1. Introduction

OJG

Open Journal of Geology

2161-7570

Scientific Research Publishing

10.4236/ojg.2017.710098

OJG-79634

Articles

Earth&Environmental Sciences

Mineral Chemistry of Wehrlite Xenoliths Hosted in Basalts from the SW of Hosséré Dammougalré (Adamawa Plateau, Cameroon): Thermobarometric Implications

Isaac

Bertrand Gbambié Mbowou

¹^*Dagwaï

Nguihdama

²Fadimatou

Ngounouno Yamgouot

³Mama

Ntoumbe

¹Abdel

Aziz Youpoungam

¹Ismaïla

Ngounouno

Department of Life and Earth Sciences, Higher Teachers’ Training College, University of Maroua, Maroua, Cameroun

School of Geology and Mining Engineering, University of Ngaoundere, Ngaoundere, Cameroon

Department of Earth Sciences, Faculty of Science, University of Ngaoundere, Ngaoundere, Cameroon

* E-mail:mbowou2000@yahoo.fr(IBGM);

16102017

07101465147724, August 201713, October 2017 16, October 2017

2014

This work is licensed under the Creative Commons Attribution International License (CC BY). http://creativecommons.org/licenses/by/4.0/

Wehrlite samples (size: ~4 cm) hosted in basaltic lavas from the SW of Hosséré Dammougalré are located in the western Adamawa Plateau. Porphyritic and allotriomorphic texture characterize respectively host Basalt and wehrlite xenoliths. The phenocrysts of olivine (Fo _68−74), and Ti-magnetite are scattered in host basalt. Wehrlite xenoliths (~4 cm size) contain Cr-rich clinopyroxene (diopise-augite), olivine (Fo _76−88) and chromiferous spinel. Equilibrium temperatures calculated from Fe/Mg exchange reaction for olivine/spinel vary between 944 °C and 1102 °C. The wehrlite olivine crystals with low Fo (<90) indicate a re-equilibration of Fe-Mg in the host basalt at low temperatures. All the analyzed wehrlite clinopyroxenes have crystallized at high pressures as evidenced by the Al ^vi and Al ^iv contents. The studied spinel-bearing wehrlite xenoliths represent probably the residual portions of the upper mantle, which are an important source of information about lithospheric composition and thermal evolution beneath the Adamawa Plateau.

Wehrlite Adamawa Plateau Hosséré Dammougalré Mineral Chemistry Geothermometry

1. Introduction

The accidental fragments called rock xenoliths, piked up by the turbulent host magma on its ascent, allowed to characterize petrologically the Earth’s upper mantle. They are an important source of information about lithospheric composition and thermal evolution in mantle regions associated with alkaline volcanism [1] . In the Adamawa Plateau (Figure 1), previously ultramafic xenoliths data are from Dibi area ( [2] [3] ), Youkou maar [4] , Ngao Voglar [5] and Hosséré Garba [6] . These ultramafic xenoliths studied are chiefly of dunite and lherzolite composition. Thus, the discovery of the wehrlite samples from the SW of Hosséré Dammougalré could improve the knowledge of the upper mantle beneath the Adamawa Plateau. Indeed, wehrlite samples hosted in basaltic lavas from the SW of Hosséré Dammougalré are located in the western Adamawa Plateau (Figure 1). Adamawa Plateau is a tectonomagmatic domain bordered by faults oriented N70˚E [7] . This plateau presented as the horst, is situated to the north of the Congo Craton, as the result of the fold belt shearing, oriented WSW-ENE [8] .

The aims of this paper are to present the first petrographical, mineral chemistry and thermobarometric data of the wehrlite xenoliths from the SW of Hosséré Dammougalre, chiefly to enhance the knowledge of upper mantle beneath the Adamawa Plateau.

2. Geological Description of the Studied Zone

The geological sketch established for the studied zone is presented (Figure 2). The trachytic outcrops of Hosséré Dammougalré and Hosséré Doro are surrounded by several basaltic units (lower, middle and upper). The lower basaltic units were almost completely weathered and converted into black reddish ferralitic soils or the clusters of residual ferruginous vacuolar cuirasses. The intermediate or middle basaltic units were fragmented into angular or rounded blocks of various sizes (5 - 50 cm), slightly weathered and dispersed. The upper basaltic units were represented by the blocks accumulated as small isolated hills (diameter: ~500 m; height <30 m). These hills consist of small prismatic blocks (0.2 - 1.7 m) and vertical columnar jointing (0.5 to 2 m) of basalt. The studied xenoliths (size: ~4 cm) were sampled within these upper basaltic units at the SW of Hosséré Dammougalré. The Hosséré Dammougalré (altitude: ~1600 m a.s.l) is a neck of needle-shaped lava which have circular basis (diameter: ≈200 m) and more or less steep slopes (45˚ - 90˚). This formation is strongly prismatic and dismantled into blocks, disseminated in chaos on the soil. However, the Hosséré Doro is a dome bounded by small steep cliffs (20 - 40 m high) and the lava blocks are accumulated to the foothill.

3. Analytical Methods

The mineral phases were analyzed in polished thin sections with the electron microprobe analyzer using a Cameca microprobe SX100 at the “Université Pierre et Marie Curie”, Paris VI (France). The standards data used for analysis are from natural (Si, Al and K on orthoclase, Ca on anorthite, Na on albite, P on apatite, Zr on zircon) and synthetic (Fe on Fe₂O₃, Ba on BaO₄, Sr on SrSiO₃)

phases.

The measurements were carried out with a beam size of 10 - 100 µm, under the following conditions expressed in kV (accelerating voltage), nA (beam current) and s (counting times at the peak): Olivine (15 kV, 40 nA, 20 s for all elements, except Si (10 s)), clinopyroxene (15 kV, 40 nA, 20 s for Si, Al, Fe, Mg, Ca, Na, Mn and 30 s for Ti and Zr), feldspar (15 kV, 10 nA, 5 s for all elements), Fe- Ti oxides and spinel (15 kV, 40 nA, 40 s for Ti, Fe, Mn, Mg, 10 s for Si, 15 s for Cr and 30 s for Al). Measurements correction was carried out using the “PAP” program [9] .

4. Results4.1. Petrography

Host Basalt is characterized by a porphyritic texture. The phenocrysts of olivine (~2 mm), clinopyroxene (1.2 - 2.1 mm) and Fe-Ti oxides (0.5 - 0.6 mm) are scattered in a groundmass consisting of clinopyroxene, Fe-Ti oxides and plagioclase microlites. Olivine phenocrysts are subhedral, cracked and their edges are sometimes destabilized into iddingsite. Clinopyroxene phenocrysts are euhedral and twinned.

Wehrlite xenoliths (~4 cm size) are characterized by an allotriomorphic texture, with inequigranular olivine (~40 vol.%), clinopyroxene (~55 vol.%) and spinel (~5 vol.%) crystals. Spinel crystals are red brown and interstitial between the crystals of olivine and clinopyroxene. The contact between the host basalt and wehrlite xenoliths is materialized by the accumulation of small Fe-Ti oxides and plagioclase crystals or the tiny host basalt veins.

4.2. Mineral Chemistry4.2.1. Olivine

In the host basalt, forsterite (Fo) values calculated for the analyzed olivine phenocrysts (Table 1) reach 73 - 74 and 68 - 72, respectively for the core and the rim. The CaO contents are high (rim, up to 0.43 wt% and core, up to 0.41 wt%). Using bulk-rock composition as a liquid at the total pressure of 1 atm, the crystallization temperatures were estimated after [10] for the core and the rim respectively to 1224˚C ± 60˚C and 1166˚C ± 48˚C.

For wehrlite xenoliths, the forsterite component (Table 1) range from 76 to 88. These values are similar to those calculated for the wehrlites from the Mount Cameroun (Fo_82-86; [11] ). NiO contents reaching 0.19 wt% and CaO up to 0.39 wt%.

4.2.2. Clinopyroxene

The clinopyroxene phenocrysts (Table 2) of the host basalt are both diopside and augite (after the nomenclature of [12] ; Figure 3). Their Cr₂O₃ contents range from 0 wt% to 0.38 wt%), while TiO₂ and Al₂O₃ contents are high (up to 3.9 wt% and 8.7 wt% respectively). The high contents of Ti and Al^iv (apfu: atom per formula unit) in diopside and augite are linked to a low-pressure of crystallization [13] .

Wehrlites contain also diopside and augite, but poor in Al₂O₃ (1.8 - 5.1 wt%), TiO₂ (0.8 - 1.7 wt%) and rich in Cr₂O₃ (up to 0.59 wt%) with Cr# (= 100 × atomic Cr/(Cr+Al)) up to 15.6.

Table 1 Representative compositions of olivine of the host basalt and the studied wehrlite

rocks	host basalt						wehrlite
sample nb.	132	132	132	132	132	132	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1
description	ph,r	ph,c	ph,c	ph,c	ph,c	ph,r
SiO₂ (wt%)	37.02	37.09	37.07	37.15	36.62	37.98	38.27	37.43	38.39	38.99	38.86	37.31	36.36	36.74
Al₂O₃	0.10	0.06	0.00	0.00	0.11	0.04	0.01	0.02	0.00	0.07	0.09	0.05	0.00	0.00
FeO	27.25	24.15	24.50	23.99	24.69	25.29	18.58	19.22	19.46	15.09	15.71	15.95	22.86	23.62
MnO	0.92	0.58	0.60	0.60	0.40	0.57	0.37	0.20	0.42	0.05	0.17	0.21	0.53	0.51
MgO	32.93	36.18	36.33	36.51	36.52	35.87	41.84	41.33	41.78	44.54	44.73	44.81	37.83	37.30
CaO	0.30	0.41	0.39	0.38	0.36	0.43	0.30	0.29	0.32	0.15	0.17	0.15	0.36	0.39
NiO	0.09	0.16	0.12	0.09	0.04	0.11	0.04	0.05	0.15	0.17	0.11	0.19	0.00	0.08
Total	98.73	98.64	99.00	98.73	98.74	100.28	99.41	98.55	100.50	99.05	99.83	98.67	97.93	98.64
Si (apfu)	1.008	0.990	0.987	0.990	0.976	1.002	0.982	0.971	0.978	0.988	0.978	0.949	0.968	0.975
Al	0.003	0.002	0.000	0.000	0.003	0.001	0.000	0.001	0.000	0.002	0.003	0.001	0.000	0.000
Fe²⁺	0.620	0.522	0.518	0.513	0.505	0.558	0.364	0.359	0.371	0.297	0.289	0.237	0.444	0.475
Mn	0.021	0.013	0.013	0.014	0.009	0.013	0.008	0.004	0.009	0.001	0.004	0.004	0.012	0.011
Mg	1.337	1.440	1.441	1.450	1.451	1.411	1.601	1.598	1.587	1.682	1.678	1.699	1.501	1.476
Ca	0.009	0.012	0.011	0.011	0.010	0.012	0.008	0.008	0.009	0.004	0.005	0.004	0.010	0.011
Ni	0.002	0.003	0.002	0.002	0.001	0.002	0.001	0.001	0.003	0.003	0.002	0.004	0.000	0.002
Fo (%)	68	73	74	74	74	72	81	82	81	85	85	88	77	76
Fa	32	27	26	26	26	28	19	18	19	15	15	12	23	24
mg#	68.30	73.41	73.56	73.84	74.17	71.66	81.49	81.65	81.07	84.99	85.29	87.74	77.16	75.65

ph.r: phenocryst. rim; ph.c: phenocryst core.

Table 2 Representative compositions of clinopyroxene of the host basalt and the studied wehrlite

rocks	host basalt				wehrlite
sample nb.	132	132	132	132	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1	132-1
description	ph.c	ph.r	ph.c	ph.c
SiO₂ (wt%)	44.07	47.59	50.66	47.01	51.06	51.80	51.60	50.69	50.90	51.93	50.99	53.18	51.14	50.43	52.17	50.29	47.72	50.86	51.10
TiO₂	3.91	1.98	0.65	1.95	0.89	1.78	0.97	1.03	0.99	0.93	0.94	1.19	1.21	0.92	0.83	1.16	3.04	1.61	0.93
Al₂O₃	8.75	7.23	5.27	8.29	4.60	4.33	3.20	4.97	4.65	4.87	4.76	1.85	3.86	5.19	4.76	3.73	5.30	3.20	4.70
Cr₂O₃	0.00	0.06	0.25	0.38	0.34	0.55	0.46	0.43	0.37	0.50	0.30	0.51	0.53	0.59	0.43	0.51	0.00	0.49	0.47
FeO	6.92	6.68	6.90	6.21	5.46	4.91	4.53	5.73	5.13	4.91	5.23	4.46	5.24	5.07	5.04	5.85	7.30	5.27	5.46
MnO	0.32	0.21	0.15	0.17	0.13	0.13	0.11	0.12	0.11	0.04	0.02	0.11	0.23	0.16	0.04	0.05	0.00	0.25	0.08
MgO	11.56	13.18	17.67	13.84	15.52	15.00	15.89	16.36	15.31	15.12	15.54	16.27	15.50	15.29	15.35	14.64	12.68	14.86	15.00
CaO	22.34	21.49	17.18	21.21	21.17	20.77	22.17	18.42	20.55	20.66	20.52	21.53	20.93	20.65	20.01	21.97	22.38	22.01	21.05
Na₂O	0.49	0.60	0.68	0.56	0.79	0.59	0.62	0.82	0.89	0.85	0.81	0.71	0.70	0.84	0.72	0.57	0.62	0.47	0.77
Total	98.37	99.02	99.40	99.60	99.94	99.85	99.55	98.57	98.91	99.80	99.12	99.81	99.33	99.12	99.35	98.75	99.04	99.01	99.57
Fe₂O₃ (calc.)	2.91	0.79	2.84	3.14	0.97	0.00	1.84	0.97	1.40	0.00	1.28	0.00	1.01	1.88	0.00	1.77	1.81	0.13	0.00
FeO (calc.)	4.31	5.97	4.35	3.38	4.59	4.91	2.88	4.86	3.88	4.91	4.07	4.46	4.33	3.38	5.04	4.26	5.67	5.15	5.46
Total (calc.)	98.66	99.10	99.69	99.91	100.04	99.88	99.76	98.67	99.05	99.87	99.26	99.81	99.45	99.35	99.40	98.93	99.22	99.06	99.57
Si (apfu)	1.670	1.793	1.850	1.736	1.885	1.907	1.894	1.873	1.879	1.901	1.877	1.948	1.886	1.857	1.919	1.874	1.793	1.892	1.900
Ti	0.111	0.056	0.018	0.054	0.025	0.049	0.027	0.029	0.027	0.026	0.026	0.033	0.033	0.025	0.023	0.032	0.086	0.045	0.026
Al^VI	0.061	0.114	0.077	0.097	0.085	0.094	0.032	0.089	0.081	0.111	0.084	0.028	0.053	0.082	0.125	0.038	0.028	0.033	0.105
Al^IV	0.330	0.207	0.150	0.264	0.115	0.093	0.106	0.127	0.121	0.099	0.123	0.052	0.114	0.143	0.081	0.126	0.207	0.108	0.100
Cr	0.000	0.002	0.007	0.011	0.010	0.016	0.013	0.013	0.011	0.014	0.009	0.015	0.015	0.017	0.012	0.015	0.000	0.014	0.011
Fe^{3+ (VI)}	0.083	0.022	0.078	0.087	0.027	0.000	0.051	0.027	0.039	0.000	0.035	0.000	0.028	0.052	0.000	0.050	0.051	0.004	0.000
Fe²⁺	0.136	0.188	0.133	0.104	0.142	0.151	0.088	0.150	0.120	0.150	0.125	0.136	0.134	0.104	0.155	0.133	0.178	0.160	0.170
Mn	0.010	0.007	0.005	0.005	0.004	0.004	0.004	0.004	0.004	0.001	0.001	0.004	0.007	0.005	0.001	0.002	0.000	0.008	0.003
Mg	0.653	0.740	0.962	0.762	0.854	0.823	0.870	0.901	0.842	0.825	0.853	0.888	0.852	0.839	0.842	0.813	0.711	0.824	0.831
Ca	0.907	0.827	0.672	0.839	0.798	0.819	0.871	0.729	0.813	0.810	0.809	0.845	0.827	0.815	0.789	0.877	0.901	0.877	0.799
Na	0.036	0.044	0.048	0.040	0.056	0.042	0.044	0.059	0.064	0.060	0.058	0.050	0.050	0.060	0.051	0.041	0.045	0.034	0.055
Wo (%)	46.56	41.93	33.15	42.43	41.56	43.24	45.41	37.60	42.82	42.95	42.26	44.65	43.11	42.63	41.59	45.54	46.80	45.28	41.86
En	44.87	46.30	59.15	51.33	50.13	47.95	49.65	53.49	50.07	48.27	50.34	47.98	49.18	51.05	49.33	46.93	42.61	45.80	48.29
Fs	8.57	11.77	7.70	6.23	8.31	8.80	4.94	8.91	7.11	8.78	7.40	7.37	7.71	6.32	9.08	7.53	10.59	8.91	9.85
Ti/Al	0.28	0.17	0.08	0.15	0.12	0.26	0.19	0.13	0.14	0.12	0.13	0.41	0.20	0.11	0.11	0.20	0.37	0.32	0.13
Cr*100/ (Cr+Al)	0.00	0.56	3.06	2.99	4.70	7.87	8.71	5.53	5.12	6.42	4.09	15.55	8.37	7.07	5.68	8.36	0.00	9.30	5.06

According to the Al^vi vs Al^iv diagram (Figure 4), these clinopyroxene crystals crystalized at high pressure near of the RMC (Refractory Mantle Clinopyroxene, [14] ) field.

4.2.3. Fe-Ti Oxides

The titano-magnetite is present in the host basalt (Table 3), with TiO₂ and FeO contents reaching respectively 25.0 wt% and 69.5 wt%.

4.2.4. Spinel

Spinel of wherlites (Al > Cr, Mg > Fe²⁺) is chromiferous with the values of Cr# (Cr × 100/(Cr + Al) and Fe²⁺/(Fe²⁺ + Mg) positively correlated (Table 4; Figure 4). The correlation trend displays on the Figure 4, present two distinct evolutions, one for the Adamawa Plateau (Nganha; [15] , Dibi; [3] ) and another for the Cameroon Volcanic Line (São Tomé; [16] , Mbarombi Mbo; [17] ), Mount Cameroon; [11] [18] and Kapsiki Plateau; [19] ). The distribution of the spinel compositions in Cr-Al-Fe³⁺ ternary diagram (Figure 5) both for Adamawa Plateau and the Cameroon Volcanic Line reflects the heterogeneous nature of the magmatic source. The Ti (0.44 - 0.52 a.p.f.u) and Fe²⁺ (3.15 - 3.59 a.p.f.u) contents are high and could be link to the re-equilibration during the crystallization of the clinopyroxene from the host basalt.

4.2.5. Plagioclase

The compositions of plagioclase (Table 5) from the host basalt range from bytownite (An₇₁Ab₂₈) to labradorite (An_61-69Ab_37-30).

5. Discussion5.1. Origin of Wehrlites

Ultramafic xenoliths are considered as fragments of lithospheric mantle [1] or the residues of the partial melting of mantle [20] .

Clinopyroxenes in the studied wehrlites are low in TiO₂ (0.8 - 1.7 wt%) and Al₂O₃ (1.8 - 5.1 wt% 3 - 4 wt%) as typical for clinopyroxenes of residual mantle origin [14] [13] . The refractory elements as Cr are enriched in the residue, as

Table 3 Representative compositions of Fe-Ti oxides of host basalt

sample nb.	132	132	132	132	132	132	132
SiO₂ (wt%)	0.00	0.00	0.05	0.03	0.13	1.01	0.07
TiO₂	24.63	24.66	25.03	24.56	19.60	19.59	17.83
Al₂O₃	2.64	2.85	2.35	2.02	2.41	1.51	5.68
Cr₂O₃	0.07	0.21	0.11	0.17	0.50	0.05	0.00
FeO	65.52	63.68	65.83	65.83	67.46	69.58	67.68
MnO	0.74	0.83	0.74	0.86	0.76	2.33	0.64
MgO	3.93	4.51	3.57	3.28	4.02	1.43	4.13
CaO	0.24	0.09	0.06	0.13	0.11	0.22	0.00
Total	97.77	96.84	97.72	96.87	95.18	96.08	96.19
Ilmenite basis
Fe₂O₃ (calc.)	36.69	35.85	36.11	36.37	41.49	40.88	41.21
FeO (calc.)	32.51	31.42	33.34	33.11	30.13	32.80	29.60
Total (calc.)	101.44	100.43	101.34	100.51	99.14	99.82	99.16
Ulvospinel basis
Fe₂O₃ (calc.)	20.27	19.41	19.39	19.98	28.31	26.93	29.93
FeO (calc.)	47.28	46.21	48.38	47.86	41.98	45.35	39.75
Total (calc.)	99.80	98.78	99.67	98.87	97.82	98.42	98.03
Si (apfu)	0.000	0.001	0.014	0.008	0.037	0.303	0.021
Ti	5.343	5.374	5.457	5.418	4.346	4.400	3.704
Al	0.898	0.973	0.803	0.698	0.836	0.531	1.960
Cr	0.017	0.049	0.025	0.039	0.117	0.011	0.000
Fe³⁺	4.399	4.231	4.231	4.411	6.281	6.051	6.591
Fe²⁺	11.402	11.194	11.729	11.739	10.350	11.327	9.728
Mn	0.180	0.204	0.180	0.212	0.190	0.590	0.159
Mg	1.689	1.947	1.542	1.434	1.766	0.638	1.800
Ca	0.073	0.028	0.020	0.041	0.034	0.069	0.000
Usp (%)	68.09	68.64	69.59	68.89	55.90	59.46	48.54

Table 4 Representative compositions of the spinel of the studied wehrlite

sample nb.	132-1	132-1	132-1
TiO₂ (wt%)	2.92	2.48	2.85
Al₂O₃	32.62	32.64	28.78
Cr₂O₃	14.90	14.26	16.15
FeO	33.62	35.77	39.57
MnO	0.32	0.23	0.50
MgO	14.11	13.65	10.84
CaO	0.01	0.00	0.06
Total	98.73	99.04	98.74
Fe₂O₃ (calc)	17.82	19.36	19.58
FeO (calc)	17.58	18.34	21.95
Total (calc)	100.52	100.98	100.7
Ti (apfu)	0.516	0.439	0.522
Al	9.042	9.044	8.259
Cr	2.771	2.651	3.109
Fe³⁺	3.154	3.426	3.588
Fe²⁺	3.458	3.607	4.471
Mn	0.063	0.046	0.102
Mg	4.949	4.786	3.934
Ca	0.003	0.000	0.015

Table 5 Representative compositions of the plagioclase of the host basalt

sample nb.	132	132	132	132	132	132
SiO₂ (wt%)	50.71	50.67	52.08	49.4	50.63	51.66
Al₂O₃	28.40	30.51	30.31	32.34	30.66	31.25
FeO	1.30	0.70	0.55	0.39	0.54	0.68
CaO	12.93	12.4	12.07	14.11	13.55	13.86
Na₂O	4.12	3.84	4.13	3.20	3.25	3.30
K₂O	0.66	0.34	0.34	0.15	0.25	0.24
Total	98.12	98.46	99.48	99.57	98.88	100.98
Si (apfu)	2.319	2.335	2.371	2.26	2.331	2.331
Al	1.531	1.657	1.626	1.744	1.664	1.661
Fe²⁺	0.000	0.027	0.021	0.015	0.021	0.026
Ca	0.634	0.612	0.589	0.691	0.668	0.670
Na	0.366	0.344	0.366	0.284	0.291	0.289
K	0.038	0.020	0.02	0.009	0.015	0.014
An (%)	64	64	61	71	69	69
Ab	32	34	37	28	30	30
Or	3	2	2	1	2	1

demonstrated for the Cr-rich clinopyroxene from the studied xenoliths. Thus, the studied spinel-bearing wehrlite xenoliths, characterized by the presence of Cr-diopside, represent probably the residual portions of the upper mantle [21] . The range of Ni contents (up to 1900 ppm) of olivine of wehrlites from the SW of Hosséré Dammougalré confirms that they are residues of melting. However, the compositions of olivine crystals which are characterized by the forsterite contents lower than 90%, may, have been modified by Fe-Mg equilibration between wehrlite olivine and the host basalt. Re-equilibration between Fe-Mg and host basalt at low temperatures is corroborated by slight similarity between wehrlite olivine Mg# (Fo76 - 88), NiO (0.04 - 0.19 wt.) and CaO (0.15 - 0.39) contents and olivine in host basalt Mg# (Fo68 - 74), NiO (0.04 - 0.16 wt%) and CaO (0.30 - 0.43). Thus, the occurrence of small plagioclase and oxides crystal surrounding the wehrlites indicates that olivine re-equilibration took place at low pressures (<0.2 GPa; [22] ).

5.2. Geothermometry and Geobarometry

Equilibrium temperatures calculated from Fe/Mg exchange reaction for olivine/ spinel using geothermometers [23] vary between 944˚C and 1102˚C. These temperatures are near of that estimated at liquidus above 1150˚ C after [24] for the crystallization of the Cr-spinel.

The CaO contents (0.15 - 0.39 wt%) of the studied wehrlite olivine are obviously higher than that of olivine of mantle origin (0.05% - 0.1%: [17] ), which involve low pressure (<0.2 GPa; [22] ) equilibrium environment, probably near the surface. However, as evidenced by the Al^vi vs Al^iv diagram (see Figure 6) all the analyzed wehrlite clinopyroxenes have crystalized at high pressures [13] near of the RMC (Refractory Mantle Clinopyroxene; [14] ) field. These contrasted results, would indicate that the wehrlite clinopyroxene would have been re-equilibrated in the host basalt at high pressures (shallow depths) during their as

cending towards the surface. As estimated for Ngao Voglar xenoliths [5] , which are situated in the same geological domain (Adamawa Plateau), the wehrlite xenoliths from the SW of Hosséré Dammougalré have likely been entrained by host basalt and carried up to the earth’s surface from the depth limit of 57 - 58 km.

6. Conclusion

Petrographical, mineral chemistry and thermobarometric data indicated that the wehrlite xenoliths from the SW of Hosséré Dammougalré are likely residual portions of the mantle partial melting, strongly re-equilibrated by the host melt which were extracted from shallow depths (~60 km) at temperatures estimated around 1100˚C.

Acknowledgements

The French “Ministère de la Coopération” is acknowledged for providing a grants to I.B.G.M. for nine-month stay in France at the “Laboratoire de magmatologie et de géochimie inorganique et expérimentale, Université Pierre-et-Marie-Curie”, Paris. Pr Bernard Déruelle is acknowledged for his assistance and his supervision during the laboratory-work at this university.

Cite this paper

Mbowou, I.B.G., Nguihdama, D., Yamgouot, F.N., Ntoumbe, M., Youpoungam, A.A. and Ngounouno, I. (2017) Mineral Chemistry of Wehrlite Xenoliths Hosted in Basalts from the SW of Hosséré Dammougalré (Adamawa Plateau, Cameroon): Thermobarometric Implications. Open Journal of Geology, 7, 1465-1477. https://doi.org/10.4236/ojg.2017.710098

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