Historiography – low Ti basalts – boninites – draft 3
1959-1979
Wilson, R.A.M. 1959. The geology of the Xeros-Troodos area. Memoir, Cyprus Geological Survey Dept., 1,
184 p.
Dallwitz, W.B., Green, D.H., and Thompson, J.E. 1966. Clinoenstatite in a volcanic rocks from the Cape Vogel
area, Papua. Jour. Petrol., 7, p. 375-403
Gass, I.G. 1968. Is the Troodos Massif of Cyprus a fragment of Mesozoic Ocean Floor ? Nature, 220, p.
39-42.
Vine, F.J. and Moores, E.M. 1969. Paleomagnetic results for the Troodos igneous massif, Cyprus. EOS
(American Geophysical Union Transactions), 50, p. 131.
Searle, D.L. and Vokes, F.M. 1969. Layered ultrabasic lavas from Cyprus. Geol. Mag., 106, p.515-530
Moores, E.M. and Vine, F.J. 1971. The Troodos Massif, Cyprus, and other ophiolites as oceanic crust:
evaluation and implications. Philos. Trans. R. Soc. London, Ser. A, 268, p. 443-466.
Nicholas, A. and Jackson, E.D. 1972. Repartition en deux provinces des peridotites des Chaines alpines
logeant la Mediterranee: implications geotectoniques. Schweiz miner. Petrogr. V. 52, 3, p. 479-495.
Griffiths, J.R. and Varne,R. 1972. Evolution of the Tasman Sea, Macquarie Ridge and Alpine Fault. Nature
Phys. Sci., 235, p. 83-86.
Gass, I.G. and Smewing, J.D. 1973, Intrusion, extrusion and metamorphism at constrictive margins: evidence
from the Troodos Massif, Cyprus. Nature, 242, p. 26-29. Off axis volcanism
Miyashiro, A. 1973. The Troodos ophiolitic complex was probably formed in an island arc. EPSL, 19, p. 218224.
Gale, G.H. 1973. Paleozoic basaltic komatiite and ocean-floor type basalts from northeastern Newfoundland.
EPSL. 18, p. 22-28.
Basic pillow lavas from northeastern Newfoundland are shown to be chemically similar to basaltic komatiites
and ocean-floor basalts. New trace element data presented for basaltic komatiites indicate that they were
derived from a magma more primitive than that producing ocean-floor basalts. A model for the derivation of
basaltic komatiite by extensive partial melting of pyrolitic upper mantle at sites of plate separation is
proposed.
Parrot, J.F. 1974. L’assemblage ophiolitique du Baer Bassit (Nord Ouest de la Syrie): etudie petrographique et
geochimique du complexe filonien, des laves en coussins qui lui sont associees, et d’une partie des formations
effusive du volcano sedimentaire. Cahier ORSTOM, Ser. Geol. VI, p. 97-126.
Smewing, J.D., Simonian, K.O., and Gass, I.G. 1975. Metabasalts from the Troodos massif, Cyprus : genetic
implications deduced from petrography and trace element geochemistry. Cont. Min. Petr., 51 p. 49-64.
Pearce, J.A. 1975. Basalt geochemistry used to investigate post-tectonic environments on Cyprus.
Tectonophysics, 25, p. 41-67.
Rocci, G., Ohnenstetter, D, and Ohnenstetter, M. 1975. La dualite des ophiolites tethysiennes
Petrologie, 1, p. 172-174.
Robertson, A.H.F. 1975. Cyprus umbers : basalt -sediment relationship on a Mesozoic ocean ridge. Jour.
Geol. Soc., v. 131, p. 511-531.
Norman, R.E. and Strong, D.F. 1975. The geology and geochemistry of ophiolitic rocks exposed at Mings
Bight, Newfoundland. CJES, 12, p. 777-797. Analyses used in Church and Coish 1976.
Miyashiro, A. and Shido, F. 1975. Tholeiitic and calc-alkaline series in relation to the behaviours of titanium,
vanadium, chromium, and nickel. Am. J. Sci., 275, p. 265-277.
Hynes, A 1975. Comment on “The Troodos ophiolitic complex was probably formed in an island arc” by A.
Miyashiro, EPSL, 25, p. 213-216.
Moores, E.M. 1975. Discussion of “Origin of Troodos and other ophiolites: a reply to Hynes” by A. Miyashiro,
EPSL, 25, p. 223-226
Miyashiro, A. 1975. Origin of Troodos and other ophiolites: a reply to Moores. EPSL, 25, p. 227-235.
Gass, I.G. et al. 1975. Comment on “The Troodos ophiolitic complex was probably formed in an island arc” by
A. Miyashiro, and subsequent correspondance by A. Hynes and A. Miyashiro. EPSL, 25, p. 236-238.
Hodges, F.N. and Papike, J.J. 1975. Deep-seated rocks recovered by DSDP Leg 37: pyroxene chemistry and
cooling history, Geol. Soc. Am. NE Sect, 10th Ann. Meet, Abst. W. Programs, 7, p. 74-75.
Church, W.R. and Coish, R.A. 1976. Oceanic versus Island Arc origin of Ophiolites. EPSL 31, p. 8-14. Sub
Dec 15 1975
“The use of titanium as a discriminant of tectonic environmentis also suspect because the titanium content of
basalts associated with Appalachian ophiolites as well as those recently recovered from the Atlantic ocean
floor ranges from the Atlantic ocean floor ranges from values even lower than those typical of island arc
tholeiites to values typical of abyssal tholeiites.”
“Miyashiro suggests that the plutonic components of ophiolites such as Troodos and Betts cove might have
formed in magma chambers located beneath volcanic complexes of oceanic island arcs.” “Miyashiro appears
to be aware of this difficulty since he comments with reference to the Troodos ophiolite that “no evidence has
been found on the origin of the underlying ultramafic rocks”, a statement which is clearly meant to contest the
interpretation of the Troodos and Vourinas harzburgite tectonites as mantle rocks.”
“the internal stratigraphy of ophiolites in both the Appalachian and Tethyan systems can only be explained on
the basis of the postulate that ophiolites originate at oceanic spreading centres rather than beneath island
arcs.”
Delaune-Mayere, M. and Parrot, J-F. 1976. Evolution de la marge continentale meridionale du Bassin
Tethysien oriental d'apres l'etude des series sedimentaires de la region opiolitique du NW Syrien.
Cah.ORSTOM., ser. Geol., v. 8, no.2, p. 173-183
Ohnenstetter, D. and Ohnenstetter, M. 1976. Modele de fonctionnement d’une ride medio-oceanique a partir
de l’etude petrologique des ophiolites corses. Bull. Geol. Soc. France v. 18, p. 889-894.
Kay, R.W. and Senechal, R.G. 1976. The rare-earth geochemistry of the Troodos ophiolite complex. J. Geoph.
Res, 81, p. 964-970.
Smewing, J.D. and Potts, P.J. 1976. Rare Earth abundances in basalts and metabasalts from the Troodos
Massif, Cyprus. Cont. Min. Pet. , 57, p. 245-258.
Fryer, B.J. and Hutchinson, R.W. 1976. Generation of metal deposits on the sea floor. CJES, 13, p. 126-135.
Robertson, A.H.F. and Fleet, A.J. 1976. The origins of rare earths in metalliferous sediments of the Troodos
Massif, Cyprus. Earth Plan. Sci. Letters, 28, p. 385-394.
Robertson, A.H.F. 1976. Origins of ochres and umbers : evidence from Skouriotissa, Troodos massif, Cyprus.
Trans. Sect. B, Inst. Min. Metal., v. 85, p. 245-251.
Church, W.R. 1977. The ophiolites of southern Quebec: oceanic crust of Betts Cove type. CJES, 14, p. 16681673. Sub Dec 19 1975; Acc Jan 12 1977
Delaune-Mayere, M., Marcoux, J., Parrot, J-F., and Poisson, A.1977. p.79-94 in International Symposium on
the Structural History of the Mediterranean Basins, Biju Duval, B. and Montadert, L. (eds), Editions Technip,
Paris
Cleintuar, M.R., Knox, G.J., and Ealey, P.J. 1977. The geology of Cyprus and its place in the East
Mediterranean framework. Geol. en Mijnbouw, 56, p. 66-82
Desmet, A., 1977. Les pillow laves du Troodos (C type), Universite de Nancy; These, p. 110-132.
Smewing, J.D., Simonian, K.O., Elboushi, I.M., and Gass, I.G.1977. Mineralized fault zone parallel to the
Oman ophiolite spreading axis. Geology, 5, Sept., p. 534-538.
Robertson., A.H.F. 1977. Kannaviou Formation of Cyprus.; Jour. Geol. Soc., 134, p.269
Robertson. A.H.F. 1977. The Moni melange, Cyprus. Jour.Geol. Soc, 133, p. 447-466.
Auden verus Robertson. 1978. Moni melange of Cyprus, Troodos. JGS 135, p.349
Coish, R.A. 1977a. Ocean floor metamorphism in the Betts Cove ophiolite, Newfoundland. Contr. Min. Pet.,
60, p. 255-270. Fe3+ versus Al3+ in epidote
Coish, R.A. 1977b. Igneous and metamorphic petrology of the mafic units of the Betts Cove and Blow Me
Down ophiolites, Newfoundland. University of Western Ontario, unpub. Ph.D. p. 119-124.
Church, W.R. 1977. The ophiolite of southern Quebec: oceanic crust of Betts Cove type. Can. J. Earth Sci.,
14, p. 1668-1673. Comment on the dual nature of the Tethyan ophiolites (Rocci et al, 1975).
Anonymous, 1977. Initial report of the geological study of oceanic crust of the Philippine Sea Floor. Ofioliti, 2,
p. 137-168.
Panayiotou, A. 1977. Geology and geochemistry of the Limassol Forest plutonic complex and the associated
Co-Ni-Co-Fe sulphide and chromite deposits, Cyprus. Ph. D. thesis, Univ. of New Brunswick, Canada.
1978 Feb 8th letter to Bob Nesbitt
1978 April, draft of Sun, S-S and Nesbitt, R.W. Geochemical regularities and genetic significance of ophiolitic
basalts. Geology
1978 April, submitted copy of Sun, S-S and Nesbitt, R.W. Geochemical regularities and genetic significance of
ophiolitic basalts. Geology. Shows concave REE pattern for sample 482/12 from the Mariana Trench “it is
suggested that they may be similar to low-Ti ophiolitic basalts. ……..in some cases the depleted mantle
sourece has been added to by a second component rich in light rare earth elements (LREE). ……….High
magnesium low-Ti basalts from the juxtaposed Internal Zone (e.g. Betts Cove) are believed to be products of
wet melting of a residual mantle at an inter-arc basin or island arc site after extraction of MOR type (e.g.
External zone) magma.”
1978 May 24 letter to Bob Nesbitt
1978 Spring Coish, R.A. and Church, W.R. 1978. The Betts Cove ophiolite, Newfoundland: some unusual
chemical characteristics. AGU Spring Meeting.
“The Betts Cove ophiolites are severely depleted in TiO2 (0.10 – 0.42 wt %) ……..20-30% melting of a
severely depleted lherzolite can produce a Betts Cove basalt.”
1978 May 8 letter from Ray Coish “I’m not sure that the U-shaped REE pattern is real, i.e. it may be
metasomatic…at AGU …I said that the LREE were enriched by metasomatism”
1978 July 31 letter to Ray. “Could the bastite replaced crystals be clinoenstatite”
Coish, R.A. and Church, W.R. 1978. The Betts Cove ophiolite, Newfoundland: some unusual chemical
characteristics. Transactions American Geophysical Union, 59, p. 408.
Upadhyay, H.D. 1978 Phanerozoic Peridotitic and Pyroxenitic Komatiites from Newfoundland. Science, 202, p.
1192-1195.
Panayiotou, A. 1978. The mineralogy and chemistry of the podiform chromite deposits in the serpentinites of
the Limassol Forest, Cyprus. Mineralium Deposita, 13(2), p. 259-274
George, R.P., Jr. 1978. Structural petrology of the Olympus ultramafic complex in the Troodos ophiolite,
Cyprus. Geol. Soc America Bull., 89, p.845-865.
Simonian, K.O. and Gass, I.G.1978. Arakapas fault belt, Cyprus : a fossil transform fault. Geol. Soc. America
Bull., 89, p.1220-1230.
Varne, R. and Brown, A.V. 1978 The geology and petrology of the Adamsfield ultramafic complex, Tasmania.
Contrib. Mineral. Petrol. 67.
Varne, R. and Brown, A.V. 1978 The geology and petrology of the Adamsfield Ultramafic complex, Tasmania.
Cont. Min. Petrol., v. 67, p. 195-207. Adamsfield ultramafic complex is opx bearing and low TiO2. No gabbro,
dolerite, or volcanic rocks. Overlain by serpentinitic sediments of Late Dresbachian - early Franconian age.
Sun, S.S. and Nesbitt, R.W. 1978 Geochemical regularities and genetic significance of ophiolitic basalts.
Geology, 6, p. 689-693
Zonenshain, L.P. and Kuzmin, M.I. 1978 The Khan-Taishir ophiolitic complex of Western Mongolia, its
petrology, origin and comparison with other ophiolitic complexes. Contrib. Mineral. Petrol. 67, p. 95-109.
Meijer, A. 1978 Petrology of volcanic rocks from the Mariana arc-trench gap and gabbros from the Mariana
inter-arc basin, IPOD Leg 60. Abst. Am. Geophys. Union, Tectonophysics, p. 1182
Dietrich, V.,Emmermann, R., Oberhansli, R., and 1978 Geochemistry of Basaltic and Gabbroic rocks from the
West Mariana Basin and the Mariana Trench. Earth Planetary Sci. Letters, 39, p. 127-144
1979 March 14 letter from Ray “…samples NH-71-1, NH-71-2, I do have REE analyses and the patterns are
enclosed. ….they have very exagerated U-shaped patterns with a possible Eu anomaly….this makes these
trondhjemites good candidates for differentiated liquids of the low-TiO2 basalts. I’ve done three trondhjemites
from Blow Me Down and their REE patterns are nearly float (40-60x chondrite) with an Eu anomaly which
becomes bigger with increasing SiO2 content…………….I’ve redone some of the upper lavas (high TiO2) that
George did. …………..I’ve also checked the low-TiO2 rock (analysys 10, 5260) done at Ross Taylor’s lab and
get very good agreement…………I have 7 or 8 low-TiO2 rocks done and they all have U-shaped REE
patterns. The intermediate TiO2 rocks, on the other hand, still have the LREE-depleted pattern.
Coish, R.A. and Church, W.R. 1979. Igneous geochemistry of mafic rocks in the Betts Cove ophiolite,
Newfoundland. Contr. Min Pet., 70, p. 29-39. Acc June 20 179 Refers to the U-shaped pattern in sample 10;
analyzed by George Jenner at ANU; other REE done by Ray at MIT
Chotin, P., et al. 1979 Le systeme d'arc insulaire des Mariannes: resultats du Leg 59, DSDP. Bull. Soc. Geol.
France, 21, p. 525-528
Upadhyay, H.D. and Neale, E.R.W. 1979 On the tectonic regimes of ophiolite genesis. Earth Planetary Sc.
Letters, 43, p. 93-102
Cameron, E.W., Nisbet, E.G., and Dietrich, V.J. 1979 Boninites, komatiites, and ophiolitic basalts. Nature 280,
p.550-553.
Wood, D.A. 1979. Dynamic partial melting: its application to the petrogenesis of basalt lava series from
Iceland, the Faero Islands, the Isle of Skye (Scotland), and the Troodos Massif (Cyprus). Geochim.
Cosmochim. Acta, 43, p. 1031-1046.
Bryan, W.B. 1979 Regional variation and petrogenesis of basaltic glasses from the FAMOUS area, MidAtlantic Ridge, Jour. Petrology 20, p. 293-325
Robertson, A.H.F. and Woodcock, N.H. 1979. The Mamonia Complex, southwest Cyprus; the evolution and
emplacement of a Mesozoic continental margin. Geol. Soc. of America Bull., 90 p. 651-665
1980 - 1989
Meijer, A. (1980): Primitive arc volcanism and a boninite series: example from W-Pacific Island arcs. In: D. F.
Hayes (ed.): The Tectonic and Geologic Evolution of southeast Asian seas and islands. AGU Monographs,
23: p. 269-282.
Hickey, R., Frey, F.A., Jenner, G., 1980. Trace element and isotopic characteristics of Boninites: implications
for their source. EOS, 61, 46, p. 1140.
“Recent projects along the Mariana arc recovered “boninite”-like lava which vary in MgO and SiO2 content,
and a “boninite series” of island arc lavas has been proposed (Meijer, 1980)………..the “boninite” source
component responsible for their varibale LREE enrichment and low Ti/Zr ratio is not dervied from subducted
MOR basalt, but is of continental or oceanic island affinity.”
1980 Nov 11 Upadhyay, H.D. 1980. On the boninite-komatiite connection: some observations from Betts Cove
and Belingwe. EOS, 61, 46, p. 1140. “some komatiites evolve into a calc-alkaline series (e.g. Betts Cove)
forming a continuous komatiite – boninite –“andesite” suite.”
Cameron, E.W. 1980 Petrographic dissimilarities between ophiolite and ocean floor basalts, in Panayiotou, A.,
ed., Ophiolites: Proceedings, International Ophiolite Symposium, Cyprus, p. 182-192
Wood, C.P. 1980 Boninite at a continental margin. Nature 288,no. 5792, p. 692-694
Shiraki, K., Kuroda, N., Uranno, H. and Maruyama, S. 1980 Clinoenstatite in boninites from the Bonin Islands,
Japan. Nature, 285, p. 31-32
Ohashi, F. and Shiraki, K. 1980 High-magnesia and high-silica volcanic rock in the Setogawa ophiolite, Central
Japan. J. Japan Assoc. Min. Petrol. Econ. Geol. , p.193
O, H. and Maruyama, S. 1980 Clinoenstatite in boninites from the Bonin Islands, Japan. Nature, 285, p. 31-32
Frey, F.A., Dickey, J.S., Thompson, G., Bryan, W.B. 1980 Evidence for heterogeneous primary MORB and
mantle sources, N.W. Indian Ocean. Contrib. Mineral. Petrol., 74, p. 387-402
Duncan, R.A. and Green, D. H. 1980 Geology, v. 8. p. 22-26
Searle, D. L. and Panayiotou, A.. 1980. Structural implications in the evolution of the Troodos Masif, Cyprus.
Proceedings Inter. Ophio. Sym., Nicosia, 50-60.
Swarbrick, R.E. 1980. The Mamonia Complex of SW Cyprus:a Mesozoic continental margin and its
relationship with the Troodos Complex.Proceedings of the International Ophiolite Symposium, Cyprus] p[86-92
Swarbrick, R.E. and Robertson, A.H.F. 1980. Revised stratigraphy of the Mesozoic rocks of southern Cyprus.
Geol. Mag. 117,6, p.547-563.
Laurent, R., Delaloye, M., Vuagnat, M. and Wagner, J. J. 1980. Composition of parental basaltic magnesian
ophiolites, Cyprus Geol. Sur. Dept., from Ophiolites proceedings Inter. Ophiolite Symposium Cyprus, p.
172-182.
Leblanc, M., Dupuy, C., Cassard, D., Moutte, J., Nicolas, A., Prinzhofer, A., and Robinovitch, M. 1980. Essai
sur la genese des corps podiformes de chromitite dans les peridotites ophiolitiques : etude des chromites de
Nouvelle-Caledonie et comparaison avec celles de Mediterranee oriental. Proc. Int. Ophiolite Symposium,
Nicosia, Cyprus.
1981
Tatsumi, Y. 1981 Melting experiments on a high-magnesian andesite. Earth Planet. Sci. Letters, 54, p. 357365.
Jenner, G.A. 1981 Geochemistry of high-Mg andesites from Cape Vogel, Papua New guinea. Chem. Jour. v.
33, p. 307-332.
Pearce, J.A., Alabaster, T., Shelton, A.W. and 1981 The Oman ophiolite as a Cretaceous arc-basin complex:
evidence and implications. Phil. Trans, R. Soc. Lond. A 300,.
Capedri, S. 1981 Petrology of an ophiolitic cumulate sequence from Pindos, Greece. Ofioliti, 6, p. 295
Crawford, Anthony J., Beccaluva, V., and Serri, 1981 Tectono-magmatic evolution of the West PhilippineMariana region and the origin of boninites. Earth and Planetary Sci. Letters, 54, p. 346-356
Serri, G. 1981 The petrochemistry of ophiolitic gabbroic complexes : a key for the classification of ophiolites
into low-Ti and high-Ti types. Earth Planetary Sci. Letters, 52, p. 203-212
Ohashi,F. and Shiraki,K. 1981 High magnesia and high silica volcanic rock in the Setogawa ophiolite. Jour.
Jap.Assoc. Min. Pet. Econ. Geol., 76, p. 69-79. (boninite?)
Capedri, S., Venturelli, G. and Bebien, J. 1981 "Low-Ti" and "high-Ti" ophiolites in northern Pindos:
petrological and geological constraints. Ofioliti, 6, p. 2296
Noiret, G., Montigny, R. and Allegre, C.J. 1981 Is the Vourinos complex an islaand arc ophiolite ? Earth and
Planetary Sci. Letters, 56, p. 375-386.
Spray, J.G. 1981. Evidence for upper Cretaceous transform fault metamorphism in West Cyprus. Earth and
Planetary Sci. Letters, 55, p. 273-291.
Dietrich. V.J., Gansser, A., Sommerauer, J. and 1981 Paleogene komatiites from Gorgona Island, east PacificA primary magma for ocean floor basalts? Geochemical Jour., 15,. 1981. p. 141-161
Ohashi,F. and Shiraki,K. 1981 High magnesia and high silica volcanic rock in the Setogawa ophiolite. Jour.
Jap. Assoc. Min. Pet. Econ. Geol., 76, p. 69-79. (boninite?)
Capedri, S., Venturelli, G., Bocchi, G., Dostal, J., 1981 The geochemistry and petrogenesis of an ophiolitic
sequence from Pindos, Greece. Contrib. Mineral. Petrol., 74, p. 1789-200.
Gale, N.H., Spooner, E.T.C., and Potts P.J. 1981. The lead and strontium isotope geochemistry of
metalliferous sediments associated with Upper Cretaceous ophilitic rocks in Cyprus, Syria, and the Sultanate
of Oman. Canadian Jour. Earth Sci., 18, p. 126.
Searle, M.P. and Malpas, J. 1981. Structure and metamorphism of rocks beneath the Semail ophiolite of
Oman and their significance in ophiolite obduction. Transactions of the Royal Soc. of Edinburgh: Earth Sci.,
71, p. 247-262.
Noiret, G., Montigny, R. and Allegre, C.J. 1981. Is the Vourinos complex an island arc ophiolite ? Earth and
Planetary Sci.Letters, 56, p. 375-386.
Serri, G. 1981. The petrochemistry of ophiolitic gabbroic complexes : a key for the classification of ophiolites
into low-Ti and high-Ti types. Earth Planetary Sci. Letters, 52, p. 203-212.
1982
Berry, R. and Jenner, G.A. 1982 Basalt geochemistry as a tst of the tectonic models of Timor. J. Geol. Soc.
London
Doe, B.R. 1982 The lead and strontium isotope geochemistry of metalliferous sediments associated with
Upper Cretaceous ophiolitic rocks in Cyprus, Syria, and the Sultanate of Oman: Discussion. Canadian Journal
of Earth Sciences, Vol.19, No.8, p. 1720-1723
Cameron, W.E. and Nisbet, E.G. 1982 Phanerozoic analogues of komatiitic basalts, in Arndt, N.T., and Nisbet,
E.G., eds., Komatiites: London, Allen and Unwin, p. 29-50
Coish R.A., Hickey, and Frey, F. 1982 Rare Earth element geochemistry of the Betts Cove ophiolite,
Newfoundland. Geochimica Cosmochimica Acta, v. 46, p. 2117-2135 sub Jan 18 1982. Rare Earth
geochemistry of the Betts Cove ophiolite, Newfoundland: complexities in ophiolite formation. “geochemical
differences can be explained if the three groups were derived from different mantle sources …..the lower
lavas may have formed by melting an extremely depleted mantle invaded by a LREE-enriched fluid. A
possible tectonic environment where these different sources could be juxterposed is a back-arc or inter-arc
basin.”
Doe, B.R. 1982. The lead and strontium isotope geochemistry of metalliferous sediments associated with
Upper Cretaceous ophiolitic rocks in Cyprus, Syria, and the Sultanate of Oman: Discussion. CJES, 19, p.
1720-1723.
Gale, N.H. and Spooner, E.T.C. 1982 The lead and strontium isotope geochemistry of metalliferous sediments
associated with Upper Cretaceous ophiolitic rocks in Cyprus, Syria, and the Sultanate of Oman: Reply.
Canadian Journal of Earth Sciences, Vol.19, No.8, p. 1724-1725
Green, D.H., Duncan, B., Harris, K., Jaques, L., and 1982 The characterization of source magmas for ophiolite
complexes. Ophiolites and Oceanic Lithosphere
Hannah, J. L. and Futa, K. 1982. Nd, Sr, and O isotope systematics in the Troodos ophiolite, Cyprus.
Abstracts with Programs, 95th Annual Meeting, The Geological Society of America, p. 506.
Jenner, G.A. and Green, D.H. 1982 Equilibria in the Mg-rich part of the pyroxene quadrilateral. Min. Mag.
Malpas, J. and Langdon, G. S. 1982. Ultramafic and related rocks of the upper pillow lava suite, Troodos,
Complex, Cyprus. Abstracts with Programs, 95th Annual Meeting of the the Geological Society of America.
Meijer, A., Anthony, E., and Reagan, M., 1982. Petrology of volcanic rocks from the forearc sites. In Hussong,
D. M., Uyeda, S., et al., Init. Repts. DSDP, 60: Washington (U.S. Govt. Printing Office), p. 709-729.
Spooner, E.T.C. and Gale, N.H. 1982. The lead and strontium isotope geochemistry of metalliferous
sediments associated with Upper Cretaceous ophiolitic rocks in Cyprus, Syria, and the Sultanate of Oman.
CJES, 19, p. 1715-1719.
Spooner, E.T.C. and Gale, N.H., reply to Doe,B.R. 1982. The lead and strontium istotope geochemistry of
metalliferous sediments associated with Upper Cretaceous ophiolitic rocks in Cyprus, Syria,and the Sultanate
of Oman: Reply. Canadian Journal of Earth Sciences, 19, 8, p.1724-1725.
Thorpe, R.I. 1982 The lead and strontium isotope geochemistry of metalliferous sediments associated with
Upper Cretaceous ophiolitic rocks in Cyprus, Syria, and the Sultanate of Oman: Discussion. Canadian Journal
of Earth Sciences, Vol.19, No.8, p. 1710-1714.
1983
Cameron, W.E., McCulloch, M.T., and Walker, D.A. 1983 Boninite petrogenesis: Chemical and Nd-Sr isotopic
constraints. Earth and Planetary Science Letters, 65, p. 75-89
McCulloch, M.T. and Cameron, W.E. 1983. Nd-Sr isotopic study of primitive lavas from the Troodos ophiolite,
Cyprus: evidence for a subduction related setting. Geology, 11, p. 727-731.
Robinson, P.T., Melson, W.G., O'Hearn, T. and Schmincke, H.-U. 1983 Volcanic glass compositions of the
Troodos ophiolite. Geology, v. 11, p. 400-404
Rothery, D.A. 1983. The base of a sheeted dyke complex, Oman opiolite: implications for magma chambers at
oceanic spreading axes Jour. Geological Society, v. 140, p. 287-296.
Schminke, H.-V., Rautenschlein, M., Robinson, P.T., and Mehegan, J.M. 1983. Troodos extrusive series of
Cyprus: a comparison with oceanic crust. Geology, 11, p. 405-409.
Walker, D.A. and Cameron, W.E. 1983 Boninite primary magmas evidence from the Cape Vogel Peninsula,
PNG. Contr. Min. Petr., 83, p. 150-158
1984
Bailey, D.G. and Robinson, P.T. 1984. Geochemistry and petrogenesis of of ultramafic extrusives from the
Troodos ophiolite, Cyprus. G.A.C. Ann. Meet., Prog w. Abst. v.9, p. 43.
Crawford, A.J. Cameron, W.E., and Keays, R.R. 1984 The association of boninite low-Ti andesite - tholeiite in
the Heathcote Greenstone belt, Victoria; ensimatic setting for the early Lachlan fold belt Aust. Jour. Earth Sci.
31, p. 161-175
Flower, M.J., Levine, H., and Mehegan, J.M. 1984 Boninite and the Arakapas Fracture zone: initiation of back
arc spreading? G.A.C. Ann. Meet., Prog w. Abst. v.9, p. 62
Malpas et. al. 1984 Investigations of the geochemistry of of some cyprus lavas from holes CY-1 and Cy-2a of
the Cyprus drilling Project. G.A.C. Ann. Meet., Prog w. Abst. v.9, p. 87
Mehegan, J.M. and Robinson, P.T. 1984 Regional geochemistry and pyroxene compositions of the Troodos
ophiolite lavas: the volcanic evolution of Troodos. G.A.C. Ann. Meet., Prog w. Abst. v.9, p. 88
Rautenschlein, M., Jenner, G.A., Hoffman, A.W., 1984 Troodos glass chemistry - Sr, Nd, Pb, O isotopes and
major trace elements. G.A.C. Ann. Meet., Prog w. Abst. v.9, p. 99
Moores, E.M., Robinson, P.T., Malpas, J., and Xenophontas, C. 1984. Model for the origin of the Troodos
Massif, Cyprus, and other mideast Ophiolites, Geology, 12, p.500-503.
Pearce, J.A., Lippard, S.J., and Roberts, S. 1984. Characteristics and tectonic significance of supra
subduction zone (SSZ) ophiolites. In Marginal basin geology: volcanic and associated sedimentary and
tectonic processes in modern and ancient marginal basins. Ed. Kokelaar, B.P. and Howells, M.F. Geological
Society London Spec. Pub., 16, p. 77-94.
Rautenschlein, M., Jenner, G.A., Hoffman, A.W., White, W.M., Schminke, H.-U. and Kerrich, R. 1984. Troodos
glass chemistry - Sr, Nd, Pb, O isotopes and major trace elements. G.A.C. Ann. Meet., Prog w. Abst. v.9, p.
99.
Thorpe,R.S. et al. 1984 Crustal growth and late Precambrian-early Palaeozoic plate tectonic evolution of
England and Wales Jour. Geological Society 141 521-536. Comment- most evolved New Harbour sample has
+ve Zr and -ve Ce or +ve Zr and concave REE; least evolved also show concave REE and strong Nb-Ta
fractionation; show some similarity in low TiO2 and concave REE to boninite; Gwna group mafic rocks are
MORB whereas the the New Harbour have TiO2 .4-.6 zr 40 and the Bryn Teg bore hole TiO2 .4-.5 Zr 10-20
and TiO2 1.0 Zr 50-70; Gwna has +ve Ta-Nb anomalies and some Gwna have transitional alkalic patterns; the
LREE depleted Gwna display a marked -ve Ce anomaly and a high Nb anomaly relative to Ta
1985
Cameron, W.E. 1985. Petrology and origin of primitive lavas from the Troodos ophiolite, Cyprus. Contr. Min.
Pet., 89, p. 239-255.
Gillis, K.M. and Robinson, P.T. 1985. Low Temperature alteration of the extrusive sequence, Troodos
ophiolite, Cyprus. Can. Jour. Earth Sci., 23, p. 431-441.
Rod, E.] au2[] ti[Model for the origin of the Troodos massif, Cyprus, and
other Mideast ophiolites: comment and reply by Moores, E.M.] p[668-669] rg[alps]
tc[tro] kw[] cm[] pb[j] yr[1985] jr[Geology] v[13] no[9
Van der Laan, S.R. et al. 1985 Experimental study of boninite genesis GSA Abst. w. Prgms. 17, 7, p. 739
Varga, R.J. and Moores, E.M. 1985. Spreading structure of the Troodos ophiolite, Cyprus. Lithos, 18, p. 165178. “Ridge jump model”
Mitchell, A.H.G.] au2[] ti[Model for the origin of the Troodos massif,
Cyprus, and other Mideast ophiolites: comment and reply by Moores, E.M.]
p[668-669] rg[alps] tc[tro] kw[] cm[] pb[j] yr[1985] jr[Geology] v[13] no[9
1986
Malpas, J. et a;. (eds) 1987. Ophiolites oceanic crustal analogues: proceedings of the symposium “Troodos
1987”. Cyprus Geological Survey Dept., 733 p.
Murton, B.J. and Gass, I.G. 1986. Western Limassol Forest complex, Cyprus: parts of an Upper Cretaceous
leaky tranform fault. Geology, 14, 255-258.
Thy, P. et al.] yr[1986] ti[Primary igneous mineral
stratigraphy and chemistry of the plutonic sequences of the Troodos ophiolite,
Cyprus. GAC-MAC-CGU, Ottawa, Prg. w. Abst., v. 11] p[137.
Murton, B.J.] au2[] ti[Anomalous oceanic lithosphere formed in a leaky
transform fault: evidence from the Western Limassol Forest complex, Cyprus]
p[845-854] rg[Alps] tc[] kw[Cyprus Troods ophiolite Betts Cove]
cm[ol-opx-cpx-plag cumulates] pb[j] yr[1986] jr[JGS] v[143] no[5
1987
Bloomer, S.H. and Hawkins, J. W. 1987. Petrology and geochemistry of boninite series volcanic rocks from the
Mariana trench. Contr. Min. Pet., 97, 3, p. 361-377.
Boninite series volcanic rocks have been recovered from three dredge hauls on the inner slope of the Mariana
Trench. These hauls included olivine boninites, boninites, boninitic andesites and boninitic dacites, as well as
island arc tholeiitic basalts and andesites. The boninite series volcanics range from 52 to 68% SiO2, and are
characterized by very low abundances of high-field-strength cations and heavy-rare-earth elements. Boninites
and olivine boninites have phenocrysts of olivine and orthopyroxene, the andesites phenocrysts of
orthopyroxene and clinopyroxene, and the dacites orthopyroxene, clinopyroxene, and plagioclase. Most of the
major and trace element variation in the series from boninite to boninitic dacite can be modelled by
fractionation of olivine, orthopyroxene, clinopyroxene, and plagioclase in the proportions 2.5:4:1:2 leaving 47%
residual liquid. The fractionation must be in part open-system: reverse zoned phenocrysts, resorbed olivine
and plagioclase xenocrysts, and bulk rock compositions which cannot be fit by simple closed system
crystallization indicate some magma mixing and phenocryst accumulation. Two boninitic magma stems
can be identified, with similar high-field-strength element abundances, but different amounts of Ca, Na, Al and
light-rare-earth elements. There is also evidence for a magma stem transitional in chemistry from the boninites
to arc tholeiites. The compositions of these boninites are consistent with hypotheses for boninite formation by
partial melting of a depleted mantle mixed with an incompatible element enriched fluid. The Mariana
forearc boninite series lacks a strong iron enrichment, but produces andesites with lower Ti, Al and Y/Zr, and
higher Mg, Ni and Cr than typical calcalkaline arc andesites and dacites. Boninites in the Mariana system were
erupted only in the earliest phases of subduction zone activity.
Philpott, G. 1988 Precious-metal and geological investigation of the Charlo River area, New Brunswick In
Thirteenth annual review of activities, project resumes. Edited by S.A. Abbott, New Brunswick Department of
Natural Resources and Energy, Information circular 88-2 27 7 20-31 Comment- ref in Paktunc 1990
Church, W.R. 1987. The geochemistry and petrogenesis of ophiolitic volcanic rocks from Lac de l’Est, Thetford
Mines Complex, Quebec, Canada: Discussion. Can. Jour. Earth Sci., 24, p. 1270-1273.
“Are the “high”-TiO2 volcanics really high in TiO2?”, “Lac de l’Est volcanics: MOR or arc rocks?”, “Are the
“high”-TiO2 volcanics and the plutonic series consanguinous?”, “Are the “high”-TiO2 And low-TiO2 volcanic
rocks coeval?”, “Significance of the red argillites at Lac de l’Est”, “The Thetford ophiolite as a strike-slip forearc sliver” “comparison with Troodos”
Dion, C. 1987. Geologie de la region de Troodhitissa, complexe plutonique de Troodos, Chypore. These
M.Sc., Universite Laval, Quebec.
Thibault, Y., 1987. Geologie et petrologie des gabbros et des dykes de la region de Phini, complexe
ophiolitique de Troodos, chypre, These, M.Sc., Universite de Laval, Laval, Quebec.
Thy, P. 1987. Magmas and magma chamber evolution, Troodos ophiolite, Cyprus. Geology, 15, p. 316-319.
Vibetti, N. J. 1987. A study of deep fluid circulation in the Troodos ophiolite, Cyprus. Thesis (Ph.D) University
of Western Ontario. (Dissertation Abstracts International, Volume: 48-06, Section: B, page: 1625)
1989
Brown, A.V. and Waldron, H.M. 198? High magnesian andesites within a Cambrian continental rift
environment,Western Tasmania. Abst. no. 68, Reikjavick, Iceland Comment- High Mg andesites have low
TiO2 (.1), concave upwards REE patterns, p. 15-20. MgO, Zr 10, Cr/Cr+Al 89-94. Are interbedded pillow,
breccia and massive flows. Flows overlie Precambrian basement. Cumulates include opx-bearing dunite.
Preceded by olivine (few) and cpx and/or plag (most) phyric- tholeiites, interbedded with terrigene clastic
rocks, with TiO2 .7-1.0. A third phase of volcanic activity produced highly depleted, low-TiO2 (.2-.6) Zr 15ppm,
Y 10 ppm, severally depleted LREE (La/Yb .5) quartz tholeiites. Interlayered with mass flow conglomerates at
the base of the middle- Middle Cambrian continental derived clastic turbidites.
Hall, J.M., Walls, C.C, and Yang, J-S. 1989. Constructional features of the Troodos ophiolite and implications
for the distribution of orebodies and the generation of oceanic crust. Can. Jour. Earth Sci., 26, p. 1137-1139.
Smith, I.E.M. and Mitchell, P.A. 1989 High magnesium lavas in the late Cenozoic volcanic arc associtions of
southeastern Papua, New Guinea. Neues Jahr. Mineralogie monats. 11, p. 481-497
1990 - present
Church, W.R. 1990. Constructional features of the Troodos ophiolite and implications for the distribution of
orebodies and the generation of oceanic crust: discussion. Can. Jour. Earth Sci., 27, p. 1137-1139. Reply p.
1139-1141.
http://instruct.uwo.ca/earth-sci/fieldlog/cyprus/church_hall.rtf
As a variation on this theme it has also been suggested (Church 1987) that low-Ti ophiolites (e.g.,
Hamois and Morency 1988) may have formed in spreading centres originating as transpressive basins in the
frontal parts of developing arcs during oblique subduction. In this context the Arakapas fault would
represent transpressive shear along which a locus of spreading had begun to develop involving intrusion
and extrusion of magmas typically showing the crystallization sequence olivine-orthopyroxeneclinopyroxene-plagioclase found in primitive spreading centres ophiolites of the Appalachians (Betts Cove
- Thetford - Mount Orford)- If the Troodos ophiolite did indeed form as a supra-subduction complex of this
type, comparisons of Troodos wlth "classic" ocean crust as made by the authors may not be entitely appropriate.
http://instruct.uwo.ca/earth-sci/fieldlog/cyprus/hall_church.rtf
The final question arising from Church's discussion concerns the large-scale tectonic
environment in which Troodos was formed. Following Pearce et al. (1984) Church suggests that
Troodos may have been formed at a spreading centre located in a transgressive basin located in the
frontal part of a developing arc during oblique subduction. The difficulty with this suggestion is that
no known example of this type of basin occurs in the present oceans. A substantial number of basins
containing some oceanic crust do occur in association with subduction zones and a better way to
proceed, following Moores et al. (1984), is to seek an analog for Troodos among these basins.
Following tentative identification, key features of the comparison can be tested, as Moores et al. have
suggested for the Andaman Sea basin, their suggested analog.
Kay, R.W. and Mahlburg-Kay, S. 1991 Creation and destruction of lower continental crust Geol. Rundschau 80
2 p. 259-278
http://www-odp.tamu.edu/publications/126_SR/VOLUME/CHAPTERS/sr126_28.pdf 1992
Henriette Lapierre,2,3 Rex N. Taylor,4 Olivier Rouer,3 and Hervé Chaisemartin3 1992. 28. MINERAL
CHEMISTRY OF FOREARC VOLCANIC ROCKS FROM THE IZU-BONIN ARC, HOLES 792E AND 793B1,
in Taylor, B., Fujioka, K., et al., Proceedings of the Ocean Drilling Program, Scientific Results, Vol. 126
The Izu-Bonin forearc basement volcanic rocks recovered from Holes 792E and 793B show the same
phenocrysts assemblage (i.e., Plagioclase, two pyroxenes, and Fe-Ti oxides ±olivine), but they differ in the
crystallization sequence and their phenocryst chemistry. All the igneous rocks have suffered low-grade
hydrothermal alteration caused by interaction with seawater. As a result, only clinopyroxenes, plagioclases,
and oxides have preserved their primary igneous compositions.
The Neogene olivine-clinopyroxene diabasic intrusion (Unit II) recovered from Hole 793B differs from the
basement basaltic andesites because it lacks Cr-spinels and contains abundant titanomagnetites (Usp 38.546.4) and uncommon FeO-rich (FeO = 29%) spinels. It displays petrological and geochemical similarities to
the Izu Arc volcanoes and, thus, can be considered as related to Izu-Bonin Arc magmatic activity.
The titanomagnetites (Usp 28.5-33) in the calc-alkaline andesitic fragments of the Oligocene volcaniclastic
breccia in Hole 793B (Unit VI) represent an early crystallization phase. The Plagioclase phenocrysts enclosed
in these rocks show oscillatory zoning and are less Ca-rich (An 78.6-67.8) than the Plagioclase phenocrysts of
the diabase sill and the basement basaltic andesites. Their clinopyroxenes are Fe-rich augites (Fs </= 19.4;
FeO = 12%) and thus, differ significantly from the clinopyroxenes of the Hole 793B arc-tholeiitic igneous rocks.
The 30-32 Ma porphyritic, two-pyroxene andesites recovered from Hole 792E are very similar to the andesitic
clasts of the Neogene breccia recovered in Hole 793B (Unit VI). Both rocks have the same crystallization
sequence, and similar chemistry of the Fe-Ti oxides, clinopyroxenes, and plagioclases: that is, Ti-rich (Usp
25.5-30.4) magnetites, Fe-rich augites, and intensely oscillatory zoned plagioclases with bytownitic cores (An
86-63) and labradorite rims (An 73-68). They display a calc-alkaline differentiation trend (Taylor et al., this
volume).
So, the basement highly porphyritic andesites recovered at Hole 792E, and the Hole 793B andesitic clasts of
Unit VI show the same petrological and geochemical characteristics, which are that of calc-alkaline suites.
These Oligocene volcanic rocks represent likely the remnants of the Izu-Bonin normal arc magmatic activity,
before the forearc rifting and extension.
The crystallization sequence in the basaltic andesites recovered from Hole 793B is olivine-orthopyroxeneclinopyroxene-plagioclase-Fe-Ti oxides, indicating a tholeiitic differentiation trend for these volcanic rocks.
Type i is an olivine-and Cr-spinel bearing basaltic andesite whereas Type ii is a porphyritic pyroxene-rich
basaltic andesite. The porphyritic plagioclase-rich basaltic andesite (Type iii) is similar, in most respects, to
Type ii lavas but contains Plagioclase phenocrysts. The last, and least common lava is an aphyric to sparsely
phyric andesite (Type iv). Cr-spinels, included either in the olivine pseudomorphs of Type i lavas or in the
groundmass of Type ii lavas, are Cr-rich and Mg-rich. In contrast, Cr-spinels included in clinopyroxenes and
orthopyroxenes (Types i and ii lavas) show lower Cr* and Mg* ratios and higher aluminium contents.
Orthopyroxenes from all rock types are Mg-rich enstatites. Clinopyroxenes display endiopsidic to augitic
compositions and are TiO2 and A12O3 depleted. All the crystals exhibit strong zoning patterns, usually
normal, although, reverse zoning patterns are not uncommon. The plagioclases show compositions within the
range of An 90-64. The Fe-Ti oxides of the groundmass are TiO2-poor (Usp16-17).
The Hole 793B basaltic andesites show, like the Site 458 bronzites from the Mariana forearc, intermediate
features between arc tholeiites and boninites: (1) Cr-spinel in olivine, (2) presence of Mg-rich bronzite, Ca-Mgrich clinopyroxenes, and Ca-plagioclase phenocrysts, and (3) transitional trace element depletion and εNd
ratios between arc tholeiites and boninites. Thus, the forearc magmatism of the Izu-Bonin and Mariana arcs,
linked to rifting and extension, is represented by a depleted tholeiitic suite that displays boninitic affinities.
Fediuk, F. 1992 Pre-Variscan boninite metavolcanics in the Bohemian Massif, Czechoslovakia Ofioliti 16 2 p.
127-128
Stern, R.J. and Bloomer, S.H. 1992 Subduction zone infancy: examples form the Eocene Izu-Bonin-Mariana
and Jurassic California arcs BGSA, 104, 12, p. 1621-1636
Sweeney, R.J. et al. 1992 Trace and minor element partitioning between garnet amphibole and carbonatitic
melt. EPSL, 113, p. 1-14 Comment- claims Zr/Nb greater in MORB than IAB, see McCulloch and Gamble
EPSL 1991
1993
Woodhead,J. et al. 1993 High field strength and transition element systematics in island arc and back-arc
basin basalts: evidence for multi-phase melt extraction and a depleted mantle wedge EPSL 114 2 p. 491-504
Morel, Steven 1993. Ian Gass - a personal tribute Geoscienteist, 5, 3 p37 cm[information on the early work re
sheeted diabases on Cyprus; fist published in attenuated form in 1960]
REX. N. TAYLOR, ROBERT W. NESBITT, PHILLIPE VIDAL, RUSSELL S. HARMON, BERNARD AUVRAY
and IAN W. CROUDACE 1994. Mineralogy, Chemistry, and Genesis of the Boninite Series Volcanics,
Chichijima, Bonin Islands, Japan J. Pet., 35, 3, 577-617.
The Bonin archipelago represents an uplifted fore-arc terrain which exposes the products of Eocene suprasubduction zone magmatism. Chichijima, at the centre of the chain, represents the type locality for the high-Mg
andesitic lava termed boninite. The range of extrusives which constitute the boninite series volcanics are
present on Chichijima, and are disposed in the sequence boninite-andesite-dacite with increasing height in the
volcano-stratigraphy. Progression to evolved compositions within the Chichijima boninite series is controlled by
crystal fractionation from a boninite parental magma containing c. 15% MgO. Olivine and clinoenstatite are the
initial liquidus phases, but extraction of enstatitic orthopyroxene, followed by clinopyroxene and plagioclase, is
responsible for the general evolution from boninite, through andesite, to dacite. Some andesites within the
overlying Mikazukiyama Formation are petrographically distinct from the main boninite series in containing
magnetite phenocrysts and a high proportion of plagioclase. As such, these andesites have affinities with the
calc-alkaline series.
Major and trace element data for 74 boninitic series rocks from Chichijima are presented. Although major
element variation is dominantly controlled by high-level crystal fractionation, the large variations in
incompatiable trace element concentrations at high MgO compositions cannot be explained by this
mechanism. Nd, Pb, and Sr isotopic data indicate the following: (1) a strong overprint on 87Sr/86Sr by seawater
alteration; (2) Pb isotopes lie above the northern hemisphere reference line (NHRL) and are thus similar to the
<30-Ma are and basin lavas of the Izu—Bonin system, and (3) EpNd(40 Ma) ranges between 2.8 and 6.8 within
the boninite series volcanics. Differences in rare-earth elements (REE), Zr, Ti, and 143Nd/144Nd at similar
degrees of fractionation can be explained by the addition of a component of fixed composition from the downgoing oceanic crustal slab to a variably depleted source region within the overlying wedge. Data presented for
Sm/Zr and Ti/Zr indicate that boninite series volcanics are characterized by low values for both of these ratios.
In particular, boninites appear to have uniquely low Sm/Zr ratios. These characteristics may be the result of
slab melting in the presence of residual amphibole; the resultant melt could combine with typical slab
dehydration fluids and infiltrate the overlying mantle wedge. Such a fluid—melt component could mix either
with shallow mantle or directly with primitive melts from depleted mantle. Trace elements, REE, and isotope
data thus point to a model for boninite genesis which requires tightly constrained pressure—temperature
conditions in the slab combined with melting of a variably depleted source in the overlying wedge. Such
constraints are rarely met except during the subduction of juvenile oceanic crust beneath a young, hot
overriding plate.
Bickle, M.J., Teagle, D.A. H., and Beynon, J. 1998. The structure and controls on fluid-rock interactions in
ocean ridge hydrothermal systems: constraints from the Troodos ophiolite, p. 127-152 in Mills, R.A. and
Harrison, K., Modern Ocean Floor Processes and the geologic record, The Geological Society, London.
Wells, D.M. and Mills, R.A., S. Roberts 1998. Rare earth element mobility in a mineralized alteration pipe
within the Troodos ophiolite, Cyprus, p. 153-176, in Mills, R.A. and Harrison, K., Modern Ocean Floor
Processes and the geologic record, The Geological Society, London.
http://www.ucm.es/info/estratig/JIG/vol30/3diaz%20azpiroz.pdf
M. Díaz Azpiroz1, A. Castro2, C. Fernández3, S. López2, J.C. Fernández Caliani2, I. Moreno-Ventas 2004.
The contact between the Ossa Morena and the South Portuguese zones. Characteristics and significance of
the Aracena metamorphic belt, in its central sector between Aroche and Aracena (Huelva). Journal of Iberian
Geology, 30 ,p. 23-51
The boundary between the Ossa Morena and the South Portuguese zones is outlined by the Aracena
metamorphic belt. The main characteristics of this region of the Iberian Massif are divided into lithologic,
structural, metamorphic, magmatic, geochemical, isotopic and experimental points of view and presented in
this paper. The Aracena metamorphic belt is divided into two main domains: the oceanic domain is composed
of MORB-derived metabasites (the Acebuches metabasites) and a former accretionary prism. The continental
domain comprises aluminous gneisses and migmatites, calc-silicate rocks, leucocratic gneisses, marbles,
amphibolites, syn- to post-tectonic noritic intrusions with high-Mg andesite (boninitic affinities) composition,
as well as post tectonic acid-to-basic intrusive rocks. The Acebuches metabasites were firstly affected by a
high-temperature/low-pressure event, which currently shows an inverted metamorphic gradient, and is related
to SW verging thrusting. The thermal peak related to this metamorphic event displays an age gradient in such
a way that older ages have been obtained towards the west. The lower half of the Acebuches metabasite pile
was later affected by a mylonitic deformation and a retrometamorphism related to the Southern Iberian Shear
Zone. Four ductile deformation phases have been defined in the continental domain: CD-D1 was related to the
formation of km-scale recumbent folds. CD-D2 could be associated with an extensional collapse or a gravity
spreading, and is coeval with a high-temperature/low-pressure metamorphic event that affected the continental
domain and gave place to several migmatitic complexes. CD-D3 produced symmetric upright folds and CD-D4
generated south-verging thrusts and thrusts accommodation folds.
The main characteristics of the Aracena metamorphic belt are interpreted as the result of a trench-trenchridge triple junction evolution. According to the proposed model, the oceanic ridge-trench interaction led to the
formation of a slab-free window beneath the continental margin, which provoked the upwelling of the
underlying astenosphere and a subsequent thermal rebound. This triple junction migrated along the
continental margin towards the east, which gave place to the generation of a high-temperature/low-pressure
metamorphic belt in the contact between the Ossa Morena and the South Portuguese zones.
http://translate.google.com/translate?hl=en&sl=zhCN&u=http://www.wanfangdata.com.cn/qikan/periodical.Articles/hddzxyxb/hddz2006/0601/060109.htm&sa=X
&oi=translate&resnum=8&ct=result&prev=/search%3Fq%3DMeijer%2BA.%2B1980%2Bboninite%26hl%3Den
%26rls%3DGGIC,GGIC:2006-50,GGIC:en
Lai Shao Yong-Fei Li Juan Wang Xin Liu Qin Jiang Feng. 2006. Bikou boninite rock geochemistry and tectonic
setting of diagenesis. Donghua Polytechnic Journal, (Journal of East China Institute of Technology) 29, 1,
p.43-48.
Major and trace elements in system shows that the Bikou Nanfan dam meta-basalts, temple Bay area, with a
low Si, Ti low, low P, high and high Mg Al2O3/TiO2 features, boninite rock geochemical characteristics;
Standardization of the N-element distribution map, the loss of high field strength elements (Ti, Zr, Y).
Enrichment refractory elements (Cr, Co, Ni), REE patterns loss was LREE leftist form suggest that the rocks
may have experienced a higher degree of partial melting of the early losses after refractory mantle wedge
peridotite. participate in a small amount of water formed by partial melting of the case. Combined with the
island-arc tholeiite, boninite rocks in this area should be an arc from the environmental mitigation, This
understanding for determining the structure of the Bikou volcanic attribute great significance.