Composition of Amphiboles from Toro Dioritic Complex, Northcentral Nigeria: A Potential Petrogenetic and Geothermobarometric Indicator
11Department of Marine Science and Technology, Federal University of Technology, Akure, Nigeria
2Department of Geology and Mining, University of Jos, Nigeria
The Toro symmetrical complex is localized within the Precambrian Basement Complex of the north central Nigeria. The complex is composed of three granites types surrounding an orthoenstantite dioritic core. Amphiboles samples from the diorite have higher Mg/ (Mg+Fe) values and are richer in Si, Ti and poorer in Al and Na+K than those in the granites. The calculated P-T results show that diorite crystallized at pressures between 4.7 kbar and 5.4 kbar and temperatures of 796°C to 821°C. The hornblende-biotite granite crystallized at pressures between 5.8 kbar to 8.5 kbar and temperatures between 633°C to 771°C. The average pressure (5.1 kbar ) for dioritic amphibole corresponds approximately to 19 km in depth of emplacement for the diorite and 24km in depth of emplacement for both hornblende-biotite (average pressure = 6.5 kbar) and porphyritic hornblende-biotite granites (average pressure = 6.4 kbar). Nature of dioritic amphibole evolution, coupled with its P-T suggests that the Toro diorite may have originated earlier with non consanguineous magma source different from the granites, which corresponds to a model of origin involving melting in the lower crust under granulite facies conditions.
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Keywords: amphibole composition, geothermobarometry, Toro diorite, northcentral Nigeria
Journal of Geosciences and Geomatics, 2013 1 (1),
Received December 29, 2012; Revised October 15, 2013; Accepted December 15, 2013Copyright: © 2013 Science and Education Publishing. All Rights Reserved.
Cite this article:
- Dada, O. A, and E. C Ashano. "Composition of Amphiboles from Toro Dioritic Complex, Northcentral Nigeria: A Potential Petrogenetic and Geothermobarometric Indicator." Journal of Geosciences and Geomatics 1.1 (2013): 41-46.
- Dada, O. A. , & Ashano, E. C. (2013). Composition of Amphiboles from Toro Dioritic Complex, Northcentral Nigeria: A Potential Petrogenetic and Geothermobarometric Indicator. Journal of Geosciences and Geomatics, 1(1), 41-46.
- Dada, O. A, and E. C Ashano. "Composition of Amphiboles from Toro Dioritic Complex, Northcentral Nigeria: A Potential Petrogenetic and Geothermobarometric Indicator." Journal of Geosciences and Geomatics 1, no. 1 (2013): 41-46.
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The Toro symmetrical complex is localized at the north east of Jos in north central Nigeria. It occupies a low hilly area above the surrounding plains within the Precambrian Basement Complex of Nigeria. The hornblende-biotite granite of Neil valley of the Jos-Bukuru ring complex truncated its southern end Figure 1.
The Toro Complex has been classified with the Charnockites of Nigeria by workers who studied the Complex from other perspectives. Geochronological studies of the Complex was carried out by [1, 2, 3] while the structural studies was done by . These studies link the emplacement of the charnockites and the “Older Granites” within the Nigerian basement migmatites to the waning phases of the Pan African thermo tectonic events. Borley  places the temperature of the formation of granites from the complex at between 600-900°C. Rahaman  from field studies of hybrid rocks is of opinion that either the granites and charnockites are contemporaneous or that the charnockites were emplaced shortly before the granites. Ashano et al.  postulates lack of consanguinity in magmatic sources of various rocks (diorites, dolerites and the granites) from the complex. They also confirmed crustal contamination of magmatic sources of the granites and very little contamination for the diorites.
In this study, we examined the chemistry of amphiboles in diorites and the granites (porphyritic hornblende-biotite and hornblende-biotite granites) from the Toro Complex, north central Nigeria, in order to throw more light on pressure and temperature, P-T condition of formation and its implications on the petrogenesis of the complex.
2. Geology of the Study Area
Ashano et al.  has described the geology of the study area. The Toro Complex is composed of three granite types surrounding an orthoenstatite dioritic core Figure 1. The complex is a symmetrical repletion of identical granite types on the two sides of the dioritic core, and the granites are discontinuous in many places. The rock types strike mainly in the north-south direction. The contacts between the rocks are sharp and dip almost vertically, and their age relationships are not quite certain, although the granites appear younger than diorites . Wright , Cooray  and Rahaman  considered the diorites to be older than the granites as dioritic xenoliths are of ubiquitous occurrences in the granites. According to , the identification and naming of the rocks of the Toro symmetrical complex by the previous workers was done mainly on relative textural characteristics.
The rocks forming the outer ring is a dark grey, fine-medium grained (locally porphyritic) biotite-muscovite granite (very rarely with any hornblende), which exhibits some degree of foliation. The central ring is a light grey, coarse grained, equigranular hornblende-biotite granite while the inner ring is medium-grained porphyritic hornblende granite with greyish colour Figure 1. The inner ring shows a sharp contact with the diorite, but marginal exposures against the diorite are dark and mottled due to contamination (granodioritic). The outer ring differs from the other granite types by the absence of hornblende and it is characterized by foliation which is parallel to its margin. This informs its classification as anatectic granite (granite gneiss in old literature). Its contact with the central granite is sharp, but where it abuts against the innermost granite in the northwestern portion of the complex, the degree of exposure precludes adequate evaluation of the relationship. The diorite outcrops in four main areas. It is typically equigranular, fine to medium grained and sometimes porphyritic. It is dark green in colour. The rock suites are discordantly cut at several places by dark grey to greenish, very fine to cryptocrystalline hyperbyssal doleritic rocks .
Dada et al.  suggested that the complex was formed by the initial intrusion of the medium-grained porphyritic granite (inner ring) whose outer sheared margin is now represented by outer ring. This is followed by the subsequent intrusion of the coarse grained equigranular granite between the outer sheared portion and the inner more massive portion. The process is seen as melting of lower crustal material during the Pan African thermo tectonic events, leading to the withdrawal of essentially silicic potassium liquids .
3. Analytical Methods
Fresh surface samples of diorite, porphyritic hornblende-biotite and hornblende-biotite granites were analysed, using a Camebax Electron Microprobe at the Clermont Ferrad University, France. The analytical conditions were 15KV high voltage with a current of 11 Na and a counting time limit of 10 seconds. Absolute error is estimated to be 2%, and the analyses were made on amphiboles present in the rocks. Representative and average microprobe analyses of amphiboles from hornblende-biotite and porphyritic hornblende-biotite granites are given in Table 1, Table 2 and Table 3. Structural formulae of the phases were computed and the rather large data summarized in the various plots displayed in Figure 2, Figure 3, Figure 4.
4. Results and Discussion4.1. Amphibole Chemistry
Amphiboles in Toro complex granitoids vary widely in composition (Table 1, Table 2, Table 3; Figure 2, Figure 3, Figure 4; Leake et al. ). Amphibole in the Toro diorite contains ferro edenite, ferro hornblende, magnesiohornblende and ferrotschermakite. The hornblende-biotite granite have amphibole ranging between hastingsite and ferrotschermakite while porphyritic hornblende-biotite granite amphibole contains crystal zoned between hastingsite and ferropargasite.
The amphiboles from diorite are chemically distinct from other rocks, going by their chemical compositions Table 1, Table 2, Table 3. In the diorite samples, the amphibole grains have the following average compositional range per formula unit (pfu): Si = 6.429-6.669, Al = 1.612-1.772, Ca = 1.734-1.859, (Na+K) = 0.133-0.593 and mg# = [Mg/(Mg+Fe)] = 0.423-0.510; in the hornblende-biotite granite sample, the values are Si = 5.979-6.371, Al = 1.847-2.419, Ca = 1.831-1.932, (Na+K) = 0.303-0.914 and mg# = [Mg/(Mg+Fe)] = 0.224-0.284. The porphyritic hornblende-biotite granite amphibole compositions are Si = 6.301-6.452, Al = 1.903-2.038, Ca = 1.866-1.941, (Na+K) = 0.619-0.794 and mg# = [Mg/(Mg+Fe)] = 0.218-0.272.
Toro diorite is poorer in Al and Na+K but richer in Si, Ti and higher in Mg/Mg+Fe than the hornblende-biotite and porphyritic hornblende-biotite granites. This suggests that diorite crystallizes from magma of higher silica activity and lower alkali contents. In the same vein, amphibole from hornblende-biotite granite shows low Si and Ca contents, and high Al, Na+K and #mg values compared with the porphyritic type.
4.1.1. Amphibole Geobarothermometry
Previous studies on parageneses of calacic amphiboles in mafic igneous rocks by [11-18] made it clear that, with increasing P-T conditions, calcic-amphiboles exhibit increases in (Mg/Mg+Fe) and in K, Al, Na and Ti contents and commensurate decreases in Si and total Fe+Mg+Mn+Ca. It has also been claimed that the total Al in hornblende may be used as a barometer in granitic rocks (), and four calibrations have been proposed ([20, 21, 22, 23]).
Determined pressures for this study are: diorite varies from 4.7 Kbar to 5.4 Kbar, hornblende-biotite granite ranges from 5.8 Kbar to 8.5 Kbar and porphyritic hornblende-biotite granite varies from 6.1 Kbar to 6.7 Kbar Table 4. The average pressures are 5.1 Kbar for diorite, 6.4 Kbar for hornblende-biotite granite and 6.4 Kbar for porphyritic hornblende-biotite Table 4.
Electron microprobe data for the amphiboles from diorite (DI), hornblende-biotite (HB) granite and porphyritic hornblende-biotite (pHB) granite from Toro Complex were used to determine temperature of formation using temperature calibration based on Ti content in hornblende by . This is best used to determine magmatic versus secondary compositions. Temperature of formation estimates for diorite vary from 796°C to 821°C, 633°C to 771°C for hornblende-biotite (HB) granite and 714°C to 779°C for porphyritic hornblende-biotite (pHB) granite. The average temperature got from amphiboles for the diorite is 789°C; 728°C for hornblende-biotite (HB) granite and 750°C for porphyritic hornblende-biotite (pHB) granite.
Table 4. Results of geobarometry, Amph-Al (Total) of diorites (DI), hornblende-biotite (HB) granite and porphyritic hornblende-biotite (pHB) granite from Toro complex, north central Nigeria. The table shows Pressure Calculations using Hammarstrom and Zen , Hollister et al.( and Schmidt 
The Toro dioritic complex amphiboles represent a wide compositional range. The dioritic amphiboles contain ferroedenite, ferrohornblende, magnesiohornblende and ferrotschermakite members. The hornblende-biotite granite amphiboles range from hastingsites to ferrotschermakite while the porphyritic type clusters between hastingsite and ferropargasite, as shown in the Mg/ (Mg+Fe2+) versus Si diagram (Figure 2; after Leake et al. ). All the amphiboles plot in the igneous field of Ca+Na+K versus Si diagram (Figure 3; Giret et al. ) and are calcic amphiboles Figure 4. This implies that the amphiboles are igneous in origin and must have formed from the intrusion of magma probably derived from the upper mantle into the pre-existing older rocks as suggested by 
Table 5. Calculated temperature using amphibole population in diorite, hornblende-biotite (HB) granite and porphyritic hornblende-biotite (pHB) granite from Toro complex, north-central Nigeria (Ti-Hbd geothermometer of Otten )
Looking at the chemical compositions of amphiboles in the studied rocks, it can be deduced that the diorite crystallized from a different magma. Though the hornblende-biotite and porphyritic hornblende-biotite granites may have had a more direct relationship, going by the slight variation in their amphibole compositions, they grew at different stages of crystallization. If these magmas once had a common parentage, they evolved independently due to different magmatic conditions where mafic minerals subsequently crystallized with unique “finger prints”.
The calculated P-T results show that the diorite crystallized at pressures between 4.7 kbar and 5.4 kbar and temperatures of 796°C to 821°C. The bornblende-biotite granite crystallized at pressures between 5.8 kbar to 8.5 kbar and temperatures between 633°C to 771°C while the porphyritic hornblende-biotite granite crystallized at pressures between 6.1 kbar to 6.7 kbar and temperatures between 714°C to 779°C. The values shown in Table 4 and Table 5 are within the range given by . Borley  stated that the temperatures of formation of the granites of the Toro complex are between 600°C and 900°C. The average pressure (5.1 kbar ) for diorite amphibole corresponds approximately to 19 km in depth of emplacement for diorite and 24km in depth of emplacement for both hornblende-biotite (average pressure = 6.5 kbar) and porphyritic hornblende-biotite granites (average pressure = 6.4 kbar). The present chemical and P-T studies on the amphiboles of the Toro dioritic complex confirms that diorite is the earliest formed rock ([6, 8, 9]) and has non consanguineous magma source with the granites ([2, 7]). This corresponds to a model of origin involving melting in the lower crust under granulite facies conditions of medium pressure and higher temperature.
Following the amphibole characteristics displayed by the diorite and granites from the Toro dioritic complex and the discussions, it can be inferred that the diorite from the complex formed earlier than the granites and its magma source has no consanguinity with the granites from the same complex.
|||Tubosun I. A, Lancelot J. R, Rahaman M. A. and Ocan O. (1984). U-Pb Pan African ages of two charnockite- granite association from SW Nigeria. Contribution to Mineralogy and Petrology, 88, pp. 188-195.|
|||Dada S.S. Lancelot J. R. and Briqueu L. (1989). “Age and origin of the annular charnockitic complex at Toro, Northern Nigeria: U-Pb and Rb-Sr evidence”. Journal of African Earth Sciences, Vol. 9, Issue 2, pp 227-234.|
|||Dada S. S, Tunbosun I. A, Lancelot J. R and Lar U. A. (1993). Late Archean U-Pb age for reactivated basement of Northern Nigeria. Journal of African Earth Sciences 16, (4), pp. 405-412.|
|||Annor A. E and Freeth, S. J. (1985). Thermotectonic evolution of the basement complex around Okenne, Nigeria with special reference to deformation mechanism. Precambrian Research, 28, pp. 269-281.|
|||Borley G. D. (1976). Ferromagnesian mineralogy and the temperature of formation of the Younger Granites of Nigeria. In Kogbe, C. A., Geology of Nigeria. Elizabethan Publishing Company Lagos, pp. 159-176.|
|||Rahaman M.A. (1988). Recent advances in the study of the Precambrian of Nigeria. 1st Symposium on Pre-Cambrian Geology of Nigeria Proceedings, Kaduna. Special Publication of Geological Survey of Nigeria.|
|||Ashano E. C, Obasi C. K, Agada I. S. (2010). Crystallochemical study and petrogenesis of the Toro Dioritic Complex, northcentral, Nigeria. Journal of Mining ang Geology, 46 (1), pp. 33-48.|
|||Wright E.P. (1971). Basement Complex. In Geology of the Jos Plateau. Bulletin, Geological Survey of Nigeria, 32 (1), 619 p.|
|||Cooray P. G. (1975). The charnockitic rocks of Nigeria. In studies in Precambrian, 50-73.|
|||Leake B.E., Woolley A.R., Arps C.E.S., Birch W.D., Gilbert M.C., Grice J.D., Hawthorne F.C., Kato A., Kisch H.J., Krivovichev V.G., Linthout K., Laird J., Mandarino J., Maresch W.V., Nickel E.H., Rock N.M.S., Schumacher J.C., Smith D.C., Stephenson N.C.N., Ungaretti L., Whittaker E.J.W. and Youzhi G. (1997). Nomenclature of amphiboles: Report of the subcommittee on amphiboles of the International Mineralogical Association Commission on New Minerals and Mineral Names". Canadian Mineralogy, 35: 219-246.|
|||Spear F. S. (1981). An experimental study of hornblende stability and compositional variability in amphibolite. American Journal of Science, 281, 697.734.|
|||Rutter M. J. (1989). Experimental data for a proposed empirical igneous geobarometer: Aluminium in hornblende at 10 kbar pressure. Geology, 17, 897-900.|
|||Mader U. K and Berman R.G. (1992). Amphibole thermobarometry, a thermodynamic approach, Current Research, Part E, Geological Survey of Canada Paper 92-1 E, 393-400.|
|||Ague J. J. and Brandon M. T. (1992). Tilt and northward offset of Cordilleran batholiths resolved using igneous barometry. Nature, 360, 146-149.|
|||Ague J. J. (1997). Thermodynamic calculation of emplacement pressures for batholitic rocks, California: implications for the aluminum-in-hornblende barometer. Geology, 25, 563-566.|
|||Ernst W. G. And Liu J. (1998). Experimental phase-equilibrium study of Al- and Ti- Contents of calcic amphibole in MORB-A semi-quantitative thermobarometer. American Mineralogist, 83, 952-969.|
|||Tuloch, A. J. and Challis G. A. (2000). Emplacement depths of Palezoic-Mesozoic plutons from western New Zealand estimated by hornblende-Al geobarometry. New Zealand Journal of Geology and Geophysics, 43, 555-567.|
|||Daif Menana and Arafa Ahmed (2007). Mineralogy and Geochemistry of Neogene Andesites from Annaba’s Area (North east Algeria) - Calcic Amphibole Thermobarometry. Medwell Online Journal of Earth Sciences 1 (2):101-107.|
|||Kutsukake T. (1997). The depth of emplacement of the Mitsuhashi Granite pluton in the Ryoke Belt, central Japan- as inferred from some geobarometric calibrations. Journal of Geological Society of Japan, 103 (6), pp. 604-607.|
|||Hammarstrom J. M and Zen E. (1986). Aluminum in hornblende: An empirical igneous geobarometer. American Mineralogy, 71: 1297-1313.|
|||Hollister L. S., Grissom G. C., Peters E. K., Stowell H.H. and Sisson V. B. (1987). Confirmation of the empirical correlation of Al in hornblende with pressure of solidification of calc-alkaline plutons. American Mineralogy, 72: 231-239.|
|||Johnson M. C. and Rutherford M. J. (1988). Experimental calibration of an Aluminium-in-hornblende geobarometer applicable to calc-alkaline rocks. EOS, 69, 1511.|
|||Schmidt M. W. (1992). Amphibole composition in tonalite as a function of pressure: An experimental calibration of the Al-in-hornblende barometer. Contrib Mineral Petrol, 110: 304-310.|
|||Otten M. T. (1984). The origin of brown hornblende in Artfjallet gabbro and dolerites. Contribution to Mineralogy and Petrology. 86, 189-199.|
|||Giret A., Bonin B. and Léger J. M. (1980). Amphibole compositional trends in oversaturated and undersaturated alkaline plutonic ring complexes. Canadian Mineralogist, 18, 481-495.|