concentration of total REEs in average bulk continental crust is about 125 ppm (Rudnick and Gao 2003). Thus, geochemical pattern of the studied samples mentioned that high solubility and mobility potential of LREEs compared with HREEs, resulting in good fractionation and enrichment of these elements in the depositional environment. So, the concentration of the (LREEs) is higher than that of (HREEs), which is in conformance to the general distribution of REEs in shale or limestone (Gromet et al. 1984; Condie 1991; Ketris and Yudovich 2009).

The concentrations of REEs in ocean waters reflect different inputs, such as river and eolian flux (Zhao et al. 2009), hydrothermal alteration of oceanic crust (Michard and Albarede 1986), and diagenesis (Derry and Jacobsen 1990). Thus, the study of REE concentrations of the studied carbonate rocks is a useful tool to define the depositional environment; fresh water or marine conditions (cf. Bolhar and Van Kranendonk 2007), hydrothermal input (cf. Derry and Jacobsen 1990; Allwood et al. 2010), and redox conditions (De Baar et al. 1988; Elderfield 1988; Kato et al. 2002). The primary distribution pattern of REEs in many carbonates has survived irrespective of their age, provenance, post-depositional processes, and metamorphic grade (Bau and Möller 1993; Webb et al. 2009).

Positive values of La and Ga are a common feature of seawater (Bau et al. 1997; Alibo and Nozaki 1999) which suggested that the higher stability of them in seawater relative to neighboring REEs during scavenging. Thus, La and Ga content indicated that the investigated carbonate rocks were deposited in marine environment. Metals may be depleted resulting to REE oxidation state and mobility under different oxidation-reduction conditions (Wang and Liang 2014; Abou El-Anwar et al. 2018). A positive relation between Fe with Hf, Br, As, I, Ba, Nd, and W indicates that iron is increasing the buffer capacity of the studied carbonate matrix; therefore, these REE may be co-precipitated with Fe.

Thus, light REEs are scavenged preferentially from the water condition compared to the heavy REEs (De Baar et al. 1985; German and Elderfield 1990; German et al. 1991). Thus, this process in the studied carbonate rocks is resulting for dissolved REEs in oxic seawater under redox behavior (De Baar et al. 1985, 1988; Byrne and Sholkovitz 1996).

The total radioactivity measurements are ranging from 4 to 5.9 ppm for U and from 5.5 to 6.6 ppm for Th. The radioactivity measurements are less than the background level of carbonates, and they are in the allowed limits for carbonate rocks and representative of less contaminated samples. Thus, the investigated carbonate rocks can be used in cement industries and as building stones (cf. Abou El-Anwar et al. 2017; Abou El-Anwar 2018).

Conclusions

The carbonate rocks of Gebel El-Qurn, west Luxor were deposited under shallow, warm open marine environment, as witnessed by the large number of shallow marine fauna (forminifera, gastropods, pelecypods, miliolids) besides algae and echinoid fragments. Also, the occurrence of nummulites indicated that these rocks were deposited under a shallow, subtidal—intertidal, warm marine environment.

The microfacies association of the studied carbonate sediments is grouped into (1) nummulitic bioclastic wackestone/mudstone, (2) nummulitic biosparite grainstone, (3) nummulitic rudstone microfacies, (4) pelecypod biomicrite wacke/packstone, and (5) biomicrite dolomitic lime-mudstone. The main diagenetic processes affecting the Lower Eocene Thebes Formation are as follow: cementation, neomorphism, compaction, dissolution, and dolomitization. Diagenesis occurred under submarine and subaerial environments. The submarine environment resulted in the formation of micritic envelope, micritization, micritic cement, compaction, and dolomitization. The subaerial diagenesis is manifested by the presence of extensive cementation, neomorphism, and dissolution.

The large nummulite size reflects deposition in a shallow, warm and open marine environment. The fine and medium quartz grains in the sediments are mostly angular to subrounded indicating that they were transported by streams and deposited in an environment characterized by a low average kinetic energy. The quartz grains are monocrystalline, which most probably represents an igneous source.

The dolomite rhombs recorded in the sediments range in a diameter from 10 to 80 μm. The formation of the dolomite took place in a near-surface environment and from less saturated solutions.

Mineralogically, the studied carbonate rocks consist mainly of calcite, dolomite as well as quartz, halite, pyrite and clay minerals. The studied dolomite samples are generally non-stoichiometric being formed from solutions with lower Mg/Ca ratio in a mixed zone.

Geochemically, SiO2 record higher value at the top beds of the studied succession, suggesting an upward increase in the influx of terrigenous constituents to the basin of deposition. The low iron content of the studied dolomite indicates precipitation under near-surface oxidizing environment. However, the low co-precipitated Na and Sr than the normal salinity of seawater, means possible loss in Na and Sr content during diagenesis. Therefore, the diagenetic processes may have taken place in an environment less saline than sea water besides; the dolomites were precipitated under mixed marine/meteoric water environment. LREEs are higher than HREEs and concentrated under redox condition. The radioactive Th and U are less than the background level of carbonates, and they are in the permissible limits for carbonates.

Declarations

Acknowledgements

The authors would like to thank the Geological Sciences Dept., National Research for its facilitates during this work.

Authors’ contributions

All authors contributed equally in all article steps. All authors read and approved the final manuscript.

Ethics approval and consent to participate

Accepted.

Consent for publication

Accepted.

Competing interests

The authors declare that they have no competing interests.

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Authors’ Affiliations

(1)
Geological Sciences Department, National Research Centre, 33 El Bohouth St. (former El Tahrir St.)-Dokki, POB: 12622, Giza, Egypt

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