U-Pb zircon geochronology of the Galway Granite, Connemara, Ireland: implications for the timing of late Caledonian tectonic and magmatic events and for correlations with Acadian plutonism in New England.
The Galway Granite occupies a key location in the Caledonkles of western Ireland. The 80 km long, WNW-trending axis of the batholith lies astride and stitches the EW-trending Skerd Rocks Fault, a splay of the orogen-parallelSouthern Uplands Fault. The Skerd Rocks Fault separates high-grade metamorphic rocks of the Connemara Massif from Lower Ordovician greenschist-facies metavolcanic and metasedimentary rocks. We present new isotopic U-Pb zircon age determinations, using thermal ionisation mass spectrometry (TIMS), for five granite samples from the central block of the Galway Granite. Early coeval diorite and granite magmas are concomitant with the development of pure flattening fabrics and are succeeded by emplacement of a suite of generally unfoliated granites intruded in a brittle fracture regime. The results of the U-Pb zircon geochronology (G1 = 394.4 [+ or -] 2.2 Ma; G2~402 Ma; G3 39Z7 [+ or -] 1.1 Ma; G4 = 399.5 [+ or -] 0.8 Ma) indicate that the emplacement of the early suite occurred over at least 8 Ma and belongs to the Late Emsian stage. Samples of commingled diorite (G3) and granite (G4) yield ages that are indistinguishable within error. Sample G5 is from an alkali feldspar leucogranite that cuts the early suite. Zircon from this granite yielded a U-Pb age of 380 [+ or -] 6 Ma and a single concordant monazite yielded 383.6 Ma, indicating emplacement at the Givetian-Frasnian boundary and a gap of ~20 Ma between intrusion of the two granite suites. These data provide constraints on the timing of final movement on the orogen-parallel strike-slip Southern Uplands-Skerd Rocks Fault System, and have implications for correlations between Acadian plutonism in New England and in western Ireland.
Le granite de Galway occupe un emplacement cle dans les Caledonides de l'ouest de l'Irlande. Le batholite de 80 kilometres de longueur suivant un axe ouest-nord-ouest chevanche et suture la faille orientde d'est en ouest des rochers Skerd, un evasement de la Faille parallele a l'orogene des Hautes terres du Sud. La Faille des rochers Skerd separe des roches metamorphiques a forte teneur do massif de Connemara de roches metasedimentaires et metavolcaniques d'un facies de schistes verts de l'Ordovicien inferieur. Nous presentons de nouvelles datations isotopiques au U-Pb obtenues a partir de zircon, au moyen de la spectrometrie de masse a ionisation thermique (SMIT), de cinq echantillons de granite provenant du bloc central du granite de Galway. Les premiers magmas granitiques et dioritiques contemporains sont apparus en meme temps que se sont etablis les fabriques d'aplanissement pures et ils ont ete suivis de l'intrusion d'un cortege de granites generalement non feuilletes penetrant darts un regime de rupture fragile. Les resultats de l'exercice gdochronologique au U-Pb 5, partir de zircon (G1 = 394,4 [+ or -] 2,2 Ma; G2 ~ 402 Ma; G3 397,7 [+ or -] 1,1 Ma; G4 = 399,5 [+ or -] 0,8 Ma) revelent que l'intrusion du premier cortege s'est etchelonnee au cours d'au moins 8 Ma et qu'elle remonte au stade de l'Emsien tardif. Des echantillons de diorite (G3) et de granite (G4) melanges ont presente des ages qu'il est impossible de distinguer sans erreur. L'echantillon G5 provient d'un leucogranite de feldspath alcalin qui entrecoupe le cortege initial. La datation au U-Pb a partir de zircon de ce granite a revele qu'il etait age de 380 [+ or -] 6 Ma et un echantillon de monazite concordant unique a ete situe a 383,6 Ma, un age temoignant d'une mise en place a la limite du Givetien et du Frasnien et d'un ecart d'environ 20 Ma entre l'intrusion des deux corteges granitiques. Ces donndes imposent des contraintes fi la localisation chronologique du deplacement sur les groupements de decrochements paralleles a l'orogene des Hautes terres du Sud-rochers Skerd, et elles ont des repercussions sur les correlations entre le plutonisme acadien en Nouvelle-Angleterre et dans l'ouest du l'Irlande.
[Traduit par la redaction]
In the North Atlantic region, the Caledonian Orogeny embraces Cambrian to Devonian tectonic and magmatic events associated with the development and subsequent closure of those parts of the Iapetus Ocean which were situated between Laurentia to the northwest and Baltica and Avalonia to the southeast and east (McKerrow et al. 2000). The orogeny includes several tectonic phases, many reflecting localized events like arc-arc, arc-continent, and continent-continent collisions, e.g., the Taconic Phase in the New England Appalachians and the Grampian Phase in Ireland and Britain.
The Caledonides of western Ireland occupy a key location along the Appalachian-Caledonian orogenic belt (Fig. 1a, b). They provide a significant N-S cross-section that includes the Laurentian margin in the north passing southwards through the South Mayo trough and the Connemara Massif to the Iapetus Suture and onto the Avalonian margin (Klemperer et al. 1991; Ryan and Dewey 1991; Friedrich et al. 1999). The South Mayo trough possesses island arc and ophiolite elements (Dewey and Ryan 1990). The boundary of the allochthonous Connemara metamorphic terrane with the South Mayo Trough is occluded by Silurian rocks. The Connemara metamorphic terrane defines the Grampian Phase in western Ireland and exposes rocks formed during a short-lived Lower Ordovician magmatic arc emplaced into Laurentian margin Dalradian rocks at ca. 475-463 Ma. (Friedrich et al. 1999). The Skerd Rocks Fault brings greenschist facies rocks of oceanic affinity, the Lower Ordovician South Connemara Group (Ryan et al. 1983; Williams et al. 1988), against the Connemara metamorphic terrane. Southward Klemperer et al. (1991) suggest that a mix of accreted, imbricated, oceanic, island arc, and continental sediments and volcanic rocks extend beneath the Carboniferous strata from Galway Bay to the Shannon Estuary which marks the southwestern end of the NE-trending Iapetus Suture in Ireland and Britain.
Three major strike-slip faults (i.e. The Great Glen, Highland Boundary and Southern Uplands Faults-see Fig. 1b) parallel the Iapetus Suture and mark significant kilometric-scale sinistral displacements of crustal blocks during the end stages of the orogen (Dewey and Strachan 2003). Furthermore, this set of regionally important orogen- parallel displacements is linked to the emplacement of late Caledonian granites in Britain and Ireland (Dewey and Strachan 2003 and references therein). High precision U-Pb geochronology (using TIMS) of the Newer Granites in Scotland has been used to constrain the timing of displacement along these faults. Early sinistral displacements "along the Great Glen Fault, for example, are linked to the emplacement of the Clunes Tonalite at 427.8 [+ or -] 1.9 Ma. (Stewart et al. 2001). Indeed, Dewey and Strachan (2003) concluded that major orogen-parallel, strike-slip motion on the Great Glen Fault and related structures in Scotland occurred between ca.425 and 410 Ma.
[FIGURE 1 OMITTED]
The ca.400 Ma Galway Granite marks an important element of the western Ireland Caledonides as it postdated and stitched a splay, the Skerd Rocks Fault, of one of these major strike-slip fault systems in Britain and Ireland, i.e. Southern Uplands Fault (Leake 1978). Here we report new high precision U-Pb zircon ages for the late-Caledonian Galway Granite and use them (a) to elucidate more fully the duration and timing of granite magmatism in Connemara, (b) to place time constraints on the finality of motion on the Skerd Rocks Fault and the regional implications for the major orogen-parallel faults, and (c) to explore implications for cross-Atlantic correlations with Acadian granite plutonism in the New England Appalachians.
GEOLOGY OF THE GALWAY GRANITE.
The Galway Granite is a late-Caledonian calc-alkaline batholith emplaced at ca. 400 Ma (Leggo et al. 1966; Pidgeon 1969) into the 474.5-462.5 Ma Metagabbro-Gneiss Suite to the north (Leake 1989; Leake and Tanner 1994; Friedrich et al. 1999), and into Lower Ordovician greenschist facies rocks (the South Connemara Group) to the south (MeRle and Burke 1955; Williams et al. 1988). The batholith emplacement postdated the Skerd Rocks Fault which Leake (1978) considered to be a splay of the Southern Uplands Fault and to have strongly influenced its siting. The granite extends for several kilometers beneath the Carboniferous rocks of the Galway Bay area, as indicated on gravity and aeromagnetic maps (Murphy 1952; Max et al. 1983; Madden 1987). The long axis of the batholith is oriented WNW-ESE and is oblique to the E-W strike of the Skerd Rocks Fault. Two major faults, the NNE-trending Shannawona Fault (SF) and the NW-trending Barna Fault (BF), define the boundaries between the western, central, and eastern blocks (Fig. 1c) in the batholith.
The western and eastern blocks expose lithologies that range from granodiorite through granite to alkali granite (Leake 1978 and references therein). The petrology, geochemistry, and field relationships of the central block granites has been described in detail by the following: Feely and Madden (1986, 1987,1988); Whitworth and Feely (1989, 1994); Feely et al. (1989, 1991); El Desouky et al. (1996); Crowley and Feely (1997); Graham et al. (2000); Baxter and Feely (2002); Baxter et al. (in review). These studies presented unequivocal evidence for several phases of granite emplacement. Interactions between coeval diorite and granite magmas (e.g. Mingling and Mixing Zone--MMZ) are concomitant with the development of pure flattening fabrics and are succeeded by emplacement of a suite of generally unfoliated granite units intruded in a brittle fracture regime. Thus, intergranite temporal relationships in this part of the batholith demonstrate that the Megacrystic Granite was emplaced first, along with the MMZ Granodiorite and its enclaves of coeval diorite magma. The Costelloe Murvey Granite (CMG) displays sharp, shallow, outward-dipping chilled marginal contacts with these earlier granites and represents the end stage of magma emplacement in the batholith (Fig. 1d).
Emplacement of the Galway batholith is considered by El Desouky et al. (1996) to have occurred in a crustal pull-apart between NW-trending dextral shear zones marked by the Maam and Clifden Faults. This model helps explain the WSW-ESE trend of the long axis of the batholith and the post-consolidation orthogonal faulting and dyking across the batholith and its envelope. Baxter et al. (in review) interpreted fabrics within the Megacrystic Granite and MMZ Granodiorite to reflect ballooning processes operating in successive magma batches (e.g., Megacrystic Granite and MMZ Granodiorite) at the emplacement level. These earlier granite batches were stoped by the later granite intrusions such as the CMG during a brittle fracture regime (Crowley and Feely 1997). The central block therefore exposes a juxtaposition of earlier deeper level granites with late-stage higher level granites.
U-PB GEOCHRONOLOGY OF THE GALWAY GRANITE
Sampling and analytical methods
TIMS U-Pb zircon geochronology was performed on five samples from the central block of the Galway Granite. Zircon selection, preparation, and thermal ionization mass spectrometry were carried out at the isotope geochemistry laboratory at the Department of Geological Sciences, University of North Carolina, Chapel Hill (Table 1; see footnote for analytical details). The sample set comprises two samples from the Megacrystic Granite, an enclave and its host MMZ Granodiorite, and one sample of the Costelloe Murvey Granite --see Fig. 1d for locations.
G1 and G2 are samples from the Megacrystic Granite which is a distinctive porphyritic granite comprising large (15-80 mm) pink megacrysts of K-feldspar (~15-20%) set in a coarse-grained (2 5 mm) groundmass of plagioclase (-44%), quartz (~22%), K-feldspar (~3 8%), biotite (~7-10%), and hornblende (~1-5%) with accessory titanite, allanite, apatite, zircon, and opaque minerals. Sample G2 is more equigranular and less mafic than G1.
G3 is an enclave hosted by the MMZ Granodiorite (see below). The enclaves are commonly medium to dark grey, and 0.2-0.8 m in length, with axial ratios ranging from 2:1 to 12:1. Mineralogically, they contain phenocrysts (1-4 mm) of plagioclase [+ or -] K-feldspar [+ or -] quartz, in a groundmass (<0.5 mm) of plagioclase (~52%), biotite (~31%), hornblende (~10%), and quartz (~2%), with accessory K-feldspar, titanite, apatite, zircon, allanite, and opaque minerals.
G4 is a sample of the granite host (i.e., MMZ Granodiorite) to sample G3. MMZ Granodiorite is typically medium- to coarse-grained (1 to 10 mm) and contains quartz (~27%), K-feldspar (~25%), plagioclase (~34%), biotite (~8%), hornblende (~3%), and accessory titanite, zircon, allanite, and apatite.
G5 is a sample of the CMG which is a light pink, medium-to coarse-grained alkali feldspar granite containing, on average, 38% quartz, 33% orthoclase, 27% albite (~An5), and 2% biotite with accessory apatite, zircon, monazite, uraninite and thorite.
New U-Pb zircon ages: implications for the magmatic and structural history of the Galway Granite
The results of the U-Pb zircon geochronology (Fig. 2 and Table 2) indicate that the emplacement of the early suite occurred over at least 8 Ma and belongs to the late Emsian stage (Megacrystic Granite G1--394.4 [+ or -] 2.2 Ma; Megacrystic Granite G2-402 Ma; Diorite Enclave G3--39Z7 [+ or -] 1.1 Ma; MMZ Granodiorite G4 = 399.5 [+ or -] 0.8 Ma).
[FIGURE 2 OMITTED]
The commingled diorite (G3) and granodiorite (G4) yield ages that are indistinguishable within error. The CMG sample, GS, yields a U-Pb age of 380.1 [+ or -] 5.5 Ma and a single concordant monazite yields a 383.6 Ma age indicating emplacement at the Givetian-Frasnian boundary and a gap of ~20 Ma between intrusion of the two granite suites. These ages support the field evidence cited above from the central block, and quantify the time gap between the emplacement of the early foliated suite and the intrusion of the CMG. Noteworthy here are the results of a gravity study by Madden (1987) which indicated that the central block is 3-4 km thinner than the western block, supporting the conclusion of Leake (1978) that the granite to the east of the SF was upthrown and eroded to expose a deeper level of the batholith. Furthermore, preliminary geobarometric studies indicate that crystallisation of zoned hornblende in the western block began at 2.6 [+ or -] 1.2 kb and ended at <1.5 [+ or -]1.0 kb, whereas east of the SF unzoned hornblende crystallised at 4.3 [+ or -] 0.7 kb (Leake and Ahmed Said 1994).
The relatively young age of the CMG coupled with its relatively shallow emplacement level and crosscutting nature suggest that it was generated and emplaced syn- to post-uplift of the central block some 20 Ma after the crystallisation of the Megacrystic Granite and MMZ Granodiorite.
Two ages for the batholith have been reported for samples from west of the SF. One is a whole-rock Rb-Sr age of 398 [+ or -] 10 Ma (Leggo et al. 1966) and the second is a bulk zircon U-Pb age from the Carna Granite of 412 [+ or -] 15 Ma. (Pigeon 1969). More precise ages from the western end of the batholith have recently been determined for molybdenite hosted by the Carna and Murvey granites (Fig. 1c; locations C and M) by Selby et al. (in press) using the Re-Os geochronometer. The molybdenite samples hosted by the Carna Granite yielded a Re-Os age of 407.3 + 1.5 Ma, while 410.5 + 1.5 Ma and 410.8 [+ or -] 1.4 Ma were determined for two samples from the Murvey granite. Gallagher et al. (1992) showed that the disseminated and vein molybdenite hosted by both granites is magmatic in origin, and therefore the Re-Os ages cited here reflect granite crystallisation ages. Combining the molybdenite ages with the new U-Pb ages defines a period of granite emplacement in South Connemara from ca. 410 to 380 Ma. In addition, the leucocratic Murvey granite at the western end of the batholith was emplaced some 30 Ma before the intrusion, in the central block, of the lithologically similar CMG. The Megacrystic granite and the MMZ granodiorite and its coeval enclaves postdated the emplacement of the Carna and Murvey granites at the western end of the batholith by ~10 Ma.
This timeframe for the emplacement of the Galway granites correlates with the upper end of the general timescale for Silurian-Devonian 'Newer Granites' both to the north and south of the lapetus Suture (see Fig. 3). A selection of recently published U-Pb TIMS ages has been also added to this timeframe, along with a monazite age (O'Connor et al. 1989) for the Leinster Granite (SE Ireland).
[FIGURE 3 OMITTED]
Implications for the timing of the orogen parallel transcurrent faults in Britain and Ireland
It is apparent from Figure 3 that the emplacement of the Galway Granite postdated Iapetan convergence by ~10 Ma. Dewey and Strachan (2003) in a review of data relevant to the diachronous closure of Iapetus in the North Atlantic Caledonian sector argued that major left-lateral displacement along the orogen-parallel Great Glen Fault and related structures is necessary in the time period 425 410 Ma. Late Caledonian transcurrent faults like the Great Glen, Highland Boundary, and Southern Uplands faults have controlled the ascent and emplacement of granite magmas in Britain and Ireland (e.g., Hutton 1988; Hutton and Reavy 1992). The emplacement of the suite was in transtensional pull-aparts and dilational splays on sinistral strike-slip faults (Hutton 1982, 1988; Hutton and McErlean 1991; Hutton and Reavy 1992; Jacques and Reavy 1994; Stewart et al. 2001). The 410 to 380 Ma period for the emplacement of the Galway granites postdated this period of major left-lateral displacements on these orogen-parallel faults. This timing is in keeping with the stitching nature of the Galway Batholith in relation to the Skerd Rocks Fault. The new ages, therefore, place an upper limit on the timing of major displacements on the Southern Uplands Fault system and support the assertion of Dewey and Strachan (2003) that the 425 410 Ma period was marked by major movement on the orogen-parallel transcurrent faults (Figs.1b, 3).
Implications for cross-Atlantic correlations with the Acadian granite plutonism in the New England Appalachians
Bradley et al. (2000) demonstrated that Acadian syn- and post-tectonic plutons ranging in composition from gabbro to granite are widespread in Maine and adjacent parts of New Brunswick, Quebec, New Hampshire, and Vermont. Dating (using U-Pb and Ar/Ar methods) of key plutons, many granitic in composition, across a broad swath from the Maine coast to the Maine-Quebec border allowed Bradley et al. (2000) to conclude that the Acadian deformation front and the locus of plutonism shifted over time, northwestward, across the northern Appalachian orogen. The timescale for this Acadian plutonism extends from ~420 to 360Ma, marked by the following groupings of pluton ages: (a) Ludlow to Lochkovian plutons that occur along the Maine coast; (b) Emsian plutons that form a NE -SW trending belt, ca.500 km long and some 120 km inland; (c) Late Emsian to Eifelian plutons in the age range 400 to 387.5 Ma that are scattered across the area; (d) Givetian to Early Tournasian plutons that are widespread throughout the region from the coast of Maine northward to the Quebec border.
The timespan of the Acadian orogen in Britain and Ireland is more restricted and extends frome mid-Emsian to mid-Famennian (McKerrow et al. 2000; Dewey and Strachan, 2003; see Fig. 3). The onset of Galway granite plutonism predated the Acadian in Britain and Ireland but correlates with the Emsian, the Late Emsian to Eifelian, and the Givetian to Early Tournasian plutonic groups in Maine. Similarities in timing of plutonism exist in a general sense between the Galway Granite and for example the Seboeis and Moxie plutons (Emsian group Bradley et al. 2000). These two granite plutons in Maine reflect relatively early pluton emplacement at ca.405 Ma followed by a significant time gap of ~35-40 Ma before the final emplacement event occurred, marked for example by the intrusion of the Beaver Cove pluton (ca.372 Ma) into the Moxie pluton and the East Branch Lake granodiorite (ca. 365 Ma) into the Sebois pluton. The emplacement of the 380 Ma CMG into the early suite of Galway granites (410 to 400 Ma) in Connemara also reflects a significant time gap of ca.20-30 Ma. Why there was a resurgence of volumetrically subordinate granite magmatism at the same crustal location some 20 to 30 Ma alter the main phase of granite magmatism had occurred and apparently during the waning stage of orogeny warrants further investigation on both sides of the North Atlantic Ocean.
SUMMARY AND CONCLUSIONS
The TIMS U-Pb ages for the five samples from the Galway granite show that, in keeping with the field relationships, the Megacrystic and MMZ granites crystallised at ca. 400 Ma and were intruded by the CMG at ca.380 Ma. Furthermore, similar ages for both enclave and host (MMZ granodiorite) confirm the coeveality of both magmas. When the TIMS ages are combined with new Re-Os dates (~ 410 Ma) from magmatic molybdenite at the western end of the batholith, it is apparent that Galway Granite plutonism extended discontinuously over a period of ca. 30 Ma. The juxtaposition of the high-level brittle fracture regime CMG with the deeper level Megacrystic and MMZ granites reflects upward movement on the bounding faults of the central block prior to emplacement of the CMG. The new ages also place constraints on the timing of motion on major orogen-parallel transcurrent faults, in particular the Southern Uplands and the Skerd Rocks faults. The emplacement of the Galway granites postdated movement on the Skerd Rocks Fault, constraining final motion to ~410 Ma in keeping with the time constraints for final motion on the Great Glen Fault. The Galway Granite can be assigned to the Acadian, although the time span of the Acadian in New England is more extensive than in Britain and Ireland. Nevertheless useful correlations can be made between the timing and emplacement history of Acadian plutonism in Maine and of western Ireland. In particular, the Moxie and Seboeis plutons of Maine, like the Galway pluton, have intergranite intrusion histories punctuated by time gaps in the order of 30 to 40 Ma. These plutons reflect the resurgence of granite magma at the same crustal location after a very significant time gap and during the waning stages of the Acadian orogeny.
Table 1. U-Pb analytical data for zircon from Galway granites in Connemara, Ireland. Concentrations Atomic ratios Frac. & Weight U Pb ([dagger]) [sup.206]Pb ([section]) no. * (mg) (ppm) (ppm) [sup.204]Pb G1 megacrystic granite z1 0.0069 1649 106.9 21510 z2 0.0033 2250 158.9 15160 z3 0.0037 2137 140.5 7414 z4 0.0059 1276 85.15 12140 G2 megacrystic granite z2 0.0016 1212 81.99 5829 z3 0.0019 612.2 44.16 1700 G3 diorite enclave zl 0.0035 1318 88.04 4498 z2 0.0013 304.9 20.88 603.9 z3 0.0040 911.3 58.02 9988 z4 0.0019 635.1 45.35 3177 G4 magma mingling zone granodiorite zl 0.0058 272.1 18.69 3865 z2 0.0017 491.7 38.47 1011 z3 0.0014 490.1 38.66 1839 z4 0.0014 792.5 65.69 1627 G5 Costelloe Murvey Granite z1 0.0023 3167 237.4 557.4 z2 0.0035 3048 198.1 3385 z3 0.0058 5749 363.9 3859 z4 0.0022 1557 104.7 636.7 z5 0.0063 1856 120.3 2266 z6 0.0016 2018 125.8 934.8 z7 0.0010 4074 425.9 65.51 z8 0.0022 6303 426.3 146.4 z9 0.0058 5972 531.1 136.8 z10 0.0012 9690 679.4 57.68 Atomic ratios Frac. [sup.206]Pb [sup.207]Pb & ([paragraph])/ ([paragraph])/ no. * [sup.238]U (%err) [sup.235]U (%err) G1 megacrystic granite z1 0.06098 (.12) 0.45862 (.16) z2 0.06094 (.15) 0.45878 (.18) z3 0.05790 (.12) 0.43546 (.16) z4 0.06183 (.11) 0.46495 (.15) G2 megacrystic granite z2 0.06430 (.17) 0.48505 (.20) z3 0.06396 (.29) 0.48303 (.33) G3 diorite enclave z1 0.06359 (.13) 0.47897 (.17) z2 0.06460 (.66) 0.49271 (.73) z3 0.06163 (.28) 0.46416 (.30) z4 0.06413 (.20) 0.48521 (.24) G4 magma mingling zone granodiorite z1 0.06393 (.18) 0.48191 (.22) z2 0.06407 (.54) 0.48615 (.60) z3 0.06420 (.30) 0.48831 (.35) z4 0.06316 (.28) 0.47763 (.38) G5 Costelloe Murvey Granite z1 0.05892 (.39) 0.44031 (.46) z2 0.05875 (.15) 0.43924 (.24) z3 0.05834 (.57) 0.43633 (.65) z4 0.05782 (.62) 0.43508 (.68) z5 0.05818 (.18) 0.43474 (.34) z6 0.05618 (1.31) 0.42001 (1.34) z7 0.04450 (.33) 0.34580 (2.13) z8 0.04309 (.50) 0.31745 (3.64) z9 0.04152 (.41) 0.31698 (3.65) z10 0.02683 (.29) 0.20220 (3.11) Atomic ratios Ages (Ma) Frac. [sup.207]Pb & ([paragraph])/ [sup.206]Pb/ [sup.207]Pb/ no. * [sup.206]Pb (%err) [sup.238]U [sup.235]U G1 megacrystic granite z1 0.05455 (.10) 381.6 383.3 z2 0.05460 (.10) 381.3 383.4 z3 0.05455 (.10) 362.8 367.0 z4 0.05454 (.10) 386.7 387.7 G2 megacrystic granite z2 0.05471 (.10) 401.7 401.5 z3 0.05477 (.14) 399.7 400.2 G3 diorite enclave zl 0.05463 (.11) 397.4 397.4 z2 0.05531 (.30) 403.6 406.8 z3 0.05462 (.10) 385.5 387.1 z4 0.05487 (.13) 400.7 401.6 G4 magma mingling zone granodiorite zl 0.05467 (.12) 399.5 399.4 z2 0.05503 (.25) 400.4 402.3 z3 0.05516 (.17) 401.1 403.8 z4 0.05485 (.24) 394.8 396.4 G5 Costelloe Murvey Granite z1 0.05420 (.23) 369.1 370.5 z2 0.05422 (.19) 368.0 369.7 z3 0.05424 (.30) 365.5 367.7 z4 0.05458 (.26) 362.3 366.8 z5 0.05419 (.27) 364.6 366.5 z6 0.05422 (.25) 352.3 356.1 z7 0.05636 (2.02) 280.7 301.6 z8 0.05343 (3.55) 271.9 279.9 z9 0.05536 (3.52) 262.3 279.6 z10 0.05466 (2.96) 170.7 187.0 Ages (MA) Frac. Total & [sup.207]Pb Corr. common no. * [sup.206]Pb coef. Pb(pg) G1 megacrystic granite z1 393.7 0.772 2.1 z2 396.0 0.845 1.9 z3 393.8 0.774 3.9 z4 393.3 0.760 2.4 G2 megacrystic granite z2 400.4 0.870 1.4 z3 402.9 0.903 2.8 G3 diorite enclave z1 397.1 0.760 4.2 z2 424.9 0.913 2.8 z3 396.9 0.944 1.4 z4 407.0 0.852 1.6 G4 magma mingling zone granodiorite z1 398.8 0.839 1.7 z2 413.4 0.910 3.4 z3 418.8 0.867 1.5 z4 406.1 0.773 2.8 G5 Costelloe Murvey Granite z1 379.2 0.864 2.2 z2 380.4 0.637 3.4 z3 381.1 0.887 5.6 z4 395.0 0.924 9.2 z5 379.0 0.601 3.1 z6 380.3 0.982 7.9 z7 466.5 0.386 240 z8 347.3 0.247 130 z9 427.0 0.344 130 z10 398.2 0.531 410 * All fractions are single grain analyses. ([dagger]) Radiogenic Pb. ([section]) Measured ratio corrected for fractionation only. All Pb isotope ratios were corrected for mass fractionation using 0.18%/amu. ([paragraph]) Corrected for fractionation, spike, blank, and initial common Pb. Common Pb correctios were made using Stacey and Kramers (1975) initial Pb. Sample processing and U and Pb separation were performed at the University of North Carolina--Chapel Hill (UNC). Analysis was accomplished with a VG Sector 54 thermal ionization mass spectrometer at the UNC. Conventional separation techniques (ie., water table, heavy liquids, magnetic) were used. Grains were separated using a Frantz Isodynamic LB-1 magnetic separator. All fractions were handpicked by color, size, and morphology. Zircon fractions were air abraded (Krogh 1982). Dissolution and isolation of U and Pb followed the methods of Krogh (1973) and Parrish (1987). All fractions were spiked with a mixed [sup.205]Pb-[sup.233]U-[sup.236]U spike. Purified Pb and U fractions were loaded on single Re filaments with silica gel and graphite, respectively. Decay constant used are [sup.238]U = 0.15513 x [10.sup.-9] [yr.sup.-1], and [sup.235]U = 0.98485 x [10.sup.-9][yr.sup.-1] (Steiger and Jager 1977). Weights are estimated using a video camera and scale, and are known to within 10%. Data reduction and error analysis was accomplished using the PbMacDat-2 by D.S. coleman, using the algorithms of Ludwig (1989, 1990) and all errors are reported in percent at the 2[sigma] confidence interval. Table 2. Tabulation of age determinations presented in the text. Granite Geological setting Megacrystic Granite (G1) Central Block Megacrystic Granite (G2) Central Block Enclave (G3) Central Block MMZ Granodiorite (G4) Central Block Costelloe Murvey Granite (G5) Central Block Molybdenite bearing Hosted by Carna Granite; quartz veins Western Block. Disseminated molybdenite Hosted by Murvey Granite; Western Block Disseminated molybdenite Hosted by Murvey Granite; Western Block Carna Granite Western Block Errisbeg Townland and Murvey Granite Western Block Granite Method Megacrystic Granite (G1) U-Pb Single crystal (zircon) Megacrystic Granite (G2) U-Pb Single crystal (zircon) Enclave (G3) U-Pb Single crystal (zircon) MMZ Granodiorite (G4) U-Pb Single crystal (zircon) Costelloe Murvey Granite (G5) U-Pb Single crystal (zircon) Molybdenite bearing quartz veins Re-Os Molydenite Disseminated molybdenite Re-Os Molydenite Disseminated mol y bdenite Re-Os Molydenite Carna Granite U-Pb Bulk zircon Errisbeg Townland and Murvey Granite Rb-Sr wholerock Granite Age Megacrystic Granite (G1) 394.4 [+ or -] 2.2 Ma. (1) Megacrystic Granite (G2) ~402 Ma. (1) Enclave (G3) 397.7 [+ or -] 1.1 Ma. (1) MMZ Granodiorite (G4) 399.5 [+ or -] 0.8 Ma. (1) Costelloe Murvey Granite (G5) 380.1 [+ or -] 5.5 Ma. (1) Molybdenite bearing quartz veins 407.3 [+ or -] 1.5 Ma. (1) Disseminated molybdenite 410.5 [+ or -] 1.5 Ma. (1) Disseminated mol y bdenite 410.8 [+ or -] 1.4 Ma. (1) Carna Granite 412 [+ or -] 15 Ma. (3) Errisbeg Townland and Murvey Granite 398 [+ or -] 10 Ma. (4) Sources: (1) this study, (2) Selby et al. (in press), (3) Pigeon (1969) and (4) Leggo et al. (1966).
The authors wish to acknowledge funding from Enterprise Ireland under the International Collaboration Programme 2002--Grant No IC/2002/013. The authors wish to acknowledge the reviewers David Gibson and Dan Lux for their critical and constructive comments on the manuscript.
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Editorial responsibility: David Gibson
MARTIN FEELY (1), DREW COLEMAN (2), SADHBH BAXTER (1), AND BRENT MILLER (2)
(1.) Department of Earth and Ocean Sciences, National University of Ireland, Galway, Ireland.
(2.) Department of Geological Sciences, University of North Carolina, Chapel Hill, NC 27599-3315 USA.
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|Author:||Feely, Martin; Coleman, Drew; Baxter, Sadhbh; Miller, Brent|
|Date:||Jul 1, 2003|
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