The Christmas Cove Dyke of coastal Maine, USA, and regional sources for Early Mesozoic flood basalts in northeastern North America.
A large Early Mesozoic quartz tholeiite dyke has been mapped discontinuously for 190 km in southern coastal Maine, USA. Including its type locality at Christmas Cove (South Bristol, Maine, USA), the dyke has features of a generally ENE strike; dip usually steep to the SSE but abruptly turning very shallow in short sections; and widths of 9 to 35 m. The dyke rock has a distinctive cross-columnar field appearance, and a subophitic to micro-porphyritic texture with abundant Ti-bearing augite, calcic plagioclase, scattered euhedral orthopyroxene phenocrysts, and coarse-grained glomerophyric clumps of augite with plagioclase. Several [sup.40]Ar/[sup.39]Ar whole- rock dates for this and associated regional dykes are close to 201 Ma, in agreement with ages of other Early Mesozoic dykes and basalts of the Central Atlantic Magmatic Province (CAMP). The geographic position, age, wholerock chemistry, and petrography indicate that the Christmas Cove Dyke is co-magmatic or contiguous with the Higganum-Holden Dyke of southern New England, which was a source for the Talcott Basalt of the Early Mesozoic Hartford rift basin. The dyke system is a 700-km long fissure source for the earliest rift basin basalts preserved in northeastern North America, and it virtually connects the Hartford Basin and the Fundy Basin in Atlantic Canada. The Caraquet Dyke of New Brunswick and central Maine may be co-magmatic with the Buttress Dyke and Holyoke Basalt of southern New England, but lava from it is not preserved in Atlantic Canada or Maine.
Un grand dyke de tholeiite remontant a lere Mesozo'ique precoce a ete cartographie de facon discontinue sur 190 km sur la cote du Sud du Maine, aux Etats-Unis. En plus de sa localite type a Christmas Cove (South Bristol, Maine, E.-U.), le dyke possede comme caracteristiques une direction generale E.-N.-E., une descente habituellement raide vers le S.-S.-E. devenant abruptement tres peu profonde sur de courtes sections et une largeur variant entre 9 et 35 m. La roche du dyke presente une prismation horizontale particuliere et une texture variant de subophitique a microporphyrique abondante en augite contenant du titane, en plagioclase calcique, en phenocristaux dbrthopyroxene idiomorphes disperses et en amas d'augite glomerophyrique granuleuse avec feldspath plagioclase. Plusieurs dates obtenues par la methode [sup.40]Ar/[sup.39]Ar sur roche totale de ce dyke et d'autres dykes lies de la meme region s'approchent des 201 Ma, ce qui correspond a lage d'autres dykes de lere Mesozoique precoce et du basalte de la province magmatique centre atlantique (PMCA). La position geographique, lage, la chimie sur roche totale et la petrographie indiquent que le dyke de Christmas Cove est comagmatique ou contigu a celui de Higganum-Holden du Sud de la Nouvelle-Angleterre, qui etait rune des sources du basalte de la montagne Talcott du bassin d'effondrement Hartford de lere Mesozoique precoce. Le reseau de dykes est une fissure d'une longueur de 700 km qui serait la source la plus ancienne de basalte de bassin d'effondrement preservee au Nord-Est de l'Amerique du Nord, et il relie pratiquement le bassin Hartford et le bassin Fundy du Canada atlantique. Le dyke de Caraquet du Nouveau-Brunswick et du centre du Maine pourrait etre comagmatique au dyke Buttress et au basalte de la chaine Holyoke du Sud de la Nouvelle-Angleterre, mais aucune lave provenant de ce dyke n'est preservee au Canada atlantique ou au Maine.
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Flood basalt provinces are typically derived from fissure eruptions that produce large volumes of tholeiite over brief time spans, with fluid pahoehoe-type lavas that can flow for great distances (Self et al. 1997; Swanson et al. 1975). Feeder dykes rise through the lithospheric mantle beneath the fissures and are exposed after overlying basalt has been removed by later uplift and erosion, so the connection of particular source dykes with remaining flood basalts may no longer be obvious (McHone 1996). However, regional studies combining field, petrologic, geochemical, and geochronological data have the potential to reveal dykelava flow links, as has been demonstrated for the Early Mesozoic Hartford Basin (Philpotts and Martello 1986) and the Columbia River Basalt Group (Swanson et al. 1975). The Christmas Cove Dyke of coastal Maine is a large intrusion of quartz tholeiite that extends between Early Mesozoic riff basins in New England and Atlantic Canada, and as we will show, appears to be co-magmatic with their Late Triassic flood basalts.
The Christmas Cove Dyke was first mapped and described at Harpswell Neck (Hussey 1971), and later in the Portland and Bath 1:100 000-scale bedrock quadrangle maps in northern Casco Bay, Maine (Berry and Hussey 1998; Hussey and Marvinney 2002). Figure 1 shows the general location of the dyke, but the bedrock geologic maps referred to above provide greater detail for the interested reader. The dyke was briefly described at Christmas Cove in South Bristol by Bascom (1899) although she did not trace it beyond that area. At most locations the dyke trends toward its next exposure, but it is not particularly linear (Fig. 1). Distinctive macroscopic and field features are consistent along its great length and distinguish the dyke from numerous older basaltic intrusions of Maine. The Christmas Cove Dyke may continue far to the northeast as well as southwest, but outcrops along its trend are generally poor, and a detailed magnetic survey may be required to trace its full extent.
We also sampled the Caraquet Dyke (Greenough and Papezik 1986) that extends a minimum of 470 km across New Brunswick (Burke et al. 1973) and into central Maine at least to Macwahoc (Boucot et al. 1964), as located by its distinct and linear aeromagnetic anomaly. Late Triassic to Early Jurassic tholeiitic dykes and basin flood basalts in the region are located in Figure 2.
Our main purpose is to describe the locations, petrography, whole-rock chemistry, and age of the Christmas Cove Dyke, and to compare it to previously described tholeiitic dykes and basalts in the region. Large dykes are sources for basalts in Early Mesozoic riff basins, and they could have produced extensive flows outside of the basins as well (McHone 1996). Petrography, geochemistry, and whole-rock [sup.40]Ar/[sup.39]Ar radiometric ages can support these genetic links. The spatial distribution of the Christmas Cove and other regional dykes, along with their correlation with basalts in the basins (Fig. 2), provide information about the origin, extent, and timing of major volcanic events of the Central Atlantic Magmatic Province, some of which may be linked to the mass extinction near the Triassic-Jurassic boundary (Schoene et al. 2010; Blackburn et al. 2013).
We visited outcrops of the Christmas Cove Dyke as located by several students and field geologists, by maps by the Maine Geological Survey cited above, and by our own field work. Locations not previously mapped are in a small road cut along Rte. 202/4 at Waterboro, in spectacular shoreline exposures at Whitehead Island (de Boer et al. 2003) and Swans Island (Perry 1994), and as a few outcrops on isolated islands (e.g., Barter Island) found via air photographs and Google Earth. The dyke generally parallels the coastline, crossing much open water in bays and cropping out at shorelines of peninsulas and islands (Fig. 1). Field visits and data collection have been underway by the authors for several decades (Hussey 1971; McHone 1984, 1993; West and McHone 1997) by searching and visiting locations, and conducting thin-section petrography, geochronological studies, and whole-rock chemical analyses. Jelle de Boer and Andrew Lindsey visited several of the same locations to obtain oriented drill cores for a paleomagnetic study of flow direction (de Boer et al. 2003). [sup.40]Ar/[sup.39]Ar radiometric ages were determined using samples from three locations along the Christmas Cove Dyke, as well as single samples from the Caraquet Dyke near Bancroft, Maine, and the Higganum Dyke at Hurd State Park in Haddam, Connecticut.
Field observations at 13 locations of the Christmas Cove Dyke are summarized in Table 1. The dyke is recognized by its massive but jointed appearance with rusty to grey weathered surfaces and uniform darker fresh surfaces, not greenish or slightly foliated as are many older dykes in Maine. At 13 to 35 m wide, it is much larger than most of the basaltic dykes that are common in southern Maine, some of which represent other post-metamorphic igneous provinces and events as summarized by McHone (1992) and McHone and Sundeen (1995). In addition, the Christmas Cove Dyke commonly exhibits large polygonal cooling columns 0.4-1.0 m in diameter and perpendicular to the dyke walls (Fig. 3). Joints parallel and perpendicular to the walls are common, and at some locations they promote erosion and useful interior exposures.
In general, the dyke is as durable as the surrounding metamorphic and plutonic rocks, so that it does not form large ridges or troughs from differential erosion except very locally. Outcrops are mainly coincidental with the removal of surficial cover by coastal wave erosion or road construction. A few inland hillside exposures, as at Phippsburg, are apparently due to glacial erosion. Probably the dyke exists between most outcrops under the sea or surficial materials, and it might be tracked by a suitable aeromagnetic survey as indicated by its sharp magnetic anomaly with a hand-held magnetometer. A few gaps along the dyke are due to offsets by faulting, en-echelon segments, or pinch-out structures. In most cases, the general strike of each exposed section of the dyke trends toward the next outcrop along the coast.
Areas where the dyke deviates significantly from its circa-075 general trend are found at its western and eastern locations, and from Harpswell Neck to Phippsburg (Table 1 and Fig. 1). At its westernmost outcrop in Waterboro, the dyke appears to trend to the southwest and toward the Onway Dyke exposures in southeast New Hampshire (Sundeen and Huff 1992). At its exposure on Swans Island, the dyke has turned more northeasterly toward the southern part of Mt. Desert Island (a possibly location is reported near Bass Harbor Light), but it has not been identified on current bedrock maps in Maine from Mt. Desert Island to Eastport, where we suspect it might continue as the Lepreau River Dyke (Fig. 2; S. Barr personal communication, 2013). Large gaps in mapped dyke locations are in areas of poor outcrop between Cumberland Foreside and Waterboro, Maine, and from Waterboro into New Hampshire. The dyke also trends into a mostly water-covered area toward the southern part of Vinalhaven and through the island archipelago south of Stonington, but without reports of its occurrence (Fig. 1).
The dyke and potential extensions into southern New England and New Brunswick cross faults and structures within Ganderian crustal belts southeast of the Norumbega fault zone (West et al. 2008). The dyke intrudes rocks of the Ellsworth, Mascarene, and St. Croix terranes in Maine (Merrimack and coastal lithotectonic blocks of Osberg et al. 1985), as well as through Silurian to Devonian granitic plutons. In the Casco Bay area the dyke crosses the Flying Point Fault with no apparent offset, although the fault had approximately 4 km of west-side-up displacement in post-Paleozoic time (West et al. 1993). Because the dyke intruded without regard to major upper crustal structures, its path may have initiated in the lower lithosphere along a pre-existing zone of weakness and then propagated both vertically and laterally through the brittle upper crust in a direction consistent with the regional stress field (McHone 1988).
In detail, however, it is clear that small faults and intrusional offsets in boundaries along the dyke are common at the current level of exposure. Sharp steps and offsets of the dyke of a few centimetres to several metres are present at Doyle Point, Harpswell Neck, Phippsburg, and Whitehead Island (Fig. 3). The steps follow high-angle metamorphic and plutonic foliations as well as brittle fractures. In nearly all cases the offsets are in a left-lateral sense along strike. This is the same offset direction shown by en-echelon steps of the Higganum Dyke in Connecticut (Rodgers 1985), which as discussed later is probably part of the same dyke system. Presumably, extensional stress at this level was not quite normal to many dyke segments but was slightly more to the NW-SE, so that the overall direction of the dyke path is a little more NE-SW than individual segments (McHone 1988).
The Caraquet Dyke is exposed on the northwest side of the Mattawamkeag River at the western town line of Bancroft, off Pitloc Road about 4 km from Rte. 171 in Maine. The dyke is at least 15 m wide, strikes 074, and dips nearly vertically (only the northern side is exposed). A left-lateral fault in the northern contact has an offset of 1.2 m. Fresh surfaces are dark grey, fine-grained, dense, hard, and unaltered.
In summary, Christmas Cove Dyke exposures are generally excellent but intermittent. Field characteristics include its large size, prominent columns, lack of alteration, and continuity along its trend. As we discuss, the observed length of 190 km in Maine is only part of a much longer dyke system between southern New England, USA, and southern New Brunswick, Canada.
Petrographic thin sections are dominated by anhedral Ca-rich augite and subhedral to euhedral calcic plagioclase laths in a subophitic
texture (Fig. 4). Grain sizes vary from a few tenths mm to 2 mm or more from contacts toward centers (fine- to medium-grained). Both sulfides and iron oxides are common but have few crystal faces. Patches of fine-grained granophyric feldspar and quartz in central areas of the dyke usually show elongated needles of apatite. Felsic granophyres in the North Mountain Basalt are ascribed to liquid immiscibility by Kontak et al. (2002) and may have a similar origin in their feeder dykes, but we have not made particular studies or analyses of the material. Small brown-green, pleochroic grains are hornblendes with variable compositions, and a few small biotite grains appear around some augite rims, but in general the rock is fresh and unaltered.
The dyke is everywhere porphyritic with abundant euhedral to subhedral orthopyroxene crystals several mm or more in length (Figs. 4 and 5). The orthopyroxene commonly shows good crystal outlines but can be corroded, with interior holes or ragged edges, and rims of magnetite and/ or small grains of pigeonite. Clumps or clusters of mediumto coarse-grained augite are also common, typically with coarse plagioclase laths in a glomeroporphyritic texture. The clusters range from a few mm to many cm in size, and larger pieces can be visible on smooth surfaces of the dyke as well as filling thin sections (Fig. 5). Individual coarse grains of clinopyroxene and plagioclase in the dyke may be from these clusters, which are often partly disaggregated. At Spruce Point the clusters occur as streamlined inclusions up to 20 cm long and are visible on glacially smoothed surfaces (Fig. 3).
Thin sections of dyke contacts show microporphyritic crystals of plagioclase, augite, and orthopyroxene scattered in a dark glassy matrix (Fig. 5). The small clusters of coarse pyroxene and plagioclase are also found near contacts, including individual large rounded grains of augite. At Doyle Point the contact with granitic wall rock has a thin layer of brown melted silicic material, which is also streaming in thin bands into the dyke with its flow direction (Fig. 5). Contamination of the original dyke magma by wallrock melting and disaggregation may be locally significant, as reported for the Higganum Dyke by Philpotts and Asher (1993), although in a petrogenetic study of the similar Ministers Island Dyke, Dunn and Stringer (1990) calculated contamination as less than a few percent. Perry (1994) came to the same conclusion with the Swans Island dyke section. Despite visual evidence of granitic "wisps" along the margin of the dyke, contamination (at least at the exposed crustal level) was apparently quite limited.
We did not conduct a detailed investigation into mineral chemistry except for SEM/EDS analyses of some plagioclase and pyroxene phenocrysts in a sample of the dyke at Swans Island, which are presented in Appendix A. Figure 6 shows ternary plots of these compositions. Enstatite (var. bronzite ~[Wo.sub.5][En.sub.78][Fs.sub.17]) and augite (~[Wo.sub.35][En.sub.54][Fs.sub.11]) show little variation between cores and rims, with tightly grouped clusters. Plagioclase phenocrysts (bytownite or labradorite; [An.sub.64-72]) have rims that are both similar to, and more sodic than, the calcic cores, with some solid solution variation within the cluster. The Caraquet Dyke lacks orthopyroxene but may contain more pigeonite than the Christmas Cove Dyke and related tholeiites, as well as olivine in the matrix (Greenough and Papezik 1986). Fields for pyroxenes from the Caraquet and Shelburne dykes are included in Figure 6 for comparison. Pigeonite (but no olivine) exists in the Christmas Cove Dyke as well, but it was not analyzed in this study.
We selected 19 samples for whole-rock chemical analyses (Tables 2 and 3), including single samples from related dykes in Connecticut and New Hampshire, seven samples along the Christmas Cove Dyke in Maine, a sample from the Caraquet Dyke at Bancroft, Maine, and nine samples roughly evenly spaced across the dyke at its excellent shoreline exposure on Swans Island. The single samples were fresh-appearing pieces broken from the interior or about a third of the width into the dyke from a contact (where one was visible). Most samples were analyzed by wavelength dispersive X-ray fluorescence spectrometry at Hamilton College and the University of Connecticut. Rock samples were cleaned, crushed, and pulverized in a tungsten carbide ring mill. The rock powders were ignited, and then fluxed with Li-tetraborate and fused into glass disks. Analyses were run against calibration curves defined using 12 USGS standards, 10 international standards, and 10 in-house standards. Precision and accuracy of the analyses were estimated by comparing the results of multiple analyses of USGS standard G-2 run as an unknown during the analytical period to published accepted values for this standard. Trace element samples in Table 2 that include rare earth elements are analyzed by ICP by Activation Laboratories Ltd.
The whole-rock chemical analyses are presented in Table 2. Only very minor differences are evident among the compositions of dyke samples from Hurd State Park (Connecticut) through New Hampshire to Swans Island (Maine). The dyke system is remarkably uniform both petrographically and chemically along its great length, with small variations possibly related to fractionation of orthopyroxene phenocrysts as well as minor assimilation of wall rocks, as also observed by Dorais et al. (2005) at Onway, and Dunn and Stringer (1990) at Ministers Island.
The complete Swans Island exposure allowed us to analyze a series of samples across the dyke, roughly evenly spaced, to search for possible compositional differences from flow fractionation or multiple magma intrusions (Table 3). Across the dyke, chemical differences are small and nonsystematic except for slightly higher MgO and lower Ti[O.sub.2] concentrations in the interior of the dyke relative to the outer margins. The small compositional differences can largely be explained (and numerically modelled) by slight variations in phenocryst populations; relatively large variations in concentrations in some of the LIL elements (e.g., Rb, Ba, and Sr) seen in some samples are apparently due to alteration and weathering (Table 3, analysis lh). Overall, the Swans Island dyke is remarkably uniform in composition considering it is 35 m wide and was carrying a fairly high phenocryst load. Flowage differentiation and in-situ differentiation played only minor roles in modifying bulk rock compositions, probably in part due to the turbulent flow of this large dyke that kept it mixed and relatively uniform in composition.
Plots of the chemical analyses show the minor fractionation of the dyke magma both along its length and across its width (Fig. 7). The dyke has a tholeiitic composition with only slight variation in MgO/Fe[O.sub.total] ratios and alkali enrichment (Irvine and Baragar 1971), which is probably related to removal or addition of Mg-rich pyroxene and plagioclase phenocrysts and glomerophyric clumps (Figs. 4 and 5). Compositions are generally in the basaltic andesite field of LeBas et al. (1986) but overlap into true basalt, as is common for quartz tholeiite derived from sub-continental lithospheric mantle (Dorais et al. 2005). Rare earth elements normalized to chondrite (Sun and McDonough 1989) have relatively flat patterns with [(La/Lu).sub.N] ratios about 3.0 to 7.5 (Fig. 7b). Although the ratio lines for analyses from the Christmas Cove, Onway, and Hurd Park dykes are the same within analytical error, they are distinct from REE patterns for the Caraquet, Shelburne, and other dyke magmas (Dunn et al. 1998; Dostal and Durning 1998; Dorais et al. 2005).
Typical of most northern Central Atlantic Magmatic Province (CAMP) magmas, the dykes analyzed are all quartz tholeiites (Fig. 7a). In particular, the whole-rock chemical composition of the Christmas Cove Dyke is within the HTQ or "high-titanium quartz" normative tholeiite group of Weigand and Ragland (1970), who made a pioneering study of groups or magmatic types of Early Mesozoic dykes and basalts in eastern North America. This type is also found throughout most of the CAMP and it is thought to represent the oldest or initial magmatic event, now known to be mainly latest Triassic in age (Jourdan et al. 2009; Cirilli et al. 2009; Deenen et al. 2010). Two subsequent (Early Jurassic) types of quartz-normative tholeiites are labelled LTQ ("low titanium quartz") tholeiite, and HFQ ("high-iron quartz") tholeiite. The three types correspond to three dyke-to-basalt flow systems in southern New England that respectively are: Higganum-Holden Dyke to Talcott Basalt; Buttress-Ware Dyke to Holyoke Basalt; and Bridgeport-Pelham Dyke to Hampden Basalt (Fig. 8; Philpotts and Martello 1986).
The MgO vs. Ti02 diagram by Philpotts and Martello (1986, their fig. 3) illustrates the petrogenetic connections among three source dykes and three basalts of the Hartford Basin in southern New England (Fig. 8). Co-genetic dyke and basalt compositions fall along particular linear trends that are mainly from pyroxene fractionation, as has been confirmed with additional analyses in later studies by Puffer (1992), McHone (1996), and Jourdan et al. (2009). In particular, Philpotts and Martello (1986) show that the Higganum dyke and the co-magmatic Fairhaven Dyke (separated by faulting) are the source for the Talcott Basalt, the earliest basalt of the basin. Superimposed on this diagram (Fig. 8), our dyke analyses show a good match of the Christmas Cove Dyke and the co-linear Onway Dyke with the Higganum/Fairhaven Dyke (including our sample from Hurd State Park). The Caraquet Dyke at Bancroft is also a match for the Buttress-Ware Dyke of southern New England, which is the source of the Holyoke Basalt.
In summary, whole-rock chemistry of the Christmas Cove dyke shows it to be essentially identical to the composition of the Ministers Island Dyke of New Brunswick, the Onway Dyke of New Hampshire and the Higganum-Holden Dyke of Connecticut and Massachusetts. The Caraquet Dyke including its locality at Bancroft has the same composition as the Buttress-Ware Dyke of southern New England. Their segments are geographically co-linear (with some wide gaps between exposures) and appear to share the same petrogenesis, and so both are considered to be co-magmatic intrusions. As will be discussed, separate dyke systems are derived from specific mantle sources with depths, temperatures, and enriched compositions that are distinct, producing magmas that vary from very similar to quite different across large areas of the CAMP (Tollo and Gottfried 1986; McHone 1996; Dorais et al. 2005).
RADIOMETRIC AGES AND CORRELATIONS
Previously published radiometric dates for regional dykes and basalts (Table 4) show a wide range of precision and accuracy using K/Ar and [sup.40]Ar/[sup.59]Ar methods. As presented by West and McHone (1997) and detailed herein, we have obtained additional whole-rock [sup.40]Ar/[sup.39]Ar dates using samples of freshest-available dolerite from dyke exposures at Christmas Cove (South Bristol, Maine), Spruce Point (Boothbay Harbor), and Doyle Point (Yarmouth); the Caraquet Dyke on the NW side of the Mattawamkeag River near Bancroft, Maine; and the Higganum Dyke in a road cut in Hurd State Park near Haddam, Connecticut. Obviously weathered and altered areas in the samples were removed before crushing. [sup.40]Ar/[sup.39]Ar radiometric analyses were performed on whole-rock samples of crushed splits at the radiometric laboratory at the University of Maine, following standard methods outlined in West et al. (1993).
The three samples from the Christmas Cove Dyke (DP-1, MR-1, SP-1), one sample from the Caraquet Dyke (Ban-1), and one sample from the Higganum Dyke (HPK1) were analyzed as whole rock samples using the [sup.40]Ar/[sup.39]Ar incremental heating technique (7 heating steps in each sample). Analytical results of these experiments and the laboratory procedures employed are provided in Appendix B. Release spectra diagrams are shown in Figure 9, and results are discussed below.
A single sample of the Caraquet Dyke collected near Bancroft, Maine yielded an essentially concordant age spectrum with total gas (201.7 Ma), plateau (201.2 Ma), and isotope correlation (201.8 Ma) ages all agreeing within analytical uncertainties. Release spectra (Fig. 9a) and isotope correlation (not shown) diagrams reveal no signs of excess [sup.40]Ar contamination or [sup.40]Ar loss. Based on these uncomplicated results, we interpret Caraquet dyke emplacement to have occurred at 201.5 [+ or -] 2.4 Ma (the average of the total gas, plateau, and isotope correlation ages).
A single sample of the Higganum Dyke collected from central Connecticut yielded a slightly discordant spectrum (Fig. 9b) with plateau (201.7 Ma) and isotope correlation (200.2 Ma) ages slightly younger than the total gas age (204.6 Ma). Both the "saddle shape" of the age spectrum and the [sup.40]Ar/[sup.36]Ar intercept (315 versus the current atmospheric value of 295.5) on the isotope correlation diagram (not shown) suggests a small amount of excess [sup.40]Ar contamination which would explain the slightly older total gas age. The age of emplacement of the Higganum Dyke is therefore taken to be 201.2 [+ or -] 2.8 Ma which is the average of the plateau and isotope correlation ages.
Christmas Cove Dyke
Three samples of the Christmas Cove dyke (DP-1, MR-1, SP-1), each collected from a different locality, were analyzed and yielded variably discordant age spectrum. Both samples MR-1 (Fig. 9d) and SP-1 (Fig. 9e) have highly discordant age spectra (both somewhat "saddle shaped") that suggest complex argon systematics in these whole rock samples. MR-1 displays ages (total gas, isotope correlation, weighted average age) that are consistently 10 to 15 Ma older than the ages from sample SP-1. Given the complicated argon systematics suggested by these results, and that these two samples are from the same dyke and should yield the same age, we will refrain from making any estimates of the timing of Christmas Cove Dyke emplacement based on the data from these two samples.
DP-1 (Fig. 9c) shows the least discordance of the three Christmas Cove Dyke samples and we prefer to base our emplacement age estimate on the results from this sample. While not as discordant as MR-1 and SP-1, individual apparent ages from consecutive increments in DP-1 are still too dissimilar to calculate a plateau age by the strict criteria of Fleck et al. (1977). However, a weighted average age of 203.1 Ma for four consecutive increments of similar age (61% of [sup.39]Ar released) is in close agreement with the isotope correlation age (203.6 [+ or -] 2.6 Ma) from this sample. The total gas age of this sample (205.3 Ma) is slightly older than these two ages due primarily to a large final age increment (22% of total 39Ar released) that has an older apparent age (209.1 Ma). Based on these results, we tentatively interpret the emplacement age of the Christmas Cove dyke to be the isotope correlation age of 203.6 [+ or -] 2.6 Ma.
In summary, we interpret our [sup.40]Ar/[sup.39]Ar results to indicate the Caraquet Dyke was emplaced at 201.5 [+ or -] 2.4 Ma, the Higganum dyke emplaced at 201.2 [+ or -] 2.8 Ma, and while complex argon systematics render this interpretation less certain, the Christmas Cove was emplaced at 203.6 [+ or -] 2.6 Ma. When the analytical uncertainties of each of these ages are considered, all overlap, and the argon data are consistent with our interpretation that all three were emplaced at around the same time. These dates are generally close to recent [sup.40]Ar/[sup.39]Ar and U-Pb dates for other dykes and basalts assigned to the CAMP in the New England-Maritimes region, as summarized in Table 4.
Petrogenetic studies using trace elements and isotopes have been performed for the Ministers Island Dyke of southern New Brunswick (Dunn and Stringer 1990), the Onway Dyke of southern New Hampshire (Dorais et al. 2005), and the Higganum Dyke of southern New England (Philpotts and Martello 1986). In addition to field mapping and descriptive petrology, our petrographic and whole-rock chemical analyses, with support from radiometric dates, show that these regional dykes are probably co-magmatic with the Christmas Cove Dyke and are members of the same dyke system, which represents the source of the initial tholeiitic flood basalts in Early Mesozoic rift basins (Fig. 8 and Table 4).
Analyses of minerals and isotope chemistry from other studies of correlated dykes are equally applicable to the Christmas Cove Dyke and we have not repeated that work. Essentially the dyke magma is found to be derived from the lower lithospheric mantle after a past enrichment event involving subduction of crustal materials into the source region, as discussed by Dostal and Durning (1998) and Murphy et al. (2011) for the Atlantic Canada region, by Pegram (1990) for the greater area of eastern North American basalts, and by Puffer (2003) for the entire Central Atlantic Magmatic Province. In addition, Murphy et al. (2011) argue that mantle sources for basalts in Atlantic Canada are essentially unchanged since the Neoproterozoic. Consequently, long-distance horizontal transport of magma from other mantle sources, or generation of magma from deep-mantle plumes is unlikely since over time both would have resulted in chemical and isotopic variations that are not observed. McHone (2000) discussed additional reasons why magmatism related to the opening of the North Atlantic Ocean is not explained by a deep mantle plume model. A similar conclusion is based on a more comprehensive study of isotopic and trace elements in the northeastern North American CAMP by Renaud et al. (2014), who see no evidence or requirement for a central deep-mantle plume source.
Many attempts have been made to derive the different tholeiites of regional dykes and basins from one or more "parent" magmas, or from each other (Weigand and Ragland 1970; Dostal and Durning 1998). Models that have been proposed include various combinations of fractional crystallization in sub-crustal magma chambers, flow differentiation in dykes and lavas, contamination by crustal wall rocks, and a filter-pressed crystal lattice mechanism (Kontak 2008). Each of these models has support from observations and experiments on samples from individual dykes or flows, but there continues to be little direct evidence to link all of the different dyke and lava systems to a common magma parent. In contrast, many studies show that at least some magma types cannot be related through reasonable differentiation processes (e.g., Tollo and Gottfried 1989; Dorais et al. 2005). There is also no physical evidence such as large plutons that might represent chambers in which these basalts could fractionate within the crust. Yet, levels of Mg and other chemical components in each dyke system show that these magmas have evolved far from any melts in equilibrium with olivine-rich mantle sources. In addition, the CAMP magmas are mantle melts that formed close to one another in time and space, although they physically overlap in northeastern North America only as lava flows within Mesozoic basins.
Tollo and Gottfried (1986) and McHone (1996) concluded from petrochemical and geographical arguments that the different groups of basaltic rocks are not derived from a common magma by differentiation, but rather each represents a distinct mantle source and/or melting event. Magma types present in dykes and basalts are very similar in widely separated areas of eastern North America and the CAMP, as well as being uniform for hundreds of kilometres along individual dykes. It is too unlikely that variable fractionation and crustal contamination of individual magmas derived from several magma chambers at depth would allow them to match so perfectly, and one such chamber is not a reasonable source for different dykes forming across such great distances in a heterogeneous mantle. Instead, similar melts may be derived from specific layers or horizons of similar mantle compositions at similar depths and temperatures (Meibom et al. 2002). The dyke magmas intruded fractures that propagated both vertically to the surface and horizontally, according to extensional stresses in the lower lithosphere as well as buoyancy pressures. Upper crustal features, including basin faults and terrane boundaries, show little influence over the greater dyke locations and paths, except at a very local and minor scale.
SIGNIFICANCE AS A FLOOD BASALT SOURCE
The Talcott Basalt of the Hartford Basin has a similar lithostratigraphy and close petrological correlation with the very large North Mountain Basalt of the Fundy Basin between New Brunswick and Nova Scotia, Canada (McHone 1996; Olsen 1997). The western side of the Fundy Basin is near the Ministers Island Dyke (Fig. 2), which we find to be petrologically similar to the Christmas Cove Dyke, but because of its relatively small size the Ministers Island Dyke has been discounted as a reasonable source for the North Mountain Basalt in several studies (Wade et al. 1996; PePiper and Piper 1999; Kontak 2008). However, the much larger Lepreau River Dyke has been subsequently mapped and could add to the similar Ministers Island Dyke for producing the Fundy Basin basalts, and a correlation with the Christmas Cove Dyke is also reasonable (McHone 2011; McHone and Barr 2003). In that case, the Christmas Cove Dyke (and possible continuity with the Lepreau River Dyke) represents a physical connection between the Hartford and Fundy basins and a co-magmatic source for the Late Triassic flood basalts.
A correlation of source dykes with their flood basalt products in the Hartford and Fundy basins (Philpotts and Martello 1986) places them into a detailed chrono-stratigraphic sequence based on Milankovitch cyclostratigraphy (Olsen 1997), which indicates the Christmas Cove--Higganum dyke system is older by about 300,000 years than the Caraquet--Buttress dyke system. Moreover, there is a younger-to-older intrusional sequence of west-to-east for the three large dyke systems of southern New England. As we have shown, the Buttress-Caraquet and Higganum-Christmas Cove dyke systems continue into northern New England and New Brunswick, where they turn more eastward and diverge along their trends (Fig. 2).
Several hundred kilometres to the east of the Christmas Cove Dyke is the Shelburne Dyke of Nova Scotia, which is a very large intrusion that extends into the eastern Gulf of Maine but does not appear in New England (Fig. 2; Papezik and Barr 1981). As observed by Pe-Piper and Piper (1999) and Kontak (2008), lavas derived from the Shelburne dyke have not been recognized in the Fundy Basin. The large Late Paleozoic South Mountain batholith of southern Nova Scotia could have presented a topographic barrier between the basin and the Shelburne dyke in Early Mesozoic time (it remains a high area today), so that Shelburne lavas did not flow into areas that are currently exposed. Such lavas may instead be preserved in submarine basins south and east of Nova Scotia (Hutchinson et al. 1988). If the west-to-east progression of younger to older ages continues into this region (Fig. 2), the Shelburne Dyke could be older than the Christmas Cove Dyke. Support for an older age has been presented by Dunn et al. (1998), who reported a [sup.40]Ar/[sup.39]Ar age of 203 [+ or -] 2 Ma for both the Shelburne dyke and the Messejana dyke system of Spain and Portugal. They regarded both dykes as essentially co-magmatic, if not formerly connected. An older age also suggests the possibility that the Shelburne-Messejana magmatic event may precede or be synchronous with the end-Triassic mass extinction (ages detailed by Blackburn et al. 2013).
In addition to assisting to map portions of the same dyke set along a great distance, the bulk chemistry of different generations of dykes can be used to correlate them with other Central Atlantic Magmatic Province basalts preserved within Early Mesozoic rift basins (Table 5).
As we relate, the Higganum-Christmas Cove dyke system is exposed for about 700 km from Long Island Sound to the western Gulf of Maine, (and potentially farther), forming a magmatic connection between the Hartford and Fundy rift basins. An extensive dyke fissure this large could have produced massive basalt flows covering both of those rift basins, as well as the areas in between (e.g., Swanson et al. 1975; Self et al. 1997). McHone (1996) proposed that similar basalts in basins of New Jersey to Pennsylvania (USA) are also linked to this great "initial Pangaean" flood basalt event of northeastern North America, with perhaps 50,000 kms of tholeiite extruded over an area of at least 500,000 km1 A volcanic event of this size must have had severe consequences for the Late Triassic world environment (McHone 2003). If large dykes in Spain, Morocco, and elsewhere (Bertrand 1991) were also active or nearly synchronous with this volcanism, the volume and area of this flood basalt would have been much greater. Because dyke systems vary in their ages across the northern CAMP, whether or not they have similar magma types, there may have been massive flood basalt eruptions in other areas that are older as well as younger than the basalts of the Hartford and Fundy basins.
SUMMARY OF CONCLUSIONS
1. The Christmas Cove Dyke is mapped for 190 km along the coast of Maine, USA, with intermittent but co-linear 13 to 35 m wide exposures of columnar dolerite. The dolerite is orthopyroxene-bearing quartz tholeiite of an "HTQ" type, and its age, mineralogy, chemistry, and geographic extent indicate that the Christmas Cove Dyke is contiguous and co-magmatic with the Onway Dyke of southern New Hampshire, the Holden Dyke of Massachusetts, the Higganum Dyke of southern New England, and probably dykes in southern New Brunswick, Canada; all parts of a giant dyke system at least 700 km long.
2. The southern part of the dyke system is the source of the Talcott Basalt, the initial (earliest) lava preserved in the Hartford Basin of Connecticut. Because the Talcott Basalt is tightly correlated and apparently co-magmatic with basalt in the Fundy Basin, Newark Basin, and possibly other basins in eastern North America, the Higganum-Christmas Cove dyke system and potential extensions represent a giant fissure source for the earliest basalts within and formerly outside of the basins. Because of that correlation, a precise U-Pb zircon date of 201.38 [+ or -] 0.02 Ma (Schoene et al. 2010) and finding of end-Triassic relative age (Cirilli et al. 2009) for the North Mountain Basalt can also apply to the Christmas Cove dyke system and its flood basalts, as allowed by our [sup.40]Ar/[sup.39]Ar dates.
3. Two other large dykes in southern New England (the Buttress and Bridgeport dykes) are linked to the middle and upper flood basalts in the Hartford Basin, which are roughly 300,000 years apart in age as shown by stratigraphy. By these connections, the three dyke systems must progress in age from younger to older, west to east. The dykes diverge northeastward through southern New England, and the mid-aged Buttress--Ware Dyke trends toward the Caraquet Dyke of central New Brunswick and Maine, which has similar petrology and age. Dyke ages may progress the same way from Maine into maritime Canada, so that the Shelburne Dyke of southern Nova Scotia may be somewhat older than the Christmas Cove Dyke and North Mountain Basalt, which are likewise older than the Caraquet Dyke. Such timing differences create distributional patterns among basalts, sills, and dykes of end-Triassic to Early Jurassic ages around the central Atlantic rift basins of northeastern North America, northwestern Africa, southwestern Europe, and possibly other areas of the Central Atlantic Magmatic Province.
Appendix A. Compositions of phenocrysts from the dyke at Swans Island. weight % Orthopyroxene Sample Si[O.sub.2] Ti[O.sub.2] Opxl core SI-PW-71b 56.71 0.00 Opx2c core SI-PW-71b 56.39 0.31 Opx2r rim SI-PW-71b 56.53 0.34 Opx3 core SI-PW-71b 56.74 0.24 Opx4c core SI-PW-71b 56.75 0.26 Opx4r rim SI-PW-71b 56.43 0.25 Opx5 core SI-PW-71b 57.29 0.00 Average SI-PW-71b 56.69 0.20 weight % Orthopyroxene [Al.sub.2] [Cr.sub.2] FeO MnO [O.sub.3] [O.sub.3] Opxl 1.40 11.08 0.00 Opx2c 2.38 10.10 0.00 Opx2r 0.99 12.01 0.42 Opx3 1.13 10.56 0.29 Opx4c 1.12 10.42 0.43 Opx4r 0.94 12.24 0.29 Opx5 1.55 11.17 0.28 Average 1.36 11.08 0.24 weight % Orthopyroxene MgO CaO [Na.sub.2]0 [K.sub.2]O Total Opxl 28.75 2.05 99.99 Opx2c 28.57 2.25 100.00 Opx2r 27.38 2.32 99.99 Opx3 28.86 2.19 100.01 Opx4c 28.81 2.22 100.01 Opx4r 27.71 2.13 99.99 Opx5 27.39 2.31 99.99 Average 28.21 2.21 100.00 cations (Basis of 6 oxygen) Orthopyroxene Si [Al.sup.iv] [Al.sup.vi] Cr Ti Opxl 1.999 0.001 0.057 0.000 Opx2c 1.980 0.020 0.078 0.008 Opx2r 2.007 0.000 0.041 0.009 Opx3 1.999 0.001 0.046 0.006 Opx4c 2.000 0.000 0.046 0.007 Opx4r 2.004 0.000 0.039 0.007 Opx5 2.020 0.000 0.064 0.000 Average 2.001 0.000 0.057 0.005 cations (Basis of 6 oxygen) Orthopyroxene [Fe.sup.2+] Mn Mg Ca Na Opxl 0.329 0.000 1.511 0.077 Opx2c 0.299 0.000 1.495 0.085 Opx2r 0.360 0.013 1.449 0.088 Opx3 0.313 0.009 1.516 0.083 Opx4c 0.309 0.013 1.513 0.084 Opx4r 0.366 0.009 1.467 0.081 Opx5 0.334 0.008 1.439 0.087 Average 0.330 0.007 1.484 0.084 end members Orthopyroxene Wo En Fs Opxl 4.0 78.8 17.9 Opx2c 4.5 79.6 16.7 Opx2r 4.7 76.4 19.9 Opx3 4.3 79.3 17.1 Opx4c 4.4 79.4 17.0 Opx4r 4.2 76.6 20.0 Opx5 4.7 77.4 18.8 Average 4.4 78.2 18.2 weight % Clinopyroxene Sample Si[0.sub.2] Ti[0.sub.2] Cpxl core SI-PW-71b 53.98 0.40 Cpx2 core SI-PW-71b 54.07 0.49 Cpx3 core SI-PW-71b 53.96 0.42 Cpx4 core SI-PW-71b 53.66 0.41 Cpx5 core SI-PW-71b 53.93 0.35 Cpx6 core SI-PW-71b 54.00 0.39 Average SI-PW-71b 53.93 0.41 weight % Clinopyroxene [Al.sub.2] [Cr.sub.2] FeO MnO MgO [O.sub.3] [O.sub.3] Cpxl 2.92 0.61 6.24 0.32 18.86 Cpx2 2.15 0.21 8.46 0.38 18.51 Cpx3 2.88 0.88 5.61 0.00 18.31 Cpx4 2.87 0.31 8.15 0.00 18.34 Cpx5 2.83 0.40 6.78 0.00 18.34 Cpx6 2.98 0.86 6.54 0.00 18.48 Average 2.77 0.55 6.96 0.12 18.47 weight % Clinopyroxene CaO [Na.sub.2]0 [K.sub.2]O Total Cpxl 16.67 0.00 100.00 Cpx2 15.73 0.00 100.00 Cpx3 17.42 0.52 100.00 Cpx4 15.87 0.39 100.00 Cpx5 16.96 0.41 100.00 Cpx6 16.45 0.30 100.00 Average 16.52 0.27 100.00 cations (Basis of 6 oxygen) Clinopyroxene Si [Al.sup.iv] [Al.sup.vi] Cr Ti Cpxl 1.952 0.048 0.077 0.017 0.011 Cpx2 1.969 0.031 0.061 0.006 0.013 Cpx3 1.952 0.048 0.075 0.025 0.011 Cpx4 1.952 0.048 0.075 0.009 0.011 Cpx5 1.956 0.044 0.077 0.011 0.010 Cpx6 1.954 0.046 0.081 0.025 0.011 Average 1.956 0.044 0.074 0.016 0.011 cations (Basis of 6 oxygen) Clinopyroxene [Fe.sup.2+] Mn Mg Ca Na Cpxl 0.190 0.010 1.017 0.646 0.000 Cpx2 0.260 0.012 1.005 0.614 0.000 Cpx3 0.171 0.000 0.988 0.675 0.036 Cpx4 0.249 0.000 0.995 0.619 0.028 Cpx5 0.206 0.000 0.992 0.659 0.029 Cpx6 0.199 0.000 0.997 0.638 0.021 Average 0.212 0.004 0.999 0.642 0.019 Clinopyroxene Wo En Fs Cpxl 34.9 54.9 10.3 Cpx2 32.7 53.5 13.8 Cpx3 36.8 53.9 9.3 Cpx4 33.2 53.4 13.4 Cpx5 35.5 53.4 11.1 Cpx6 34.8 54.4 10.9 Average 34.6 53.9 11.5 weight % Plagiodase Sample Si[O.sub.2] Ti[O.sub.2] Fspl core SI-PW-71b 51.16 Fsp2c core SI-PW-71b 51.26 Fsp2r rim SI-PW-71b 51.26 Fsp3c core SI-PW-71b 52.52 Fsp3r rim SI-PW-71b 50.88 Fsp4 core SI-PW-71b 51.93 Average SI-PW-71b 51.50 weight % Plagiodase [Al.sub.2] [Cr.sub.2] FeO MnO MgO [O.sub.3] [O.sub.3] Fspl 30.60 0.82 0.46 Fsp2c 30.48 0.79 0.43 Fsp2r 30.45 1.21 0.48 Fsp3c 29.79 0.55 0.47 Fsp3r 30.72 0.77 0.48 Fsp4 30.05 0.85 0.42 Average 30.35 0.83 0.46 weight % Plagiodase CaO [Na.sub.2]0 [K.sub.2]O Total Fspl 13.35 3.31 0.30 100.00 Fsp2c 13.90 3.14 0.00 100.00 Fsp2r 13.46 3.14 0.00 100.00 Fsp3c 12.69 3.77 0.20 99.99 Fsp3r 13.80 3.11 0.25 100.01 Fsp4 12.96 3.56 0.24 100.01 Average 13.36 3.34 0.17 100.00 cations (Basis of 6 oxygen) Plagiodase Si Al [Fe.sup.3+] [Fe.sup.3+] Fspl 2.332 1.644 0.003 0.029 Fsp2c 2.341 1.641 0.000 0.030 Fsp2r 2.343 1.640 0.000 0.046 Fsp3c 2.388 1.597 0.021 Fsp3r 2.322 1.652 0.029 Fsp4 2.365 1.613 0.032 Average 2.348 1.631 0.320 cations (Basis of 6 oxygen) Plagiodase Mg Ca Na K Fspl 0.031 0.652 0.293 0.017 Fsp2c 0.029 0.680 0.278 0.000 Fsp2r 0.033 0.659 0.278 0.000 Fsp3c 0.032 0.618 0.332 0.012 Fsp3r 0.033 0.675 0.275 0.015 Fsp4 0.029 0.632 0.314 0.014 Average 0.310 0.653 0.295 0.010 Plagiodase An Ab Or Fspl 67.8 30.4 1.8 Fsp2c 71.0 29.0 0.0 Fsp2r 70.3 29.7 0.0 Fsp3c 64.3 34.5 1.2 Fsp3r 70.0 28.5 1.5 Fsp4 65.8 32.7 1.5 Average 68.1 30.8 1.0 Note: most of the analyses are SEM/EDS "standardless" analyses that are only reported as normalized data (totals at or near 100%). Our few microprobe analyses are very similar and compare well with the majority, and we have also normalized them for consistency. For more a detailed study of mineral compositions in this dyke system see Dorais et al. (2005). Appendix B: [sup.40]Ar/[sup.39]Ar analytical data from whole rock dyke samples (moles [sup.39]Ar x [10.sup.-13]) *. Temp [degrees]C [sup.40]Ar/ [sup.37]Ar/ [sup.36]Ar/ [sup.39]Ar [sup.39]Ar [sup.39]Ar Sample: Ban - 1 (Caraquet Dyke), J-value = 0.006421 660 55.177 3.7475 0.12614 785 26.676 4.3372 0.02840 880 22.350 5.6259 0.01476 975 21.114 5.8502 0.01106 1050 20.950 5.4912 0.01053 1130 21.271 4.9834 0.01125 Fuse 23.493 16.355 0.02267 Temp [degrees]C Moles % Total % Rad [sup.39]Ar Sample: Ban - 1 (Caraquet Dyke), J-value = 0.006421 660 8.7 2.9 33.0 785 34.6 11.7 69.8 880 57.8 19.4 82.4 975 56.6 19.1 86.6 1050 49.7 16.8 87.0 1130 32.8 11.1 86.0 Fuse 56.5 19.1 76.9 Temp [degrees]C K/Ca Age (Ma) Sample: Ban - 1 (Caraquet Dyke), J-value = 0.006421 660 0.130 199.7 [+ or -] 15.0 785 0.113 204.2 [+ or -] 2.9 880 0.087 202.4 [+ or -] 2.4 975 0.083 201.1 [+ or -] 2.4 1050 0.088 200.7 [+ or -] 2.2 1130 0.096 201.3 [+ or -] 2.1 Fuse 0.030 200.3 [+ or -] 2.1 Total gas age = 201.7 [+ or -]3.2 Ma Isotope correlation age = 201.8 [+ or -] 1.7 Ma ([sup.40]Ar/[sup.36]Ar intercept = 294.9) Plateau age = 201.2 [+ or -] 2.6 Ma (66% of [sup.39]Ar released) Temp [degrees]C [sup.40]Ar/ [sup.37]Ar/ [sup.36]Ar/ [sup.39]Ar [sup.39]Ar [sup.39]Ar Sample: HPK - 1 (Higganum Dyke), J-value = 0.006467 660 45.344 11.5080 0.08925 785 23.087 4.3202 0.01708 880 21.826 5.5626 0.01335 975 21.192 5.7969 0.01161 1050 21.197 5.3088 0.01136 1130 21.507 4.8019 0.01279 Fuse 23.138 12.9360 0.01772 Temp [degrees]C Moles % Total % Rad [sup.39]Ar Sample: HPK - 1 (Higganum Dyke), J-value = 0.006467 660 24.1 7.1 43.8 785 43.0 12.7 79.5 880 58.5 17.3 83.9 975 56.5 16.7 85.9 1050 45.7 13.5 86.0 1130 42.0 12.4 83.7 Fuse 68.6 20.3 81.7 Temp [degrees]C K/Ca Age (Ma) Sample: HPK - 1 (Higganum Dyke), J-value = 0.006467 660 0.042 219.8 [+ or -] 6.0 785 0.113 203.0 [+ or -] 4.8 880 0.088 202.6 [+ or -] 2.5 975 0.084 201.6 [+ or -] 2.6 1050 0.092 201.9 [+ or -] 2.0 1130 0.102 200.2 [+ or -] 1.9 Fuse 0.038 210.0 [+ or -] 2.1 Total gas age = 204.6 [+ or -] 3.0 Ma Isotope correlation age = 200.2 [+ or -]2.8 Ma ([sup.40]Ar/[sup.36]Ar intercept = 318.7) Plateau age = 201.7 [+ or -] 2.8 Ma (60% of [sup.39]Ar released) Temp [degrees]C [sup.40]Ar/ [sup.37]Ar/ [sup.36]Ar/ [sup.39]Ar [sup.39]Ar [sup.39]Ar Sample: DP - 1 (Christmas Cove Dyke), J-value = 0.006092 660 50.750 2.8950 0.10638 785 28.394 4.0072 0.03270 880 25.296 4.7518 0.02220 975 23.813 5.2994 0.01689 1050 22.961 4.1600 0.01116 1130 22.927 4.0858 0.01211 Fuse 25.068 14.0980 0.02097 Temp [degrees]C Moles % Total % Rad [sup.39]Ar Sample: DP - 1 (Christmas Cove Dyke), J-value = 0.006092 660 13.0 3.9 38.4 785 41.9 12.5 67.0 880 35.9 10.7 75.5 975 60.3 17.9 80.7 1050 54.0 16.1 87.0 1130 55.3 16.4 85.6 Fuse 75.7 22.5 79.6 Temp [degrees]C K/Ca Age (Ma) Sample: DP - 1 (Christmas Cove Dyke), J-value = 0.006092 660 0.171 203.2 [+ or -] 5.3 785 0.122 198.5 [+ or -] 4.6 880 0.103 199.2 [+ or -] 4.8 975 0.095 200.5 [+ or -] 2.3 1050 0.177 207.9 [+ or -] 2.0 1130 0.122 204.6 [+ or -] 2.1 Fuse 0.034 209.1 [+ or -] 2.5 Total gas age = 205.3 [+ or -] 3.1 Ma Isotope correlation age = 203.6 [+ or -] 2.6 Ma ([sup.40]Ar/[sup.36]Ar intercept = 288.4) Average age = 203.1 (61% of [sup.39]Ar released) Temp [degrees]C [sup.40]Ar/ [sup.37]Ar/ [sup.36]Ar/ [sup.39]Ar [sup.39]Ar [sup.39]Ar Sample: MR - 1 (Christmas Cove Dyke), J-value = 0.006733 660 41.966 4.4992 0.07478 785 25.804 3.1368 0.02563 880 21.350 4.3602 0.01256 975 20.693 4.8337 0.00981 1050 20.094 3.9068 0.00755 1130 20.172 3.2905 0.00772 Fuse 23.394 10.0790 0.01325 Temp [degrees]C Moles % Total % Rad [sup.39]Ar Sample: MR - 1 (Christmas Cove Dyke), J-value = 0.006733 660 12.0 3.2 48.2 785 34.2 9.0 71.5 880 35.4 9.4 84.2 975 52.5 13.9 87.8 1050 85.5 22.5 90.4 1130 49.7 13.1 89.9 Fuse 109.6 28.9 86.6 Temp [degrees]C K/Ca Age (Ma) Sample: MR - 1 (Christmas Cove Dyke), J-value = 0.006733 660 0.109 230.8 [+ or -] 8.9 785 0.156 211.8 [+ or -] 3.7 880 0.112 206.6 [+ or -] 4.6 975 0.101 208.8 [+ or -] 2.5 1050 0.125 208.6 [+ or -] 2.2 1130 0.149 208.3 [+ or -] 2.4 Fuse 0.048 232.3 [+ or -] 2.5 Total gas age = 214.8 [+ or -] 3.0 Ma Isotope correlation age = 204.8 [+ or -] 2.7 Ma ([sup.40]Ar/[sup.36]Ar intercept = 325.6) Average age = 208.1 (59% of [sup.39]Ar released) Temp [degrees]C [sup.40]Ar/ [sup.37]Ar/ [sup.36]Ar/ [sup.39]Ar [sup.39]Ar [sup.39]Ar Sample: SP - 1 (Christmas Cove Dyke), J-value = 0.006253 660 88.511 3.1490 0.21871 785 26.032 3.3465 0.02434 880 22.954 3.8914 0.01515 975 21.159 3.7523 0.01030 1050 20.393 3.0286 0.00775 1130 20.593 2.6849 0.00825 Fuse 24.582 9.0482 0.01917 Temp [degrees]C Moles % Total % Rad [sup.39]Ar Sample: SP - 1 (Christmas Cove Dyke), J-value = 0.006253 660 4.3 1.1 27.1 785 51.2 12.5 73.2 880 60.2 14.7 81.4 975 54.7 13.4 86.8 1050 68.4 16.7 89.8 1130 49.7 12.2 89.0 Fuse 119.8 29.3 79.8 Temp [degrees]C K/Ca Age (Ma) Sample: SP - 1 (Christmas Cove Dyke), J-value = 0.006253 660 0.162 253.9 [+ or -] 5.3 785 0.146 203.9 [+ or -] 2.7 880 0.126 200.7 [+ or -] 2.3 975 0.130 196.9 [+ or -] 2.0 1050 0.161 196.1 [+ or -] 1.9 1130 0.181 196.3 [+ or -] 1.9 Fuse 0.054 210.0 [+ or -] 2.0 Total gas age = 196.4 [+ or -] 2.8 Ma Isotope correlation age = 196.4 [+ or -] 3.0 Ma ([sup.40]Ar/[sup.36]Ar intercept = 326.9) Average age = 197.0 (57% of [sup.39]Ar released) * All samples were analyzed as whole rock splits after sieving to a 100 to 150 micron grain size and after any carbonate minerals were dissolved through washing with warm dilute hydrochloric acid. These samples, along with an internal flux monitor (SBG-7 = 240.9 Ma relative to MMhb-1), were wrapped in Sn foil, sealed in silica glass vials and irradiated in the L67 facility of the Ford Nuclear Reactor at the University of Michigan. Purification of the gases extracted from the flux monitors and unknowns follow standard laboratory procedures described in detail by West et al. (1992). The isotopic composition of argon was measured in 1995 using a Nuclide 6-60 SGA 1.25 mass spectrometer at the University of Maine. Corrections were made for all interfering isotopes produced during irradiation using correction factors determined from irradiated K and Ca salts. The uncertainty in the calculated J values is believed to be less than 0.5%. Individual ages and uncertainties (2 sigma) were calculated using the decay constants and isotope abundances recommended by Steiger and Jager (1977) and the equations given by Dalrymple et al. (1981). Total gas ages represent weighted averages based upon the amount of [sup.39]Ar in each increment. Criteria for the determination of plateau ages are from Fleck et al. (1977) and uncertainties associated with the reported plateau ages are two standard deviations about the mean plus an uncertainty in the J-value (estimated at 0.5%). For convenience, where the apparent ages of consecutive increments are similar but do not satisfy the formal criteria for a plateau age, a weighted average age for the consecutive steps is reported.
Sandra Barr and Anthony Philpotts assisted with thin sections and chemical data used in this study, and we thank them for much additional information and encouragement. Daniel Lux provided facilities of the University of Maine radiometric isotope lab for argon dates. Andrew Lindsey and Jelle de Boer located and described the dyke at Whitehead Island. Nancy McHone, Chris White, Michael Dorais, Daniel Kontak, Jelle de Boer, John Puffer, Paul Olsen, Daniel Sundeen, and Paul Ragland provided many useful discussions and other assistance. We appreciate the helpful comments and reviews of the manuscript by John Greenough and Jarda Dostal.
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Editorial responsibility: Sandra M. Barr
Received 22 January 2014 f accepted 04 March 2014
J. GREGORY MCHONE (1) *, ARTHUR M. HUSSEY, II (2), DAVID P. WEST, JR. (3), AND DAVID G. BAILEY (4)
(1.) 9 Dexters Lane, Grand Manan, New Brunswick E5G3A6, Canada
(2.) Department of Earth and Oceanographic Science, Bowdoin College, Brunswick, Maine 04011 USA
(3.) Department of Geology, Middlebury College, Vermont 05753 USA
(4.) Department of Geosciences, Hamilton College, Clinton, New York 13323 USA
* Corresponding author < firstname.lastname@example.org>
Table 1. Field observations of the Christmas Cove Dyke, SW to NE. Location General Contact Dip Width (m) Strike Azimuth Rte 202/4, Waterboro N50E 50? 90? >8 shore at Cumberland N80E 80 85 S 18 Foreside Doyle Point, N78E 73 68 N 32.3 Yarmouth tank farm, Harpswell N71E 79 60 NW 19 Neck Rte. 123, Harpswell N53E 80 90 >20 Mountain Rd, N83E 91? 55 S >20 Harpswell Dingley Rd, 90E varies 62-80 84 S 19.2 Harpswell hillside above N84E 89 81 S 28.4 store, Phippsburg Spruce Point, N83E 78 85 N 12 Boothbay Harbor Christmas Cove, N77E 77 85 S 22 South Bristol Whitehead Island, N75E varies 10-90 90 13 St. George SW shoreline, N55E 55 85 S 35 Swans Island Location Notes Rte 202/4, Waterboro partially exposed road cut on the south side shore at Cumberland well exposed in a low hill, Foreside contact rotates at the north end Doyle Point, well exposed, trends toward Yarmouth Harpswell Neck tank farm, Harpswell partially offset (faulted?) Neck to the north, with slickensides Rte. 123, Harpswell in a low cut on the SE roadside, contacts not well exposed Mountain Rd, contacts not well exposed; Harpswell very large columns dipping S Dingley Rd, low road cut, N and S contacts Harpswell poorly exposed hillside above in wooded bank above store; store, Phippsburg jog in woods is N30E Spruce Point, attitude from fractures, with the Boothbay Harbor center exposed in whalebacks Christmas Cove, interior open along small cove, South Bristol N contact exposed Whitehead Island, visible with Google Earth on the S St. George shoreline; several left-lateral jogs SW shoreline, exposed along the SW coastline Swans Island and on the northern shore Table 2. Chemical analyses of the Christmas Cove Dyke and related dykes. Sample HPK RT-4 CF-1 DP-I Si[O.sub.2] (wt. %) 52.1 51.11 50.3 50.4 Ti[O.sub.2] 0.98 1.11 1.16 1.15 [Al.sub.2][0.sub.3] 15 12.37 13.94 14.3 [Fe.sub.2][0.sub.3] 10.8 12.12 11.9 11.2 MnO 0.17 0.17 0.17 0.19 MgO 7.64 8.24 7.31 7.23 CaO 10.6 11.86 11.63 10.40 [Na.sub.2]0 2./14 2.26 2.87 1.94 [K.sub.2]0 0.5 0.75 0.72 0.54 [P.sub.2][0.sub.5] 0.12 0 0.13 LOI 0.2 2.25 Total 100.15 99.99 100.00 99.73 Rb (ppm) 17 30 23 10 Sr 181 164 199 166 y 22.1 25.3 17 16 Zr 74 102 114 100 Nb 4.1 6.3 10 10.0 Ba 140 201 192 148 Cr 241 231 230 300 Ni 92 83 75 V 233 268 223 Co 41 47 55 Cu 107 122 135 Zn 82 93 59 Cs 1.4 1.4 La 9.55 11.2 Ce 20.4 24.9 Pr 2.4 3.15 Nd 9.79 11.9 Sm 3.11 3.45 Eu 1.1 1.24 Gd 3 3.95 Tb 0.58 0.67 Dy 3.9 4.31 Ho 0.g0 0.96 Er 1.98 2.45 Tm 0.3 0.34 Yb 2.06 2.2 Lu 0.33 0.38 Hf 2 2.7 Ta 0.41 0.55 W 42.8 Tl 0.09 0.16 Th 1.73 2.15 U 0.36 0.45 Sample DP-2 MTP, SP-1 XC-2 Si[O.sub.2] (wt. %) 49.75 51.6 50.88 51.70 Ti[O.sub.2] 1.27 1.11 1.13 1.1 [Al.sub.2][0.sub.3] 13.82 14.1 13.92 13.9 [Fe.sub.2][0.sub.3] 12.7 11.5 i1.70 11.6 MnO 0.2 0.17 0.18 0.17 MgO 7.05 7.59 7.51 8.01 CaO 11.98 10.3 11.13 10.2 [Na.sub.2]0 2.46 1.92 2.25 1.94 [K.sub.2]0 0.75 0.6 0.64 0.61 [P.sub.2][0.sub.5] 0.13 0.1 0.13 LOI 0.65 1.03 0.95 Total 99.98 99.67 100.47 100.31 Rb (ppm) 24 27 22 10 Sr 231 187 175 162 y 19 23.3 23 16 Zr 126 83 81 101 Nb 9 5.6 5.4 10 Ba 204 158 143 141 Cr 298 329 328 300 Ni 83 111 113 V 246 273 258 Co 53 49 48 Cu 138 108 112 Zn 89 63 85 Cs 1.5 0.7 La 10.4 10.2 Ce 20.6 21.5 Pr 2.62 2.52 Nd 11.4 10.4 Sm 3.45 3.38 Eu 1.08 1.11 Gd 3.33 3.22 Tb 0.69 0.61 Dy 4.34 4.2 Ho 0.83 0.84 Er 2.23 2.07 Tm 0.36 0.32 Yb 2.22 2.17 Lu 0.34 0.34 Hf 2.4 2.2 Ta 0.56 0.55 W 53.4 71.4 Tl 0.15 0.14 Th 1.78 1.72 U 0.4 0.37 Sample XC-I SI av BAN Si[O.sub.2] (wt. %) 49.21 52.03 50 Ti[O.sub.2] 1.18 1.12 0.79 [Al.sub.2][0.sub.3] 13.59 14.05 14.54 [Fe.sub.2][0.sub.3] 13.09 11.03 12.66 MnO 0.17 0.16 0.2 MgO 7.64 7.44 7.19 CaO 11.87 10.62 11.14 [Na.sub.2]0 2.53 2.06 2.69 [K.sub.2]0 0.7 0.5 0.6 [P.sub.2][0.sub.5] 0.13 0.18 LOI 0.75 Total 99.98 99.89 99.99 Rb (ppm) 24 25 16 Sr 172 205 158 y 22.9 31 18 Zr 86 98 78 Nb 5 8 Ba 185 178 170 Cr 299 291 112 Ni 92 79 46 V 246 281 192 Co 43 48 Cu 109 88 Zn 82 85 72 Cs 0.7 La 9.24 Ce 20.9 Pr 2.62 Nd 9.99 Sm 3.05 Eu 1.12 Gd 3.3 Tb 0.58 Dy 3.88 Ho 0.85 Er 2.16 Tm 0.3 Yb 2.04 Lu 0.35 Hf 2.4 Ta 0.43 W Tl 0.14 Th 1.8 U 0.37 Sample CAR BUT Si[O.sub.2] (wt. %) 51.12 51.74 Ti[O.sub.2] 0.83 0.79 [Al.sub.2][0.sub.3] 14.78 15.12 [Fe.sub.2][0.sub.3] 12.18 10.63 MnO 0.19 0.19 MgO 7.58 7.4 CaO 10.34 11.11 [Na.sub.2]0 2.05 2.43 [K.sub.2]0 0.58 0.44 [P.sub.2][0.sub.5] 0.12 0.15 LOI Total 99.76 100 Rb (ppm) 17 12 Sr 134 111 y 25 29 Zr 65 66 Nb 5 Ba 124 Cr 141 202 Ni 53 51 V 254 291 Co Cu 65 104 Zn 75 Cs La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Hf Ta W Tl Th U Sample codes: HPK = Higgamnn Dyke at Hurd State Park, Connecticut; RT-4 = Onway Dyke at its Route' 4 roadcut west of Durham, New Hampshire; CF-1 = Christmas Cove Dyke at Cumberland Foreside, Maine; DP-1 and DP2 = Doyle Point on Cousins Island, Maine; MTR = Mountain Road in Harpswell, Maine; SP-1 = Spruce Point in Southport, Maine; XC-1 and XC-2 = Christmas Cove in Sooth Bristol, Maine; SI average = average of 9 samples from Swans Island, Maine (Table 3); BAN = Caraquet Dyke at Mattawamkeag River in Bancroft, Maine; CAR = average of Caraquet Dyke analyses (Greenough and Papzeik 1986); BUT = average of Buttress Dyke analyses (Philpotts and Martello 1986). Table 3. Whole rock analyses across the dyke at Swans Island. Sample SI-DB18 SI-PP-1a SI-PP-1b Si[O.sub.2] (wt. %) 52.31 51.81 52.25 Ti[O.sub.2] 1.09 1.15 1.17 [Al.sub.2][O.sub.3] 13.61 14.64 13.7 [Fe.sub.2][O.sub.3] 11.21 11.25 11.4 MnO 0.17 0.16 0.17 MgO 7.59 6.77 7.21 CaO 10.64 10.83 10.58 [Na.sub.2]0 1.85 2.18 2.12 [K.sub.2]0 0.58 0.52 0.57 [P.sub.2][0.sub.5] 0.13 0.13 0.13 LOI 0.48 0.43 0.4 Total 99.66 99.87 99.7 Rb (ppm) 17 16 17 Sr 168 195 176 Y 23 36 33 Zr 86 106 103 Nb Ba 146 168 153 Cr 305 209 264 Ni 84 74 78 V 265 279 282 Zn 80 87 86 Sc 40 38 40 CIPW normative modes %AN 62.02 59.39 57.91 Q 5.82 4.47 5.1 Or 3.53 3.15 3.46 Ab 17.1 20.08 19.57 An 27.92 29.38 26.92 Di 20.44 19.91 20.94 Hy 20.57 18.24 19.19 Wo 0 0 0 Ol 0 0 0 Ac 0 0 0 Mt 2.79 2.84 2.87 Il 1.56 1.64 1.68 Hem 0 0 0 Ti 0 0 0 Ap 0.28 0.28 0.28 Sample SI-PP-1c SI-PP-1d SI-PP-1e Si[O.sub.2] (wt. %) 51.87 51.95 51.80 Ti[O.sub.2] 1.11 1.01 1.07 [Al.sub.2][O.sub.3] 13.66 13.97 14.28 [Fe.sub.2][O.sub.3] 11.3 10.69 10.93 MnO 0.17 0.16 0.16 MgO 7.80 8.05 7.66 CaO 10.74 10.89 10.69 [Na.sub.2]0 2.06 1.99 2.21 [K.sub.2]0 0.52 0.4 0.52 [P.sub.2][0.sub.5] 0.13 0.11 0.12 LOI 0.4 0.68 0.54 Total 99.76 99.9 99.98 Rb (ppm) 17 14 18 Sr 179 200 194 Y 30 26 24 Zr 98 93 87 Nb Ba 137 116 140 Cr 328 350 318 Ni 85 93 78 V 291 273 276 Zn 80 79 76 Sc 40 40 39 CIPW normative modes %AN 58.89 61.05 58.1 Q 4.14 4.45 3.46 Or 3.15 2.42 3.14 Ab 18.96 18.29 20.27 An 27.15 28.67 28.1 Di 21.27 20.72 20.22 Hy 20.67 21.09 20.30 Wo 0 0 0 Ol 0 0 0 Ac 0 0 0 Mt 2.8 2.69 2.74 Il 1.58 1.44 1.52 Hem 0 0 0 Ti 0 0 0 Ap 0.28 0.24 0.26 Sample SI-PP-1f SI-PP-1g SI-PP-1h Si[O.sub.2] (wt. %) 52.08 51.97 52.23 Ti[O.sub.2] 1.06 1.16 1.23 [Al.sub.2][O.sub.3] 13.91 14.07 14.64 [Fe.sub.2][O.sub.3] 10.86 11.4 10.2 MnO 0.16 0.17 0.16 MgO 7.63 7.34 6.88 CaO 10.7 10.74 9.77 [Na.sub.2]0 2.12 1.94 2.06 [K.sub.2]0 0.5 0.37 0.52 [P.sub.2][0.sub.5] 0.12 0.13 0.16 LOI 0.72 0.82 2.31 Total 99.86 100.11 100.16 Rb (ppm) 16 12 111 Sr 190 185 360 Y 34 38 37 Zr 94 105 106 Nb Ba 137 131 476 Cr 311 276 260 Ni 91 76 48 V 278 293 290 Zn 81 91 107 Sc 40 40 39 CIPW normative modes %AN 58.62 62.14 61.19 Q 4.49 5.7 7.38 Or 3.03 2.25 3.2 Ab 19.52 17.92 19.25 An 27.66 29.42 30.36 Di 20.79 19.63 15.21 Hy 19.99 20.28 19.5 Wo 0 0 0 Ol 0 0 0 Ac 0 0 0 Mt 2.75 2.86 2.97 Il 1.51 1.66 1.78 Hem 0 0 0 Ti 0 0 0 Ap 0.26 0.28 0.35 Notes: Samples are roughly equally spaced across the dyke, northwest to southeast. See the text for discussion of the analytical methods. Table 4. Radiometric dates (Ma) of regional dykes and basahs. K/Ar K/Ar Method whole rock plagioclase Holyoke Basah Talcott Basalt 186 [+ or -] 3 (4) 186 [+ or -] 8 (4) North Mountain Basalt (NMB) Higganum Dyke 194 [+ or -] 12 (3) Christmas Cove 191 [+ or -] 10 (2) Dyke Caraquet Dyke 191 [+ or -] 2 (6) Ministers Is. 189 [+ or -] 8 (5) Dyke Shelburne Dyke 193 [+ or -] 2 (6) [sup.40]Ar/ [sup.40]Ar/ [sup.39]Ar [sup.39]Ar Method biotite whole rock Holyoke Basah Talcott Basalt North Mountain 201 [+ or -] 2.5 (8) Basalt (NMB) 200.8 [+ or -] 2.2 (8) Higganum Dyke 201.2 [+ or -] 2.4 (1) Christmas Cove 196.4 - 204.8 (1) Dyke Caraquet Dyke 201.5 [+ or -] 2.4 (1) Ministers Is. Dyke Shelburne Dyke 202 [+ or -] 3 (7) [sup.40]Ar/ [sup.39]Ar Method plagioclase U/Pb zircon Holyoke Basah 199.3 [+ or -] 1.2 (9) Talcott Basalt 187 [+ or -] 10 (4) North Mountain 201.0 [+ or -] 1.4 (9) 201.7 [+ or -] 1.4 (10) Basalt (NMB) 198.9 [+ or -] 0.7 (8) 201.27 [+ or -] 0.06 (11) 201.38 [+ or -] 0.02 (12) Higganum Dyke Christmas Cove Dyke Caraquet Dyke Ministers Is. Dyke Shelburne Dyke References: (1) this paper; (2) Weston Geophysical 1977; (3) Armstrong and Besancon 1970; (4) Seiderman et al. 1984; (5) Stringer and Burke 1985; (6) Hodych and Hayatsu 1988; (7) Dunn et al. 1998; (8) Kontak and Archibald 2003; (9) Jourdan et al. 2009; (10) Hodych and Dunning 1992; (11) Schaltegger et al. 2008; (12) Schoene et al. 2010. Table 5. Large dykes and correlated flood basalts of the northern CAMP. (1) York (2) Palisades (3) Higganum Source Dyke Haven Sill Holden Si[O.sub.2] (wt. %) 51.84 51.98 52.62 Ti[O.sub.2] 1.09 1.22 1.17 [Al.sub.2][O.sub.3] 14.34 14.48 14.96 FeO * 9.93 10.19 10.20 MnO 0.20 0.18 0.17 MgO 7.72 7.59 7.59 CaO 10.73 10.33 10.94 [Na.sub.2]O 1.96 2.04 2.33 [K.sub.2]O 0.60 0.84 0.56 [P.sub.2][O.sub.5] 0.12 0.20 (4) Christmas (5) Ministers Source Dyke Cove Island Si[O.sub.2] (wt. %) 52.58 52.94 Ti[O.sub.2] 1.15 1.14 [Al.sub.2][O.sub.3] 14.47 14.13 FeO * 10.53 10.05 MnO 0.18 0.20 MgO 7.81 7.92 CaO 10.57 10.94 [Na.sub.2]O 1.98 1.97 [K.sub.2]O 0.60 0.55 [P.sub.2][O.sub.5] 0.13 0.14 (6) Foum Source Dyke Zguid (7) Messejana Si[O.sub.2] (wt. %) 51.99 52.07 Ti[O.sub.2] 1.10 1.04 [Al.sub.2][O.sub.3] 15.05 15.90 FeO * 9.52 9.28 MnO 0.18 0.16 MgO 7.69 7.16 CaO 11.75 11.51 [Na.sub.2]O 1.97 2.16 [K.sub.2]O 0.60 0.58 [P.sub.2][O.sub.5] 0.15 0.14 (8) Mt. Zion (9) Orange Basalt Product Church Mountain (10) Talcott ? Si[O.sub.2] (wt. %) 51.37 51.45 51.86 Ti[O.sub.2] 1.18 10.2 1.07 [Al.sub.2][O.sub.3] 14.24 14.34 14.27 FeO * 10.86 10.36 10.86 MnO 0.17 0.15 0.16 MgO 7.58 8.19 7.98 CaO 10.78 10.86 11.24 [Na.sub.2]O 2.05 2.10 2.06 [K.sub.2]O 0.21 0.54 0.50 [P.sub.2][O.sub.5] 0.13 0.13 (11) North (12) High Basalt Product Mountain Atlas ? Si[O.sub.2] (wt. %) 52.16 51.06 Ti[O.sub.2] 1.06 1.06 [Al.sub.2][O.sub.3] 14.29 14.84 FeO * 10.35 10.33 MnO 0.16 0.19 MgO 7.05 8.17 CaO 10.35 12.25 [Na.sub.2]O 2.39 1.69 [K.sub.2]O 0.60 0.49 [P.sub.2][O.sub.5] 0.16 0.16 References: this paper; Bertrand 1991; Dunn and Stringer 1990; Philpotts and Martello 1986; Puffer 1992; Smith et al. 1975. Each of the above are averages of four to ten analyses. Locations: (1) southern Pennsylvania. USA; (2) eastern New jersey, USA; (3) eastern Connecticut and Massachusetts, USA; (4) southern Maine, USA; (5) southwestern New Brunswick, Canada; (6) southeastern Morocco; (7) Portugal and Spain; (8) Culpeper Basin of Northern Virginia, USA; (9) Newark Basin of New Jersey, USA; (10) Hartford Basin of Connecticut, USA; (11) Fundy Basin of Nova Scotia and New Brunswick, Canada; (12) Argana Basin of Morocco. Question mark signifies that basalt products are undetermined.
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|Author:||McHone, J. Gregory; Hussey, Arthur M., II; West, David P., Jr.; Bailey, David G.|
|Date:||Jan 1, 2014|
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