Geochemistry of Proterozoic volcanic and granitic rocks from the Gold Hill-Wheeler Peak area, northern New Mexico

Condie, Kent C.; McCrink, Timothy P.

doi:10.1016/0301-9268(82)90056-0

Cited by 24 publications

(4 citation statements)

References 22 publications

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“…Potentially the Mazatzal terrane was moving north towards the Yavapai terrane as indicated by the W–E orientation of FIA‐I, but had not arrived. This fits with the generally accepted model for Laurentian accretion of juvenile island‐arc terranes accreting from the south onto Achean provinces (Condie & McCrink, 1982; Karlstrom et al. , 1987; Karlstrom & Bowring, 1988; Amato et al.…”

Section: Discussionsupporting

confidence: 88%

FIA trends along the Precambrian Rocky Mountains: a new approach to timing continental docking

Cao

Fletcher

2012

Journal Metamorphic Geology

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A similar succession of Foliation Inflection/Intersection Axis (FIAs) trends preserved within porphyroblasts is present in two areas separated by 200 km along the Rocky Mountains. The Precambrian rocks in Central Colorado and Northern New Mexico were affected by deformation and metamorphism from ∼1506 to 1366 Ma. A succession of five FIAs trending W–E, SSW–NNE, NNW–SSE, NW–SE and WSW–ENE is distinguished in Central Colorado and dated at 1506 ± 15 Ma, 1467 ± 23 Ma, 1425 ± 18 Ma, not dated and 1366 ± 20 Ma respectively. To the south in Northern New Mexico, a succession of five FIAs trending SSW–NNE, WNW–ESE, NNW–SSE, NW–SE and WSW–ENE is distinguished and dated at 1482 ± 48 Ma, 1448 ± 12 Ma, 1422 ± 35 Ma, not dated and 1394 ± 22 Ma. The excellent correlation of the sequence of FIA trends and their ages between regions reveals a sixfold‐FIA succession across the region with the first developed FIA set in Central Colorado not present in Northern New Mexico and the third FIA set in the region not present in Central Colorado. Preferential partitioning of W–E trending deformation into the Central Colorado region ∼1506 ± 15 Ma was followed by SSW–NNE trending deformation that affected both regions at 1470 ± 20 Ma. However, preferential partitioning of WNW–ESE trending deformation into Northern New Mexico at 1448 ± 12 Ma left Central Colorado unaffected. Both regions were then affected by the three remaining periods of orogenesis, the first trending NNW–SSE at 1424 ± 15 Ma followed by one trending NW–SE that has not yet been dated, and then one trending WSW–ENE at 1390 ± 19 Ma. This suggests that the Yavapai terrane was tectonized at ∼1506 Ma, prior to amalgamation with the Mazatzal terrane ∼1470 Ma. Subsequent orogenesis was initially partitioned preferentially into the Mazatzal terrane, but the following three periods of tectonism affected both terranes in a similar manner.

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Section: Discussionsupporting

confidence: 88%

FIA trends along the Precambrian Rocky Mountains: a new approach to timing continental docking

Cao

Fletcher

2012

Journal Metamorphic Geology

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“…As with other Proterozoic arc associations in the Southwest (Condie and Nuter, 1981;Condie and Shadel, 1984;Condie and McCrink, 1982;Boardman and Condie, 1986;Condie, 1986;Knoper and Condie, 1988), the Pecos succession is characterized by bimodal volcanism. Young bimodal volcanic arc systems have been reported (Whitney and others, 1978;Condie and Shadel, 1984;Condie, 1986), but they appear to be more common in the Proterozoic.…”

Section: Tectonic Settingmentioning

confidence: 52%

Geology and geochemistry of early Proterozoic volcanic and subvolcanic rocks of the Pecos greenstone belt, Sangre de Cristo Mountains, New Mexico

Robertson

Condie

1989

Geological Society of America Special Papers

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The Pecos greenstone belt, dated at ca. 1,720 Ma, consists of metamorphosed subaqueous basalts together with locally important felsic volcanic rocks, iron-formation, and metasedimentary rocks, some of volcanic provenance. Volcanic rocks define a compositionally bimodal suite of basalt (80 percent) and dacite-rhyolite (20 percent). Mafic volcanics are mostly fine-grained, massive to well-foliated amphibolite that locally display relict amygdules, pillows, and pillow breccia. Felsic volcanic rocks are mainly porphyritic flows and crystal-rich volcaniclastic units that contain variable amounts of quartz, K-feldspar, and plagioclase phenocrysts. The greenstone belt also includes a compositionally bimodal subvolcanic complex that intrudes, and is locally overlain by, portions of the volcano-sedimentary pile. The subvolcanic complex comprises concordant to discordant, hypabyssal intrusions of tonalite-trondhjemite (65 percent) and diabase-gabbro (30 percent). Ultramafic and mafic rocks with possible ophiolitic affinities constitute the remaining 5 percent of the subvolcanic complex.Greenstone-belt rocks have undergone regional metamorphism of upper greenschist to lower amphibolite grade and show the effects of at least three periods of deformation. The metamorphic sequence is cut by pre-to syn-orogenic granites and quartz porphyries dated at ca. 1,650 Ma and by syn-to post-orogenic granitic rocks dated at ca. 1,500 to 1,450 Ma. Mafic volcanic and subvolcanic rocks define four distinct chemical populations: (1) ultramafic, (2) high-Mg tholeiite, (3) tholeiite, and (4) calc-alkaline basalt (CAB).Geochemically, the high-Mg tholeiites are similar to Archean high-Mg tholeiites, whereas the tholeiites and calc-alkaline basalts are similar to their counterparts in modern arc systems. The ultramafic rocks and various basalt groups cannot be related to each other by closed-system fractional crystallization or batch melting of a single mantle source. Their incompatible-element ratios seem to demand at least three different mantle sources (one depleted). Felsic volcanics can be divided into three groups (one rhyolitic and two dacitic) on the basis of immobile-element abundances. The rhyolites and one dacite group can be produced by fractional crystallization of CAB. The other dacite group (Doctor Creek dacite) is not obviously or easily related, chemically or genetically, to the rest of the Pecos volcanic and subvolcanic rocks. It instead may belong to a younger (ca.

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“…Cullers and Graf Table 3. Characteristics of I-and S-type granites (Chappell and White 1974;Beckinsale 1979 Barker et al 1976;Condie and McCrink 1982) or fractionation of, say, hornblende and plagioclase during crystallization (e.g., Arth et al 1978;Frey et al 1978;Condie and McCrink 1982). Several minor minerals present either in the residue or as crystallizing phases obviously have an important effect on the REE patterns of felsic magmas (Fourcade and Allegre 1981;Miller and Mittlefehldt 1982).…”

Section: Synkinematic Granitoidsmentioning

confidence: 99%

“…Hence many authors favour partial melting as the principal mechanism producing voluminous granitic magmas (White and Chappell 1977;Green 1980;Barker et al 1981;Pitcher 1983;Othman et al 1984). However, the Proterozoic tonalites of the Uusikaupunki-Kalanti area and northern New Mexico are very closely related to basic and intermediate rocks, including cumulus amphibolite and hornblendite (Arth et al 1978;Condie and McCrink 1982). It is probable from field geology and petrogenetic modelling that these tonalites represent fractional crystallization products of tholeiitic basaltic magmas.…”

Section: Synkinematic Granitoidsmentioning

confidence: 99%

The Proterozoic granitoids of Finland: Granite types, metallogeny and relation to crustal evolution

Nurmi¹,

Haapala²

1986

Bull Geol Soc Finland

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Geochemistry of Proterozoic volcanic and granitic rocks from the Gold Hill-Wheeler Peak area, northern New Mexico

Cited by 24 publications

References 22 publications

FIA trends along the Precambrian Rocky Mountains: a new approach to timing continental docking

FIA trends along the Precambrian Rocky Mountains: a new approach to timing continental docking

Geology and geochemistry of early Proterozoic volcanic and subvolcanic rocks of the Pecos greenstone belt, Sangre de Cristo Mountains, New Mexico

The Proterozoic granitoids of Finland: Granite types, metallogeny and relation to crustal evolution

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