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Late Proterozoic-Cambrian Metamorphic Basement of the Alexander Terrane on Long and Dall Islands, Southeast Alaska

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Late Proterozoic-Cambrian Metamorphic Basement of the Alexander Terrane on Long and Dall Islands, Southeast Alaska Late Proterozoic-Cambrian metamorphic basement of the Alexander terrane on Long and Dall Islands, southeast Alaska GEORGE E. GEHRELS Department of Geosciences, University of Arizona, Tucson, Arizona 85721 ABSTRACT much of southeast Alaska and parts of coastal Previous Work British Columbia, southwestern Yukon, and Geologic and U-Pb (zircon) geochrono- eastern Alaska (Fig. 1; Berg and others, 1972; Buddington and Chapin (1929) mapped the logic studies demonstrate that Long Island Gehrels and Saleeby, 1987a). In contrast to the shorelines of Dall and Long Islands in recon- and southern and central Dall Island are un- relatively nondeformed Ordovician through naissance fashion and published the first geo- derlain in large part by upper Proterozoic- Triassic strata that characterize much of the logic map and descriptions of the area. Various Lower Cambrian metamorphic rocks of the Alexander terrane, Long and Dall Islands are U.S. Geological Survey workers have studied Wales Group. The group comprises a lower underlain in large part by upper Proterozoic- parts of Dall and Long Islands, but only the assemblage of predominantly metadacite, Lower Cambrian metamorphic rocks. These northern part of Dall Island has been described metamorphosed to amphibolite and green- older rocks apparently served as the metamor- in published reports (Condon, 1961; Eberlein schist facies, and an upper assemblage of phic basement for the widespread Ordovician and others, 1983). These reports, combined with lower-grade basaltic metavolcanic rocks, and younger strata. investigations on southern Prince of Wales Is- thick marble layers, and interlayered calcare- land (Herreid and others, 1978; Gehrels and Sa- ous metadacite, marble, metapelite, and met- leeby, 1986, 1987a, 1987b), provided the agraywacke. Rocks of both assemblages are geologic and tectonic framework for this study. intruded by metagranodiorite-diorite-gabbro suites, one of which (Kaigani orthogneiss) This Study yields a concordant U-Pb (zircon) age of 554 ± 4 m.y. (Early Cambrian). Rocks of the The geology of Long Island and southern and upper Wales assemblage were thrust over central Dall Island was mapped in reconnais- Ordovician(?)-Silurian strata of the Descon sance fashion by foot and skiff traverses along Formation, possibly during the Middle Silu- shoreline, and by foot traverses and selected rian-earliest Devonian Klakas orogeny. A helicopter landings in the interior of the islands. younger normal(?) fault juxtaposes rocks of This report presents (1) an overview of the first- the upper Wales Group, and locally the order geologic components and structures, Descon Formation and Heceta Limestone, (2) U-Pb (zircon) geochronologic constraints for over higher-grade rocks of the lower Wales two of the main intrusive units, and (3) an out- Group. This poorly known structure may line of the tectonic history of the region. have been active during a Late Permian(?)- Triassic rifting event recorded along the GEOLOGIC FRAMEWORK northeastern margin of the terrane. The youngest major unit in the area is the Stripe Long Island and much of southern and cen- Mountain granodiorite, which yields a con- tral Dall Island (Figs. 2 and 3) are underlain by cordant U-Pb (zircon) age of 114 ± 2 m.y. metavolcanic and metasedimentary rocks of the Wales Group (Wales metamorphic suite of INTRODUCTION Gehrels and Saleeby, 1987b). Intrusive into these rocks are the Lower Cambrian Kaigani Regional Framework orthogneiss and correlative metaplutonic suites, various ultramafic bodies of probable Late Or- Long and Dall Islands comprise a variety of dovician age, and several Cretaceous granodio- stratified, intrusive, and metamorphic rocks that rite plutons. Stratified units in the area are in range in age from Late Proterozoic-Early Cam- Figure 1. Location map of Long and Dall fault contact with the Wales Group and include brian through Early Cretaceous. These rocks be- Islands and the Alexander terrane (adapted Ordovician(?)-Silurian clastic strata of the Des- long to the Alexander terrane, which underlies from Berg and others, 1972). con Formation and the Silurian Heceta Lime- Geological Society of America Bulletin, v. 102, p. 760-767, 6 figs., 1 table, June 1990. 760 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/102/6/760/3380934/i0016-7606-102-6-760.pdf by guest on 27 September 2021 Figure 2. Sketch map of the main lithic units and structures on Long Island and southern and central Dall Island. Some map relations north of 55°N are adapted from Condon (1961) and Eberlein and others (1983). Map relations south of 55°N are from this study. AB, American Bay; CH, Coco Harbor; CM, Cape Muzon; DH, Datzkoo Harbor; GH, Grace Harbor; GM, Grace Mountain; KH, Kaigani Harbor; PB, Port Bazan; RI, Rose Inlet; SM, Stripe Mountain; WB, Waterfall Bay. On inset map: GI, Gravina Island; AI, Annette Island; POWI, Prince of Wales Island. Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/102/6/760/3380934/i0016-7606-102-6-760.pdf by guest on 27 September 2021 762 G. E. GEHRELS stone. Predominant structures include the Au- the underlying volcanic rocks. A similar clastic schists are structurally overlain by greenschist- gustine thrust fault, which juxtaposes the Wales sequence is below the marble layer in Waterfall facies rocks of the upper assemblage. To the Group over the Descon Formation, and the Bay (Fig. 2). northwest, the grade decreases to greenschist fa- Rose Inlet normal(?) fault, which juxtaposes Most of the units in this assemblage display cies, and north of Grace Harbor, protolith rela- strata of the Descon and Heceta Formations and strong flattening and elongation fabrics, and tions are well preserved. Graded beds and lower-grade rocks of the Wales Group over a some are highly folded. Marble layers show the cross-bedding in clastic strata north of Rose Inlet higher-grade assemblage of Wales Group rocks. least deformation and commonly retain their suggest that the lower assemblage is younger to primary bedding characteristics. Primary lime- the northwest. The predominant lithic type in Wales Group stone breccias with well-preserved angular clasts the lower-grade areas is a dacitic to andesitic attest to the lack of deformation in some areas. volcanic rock with 1- to 20-cm-scale fragments. The Wales Group is herein divided into upper In most regions, however, the marbles are mod- Such lithic types grade into the strongly de- and lower assemblages on the basis of differ- erately foliated and display pervasive stylolites. formed schists of similar bulk composition to the ences in protoliths and metamorphic grade (Fig. Strongly flattened and elongated pillows and southeast. Hence, most metamorphic rocks of 4). The Rose Inlet fault separates the two fragments record high strain in the volcanic the lower assemblage were apparently derived assemblages. rocks, but folds are rare in this unit. In contrast, from a thick and regionally extensive pile of Upper Assemblage. Three predominant units rocks of the calcareous metadacite and metape- silicic to intermediate volcanic rocks. in this assemblage (Fig. 4) include (1) pillow lite unit commonly display complex centimeter- Correlation of Units in Upper and Lower basalt, subordinate pillow breccia and tuffaceous to meter-scale asymmetric folds. Assemblages. As shown in Figure 4, units near breccia, and minor tuff and volcaniclastic gray- Metamorphism generally reached greenschist the base of the upper assemblage are tentatively wacke; (2) gray, bluish-gray, tan, and white facies, as recorded by chlorite-albite-epidote as- correlated with strata near the top of the lower (generally light gray to tan on weathered sur- semblages in rocks of mafic to intermediate assemblage. The sequence suspected to be cor- face) marble that is massive to thick bedded; and composition. At the southern tip of Dall Island, relative consists of basaltic pillow flows inter- (3) dacitic tuff, calcareous tuff, marble, calcare- however, the grade increases and the predomi- bedded with 1- to 10-m-thick layers of marble, ous siltstone, and dark gray to black phyllite that nant metagraywacke lithology is a biotite- 10- to 100-m-thick volcaniclastic turbidites, and are interbedded on a centimeter scale. Unit 3 hornblende-plagioclase schist. fragmental dacitic volcanic rocks. Similar lithic above has many sulfide-rich layers along the Lower Assemblage. The lower assemblage associations do not occur elsewhere in either the west shore of Dall Island. Subordinate units in comprises a tremendous thickness of dacitic upper or lower assemblages. Alternatively, if this the upper assemblage include (1) fragmental da- metavolcanic rocks and subordinate marble, correlation is incorrect, then the Rose Inlet fault citic metavolcanic rocks similar to those in the metabasalt, metarhyolite, and metavolcaniclastic has removed considerable stratigraphic section, lower assemblage; (2) black phyllite (with local strata (Fig. 4). These rocks are in a structural because the lower assemblage does not contain sulfide-rich horizons) derived from laminated window, separated from the upper assemblage the thick marble layer seen in the upper assem- black shale; (3) metarhyolite that displays by the Rose Inlet fault (Figs. 2 and 3). In blage, and a thick section of dacitic breccia and centimeter- to meter-scale angular volcanic general, the lower assemblage decreases in tuff is not in the upper assemblage. fragments; and (4) metagraywacke with local metamorphic grade northwestward from am- Age of the Wales Group. The protolith age conglomeratic horizons. phibolite to greenschist facies. Highest meta- of the Wales Group has not yet been determined Stratigraphic facing in the upper assemblage morphic grades are near American Bay (Fig. 2), directly; many samples of marble from through- is constrained by a 2-m-thick conglomeratic ho- where most rocks are medium- to coarse- out the study area have not yielded conodonts rizon that crops out immediately beneath the grained schists comprising garnet, hornblende, (N. M. Savage, 1988, oral commun.), and sev- main marble layer on Dall Island. On the south muscovite, biotite, quartz, and plagioclase.
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