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The Geology of Precambrian Rocks of Newport and Middledown, Rhode Island

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The Geology of Precambrian Rocks of Newport and Middledown, Rhode Island University of New Hampshire University of New Hampshire Scholars' Repository New England Intercollegiate Geological NEIGC Trips Excursion Conference Collection 1-1-1981 The Geology of Precambrian Rocks of Newport and Middledown, Rhode Island Rast, Nicholas Skehan, James W. Follow this and additional works at: https://scholars.unh.edu/neigc_trips Recommended Citation Rast, Nicholas and Skehan, James W., "The Geology of Precambrian Rocks of Newport and Middledown, Rhode Island" (1981). NEIGC Trips. 293. https://scholars.unh.edu/neigc_trips/293 This Text is brought to you for free and open access by the New England Intercollegiate Geological Excursion Conference Collection at University of New Hampshire Scholars' Repository. It has been accepted for inclusion in NEIGC Trips by an authorized administrator of University of New Hampshire Scholars' Repository. For more information, please contact [email protected]. 67 Trip B-2 THE GEOLOGY OF PRECAMBRIAN ROCKS OF NEWPORT AND MIDDLETOWN, RHODE ISLAND by Nicholas Rast and James W. Skehan, S.J. Department of Geology Weston Observatory University of Kentucky Dept, of Geology & Geophysics Lexington, KY 40506 Boston College Weston, MA 02193 INTRODUCTION The older rocks of Newport, Rhode Island have been extensively described (full bibliography in Quinn, 1971). In recent years these rocks were dis­ cussed by Kay and Chappie (1976), mapped by Moore (1975), and Smith (1978) has dated the Newport granite which intrudes the bedded rocks. The bedded succ­ ession has been referred to, on incomplete evidence but correctly,as a meta sedimentary sequence overlain by volcaniclastic rocks (Quinn, 1971). Each of the two sequences is of a considerable thickness and the informal terms, New­ port and Price's Neck formation have been given to the metasedimentary and the metavolcanic sequence respectively (Rast and Skehan, in press 1981). The Newport formation was thought to be possibly Lower Cambrian (Murray and Skehan, 1979), but the present mapping establishes the rocks as Precambrian. The structure of the area so far has been incompletely described although it has been recognized that the bedded rocks have undergone polyphase deform­ ation (Kay and Chappie, 1976). We have remapped the critical contacts and have established a general sequence of stratigraphic and structural events with special attention being paid to sedimentary facing and extensive refolding. GENERAL SETTING In Newport and Middletown townships (Fig. 1) the Precambrian rocks outcrop in western Newport, in southern Newport on Cliffwalk, and on Sachuest Point and Gould Island of the Sakonnet River (Fig. 1). The western Newport outcrop, being the largest, has been called the Main Outcrop . In the Main Outcrop the metasedimentary strata are folded into over­ turned recumbent folds, while the volcanogenic rocks are in upright folds. In both cases these folds (F^) are refolded by small second folds (F2) . Both sets of folds have axial plane cleavages (Si and S2) but the most pervasive cleavage is the S2 . Contemporaneous and later faults are abundant. The contact between sedimentary and volcanogenic rocks (Table 1) is in most cases a fault although at Stop 4 (Fig. 1) a small outlier of Price's Neck formation grades down into metasedimentary rocks, and in the northern part of Stop 6 (Fig. 1) volcanogenic layers can be recognized as interbeds in the metasedimentary rocks. At both stops and also at Locality A (Fig. 1) the New­ port formation faces into the Price's Neck formation. Therefore, the collect­ ive evidence is that volcanogenic rocks of the Price's Neck formation are younger than the metasedimentary rocks of the Newport formation and that, 68 o . ddllD a> CD 2 * a . o ° <75 ft »• < .i ft 00 c •H £ o rC CO T3 e cd MCO 0) nj O o u CO 0) cd a • cd 4J X u 0) u o p . c OCEAN ts •H a) 2 O U O <U c o •H 0) 4-» M-l <U O a CO cd 0) •H M-l •P o •H rH a * cd cd a 6 o rH rH cd a e •H cd 00 o CO T—1 cx o o 0) u o CO a • •H rH I 4J a) HJ g l rH a) UDIUDAlAsuua^J UDuqiUDO U D iu A jp D H •Hi •H <4-1 4 69 despite the appreciable recumbent early folds, the succession as a whole faces upward. Within the Newport formation the F^ overturned to recumbent folds cause rapid and sudden inversions of sedimentary facing. Price's Neck formation (purple volcaniclastic turbidites and tuffs in felsic volcanogenic sequence) - Units 1-4. member - upper part (diamicite or olistostrome ted graywacke turbidites. Quartzites, dolomite Ft. Adams member - lower part (semipelites with interbedded quartzite and olistoliths). Graves Point member (pelites and siltstones, with thin turbidites and volcanogenic intercalations). Brenton Point member (turbidites, felsic to intermediate pelitic tuff). Castle Hill member (turbidites, slates and tuffs) Table 1. Stratigraphic succession of Newport and Price's Neck formations of Newport and Middletown, Rhode Island (modified from Rast and Skehan, in press, 1981). STRATIGRAPHY On the basis of sedimentary facing, Rast and Skehan (in press, 1981) have divided the Newport formation as follows from the bottom upward: Castle Hill member - This member consists mainly of composite graywacke beds of sandstone and slate 30 cm to 1.5 m thick, the sandy part grading up ■ into slate. Thicker graywacke beds commonly show soft-sediment deformation including chaotic bedding, slump folding, and intraformation shale-fragment breccias. These features suggest that these rocks are fluxoturbidites deposited on a slope. A few beds of conglomerate, limestone, and dolomite concretions are present in restricted parts of the section. Brenton Point member - Upward grading sandstones or turbidites of the type found in the Castle Hill member grade up into thin-bedded siltstones inter- 70 layered with thin felsic volcanic units. The felsic units, that are usually buff weathering and porcellanitic, contain few sedimentary structures except for ubiquitous lamination, and are not traceable for distances greater than several hundred feet. At the contacts with the Brenton Point and Castle Hill members, these volcanic horizons are particularly abundant and show slumping. Graves Point member - This member consists essentially of fine-grained deposits of siltstones, pelites and volcanogenic intercalations. The pelites vary from true phyllites to metasiltstones, are variably gray to green to maroon and contain occasional thin turbidites. The Graves Point member on the western side of the Fort Adams peninsula (Fig. 1) gradually passes to the east into chaotically disturbed rocks of the Fort Adams member. Fort Adams member - This member is comprised of fragments of Mpull-apartM beds and exotic blocks in a fine-grained pelitic and semipelitic matrix. On the eastern side of the Fort Adams Peninsula the member contains elongated fragments of disjointed turbidites, white quartzites, buff weathering calc- silicate rock, and carbonates. In addition, there are rarer fragments of mafic and, at Locality A (Fig. 1), ultramafic rocks. Toward the top, the Fort Adams member passes into volcaniclastic and slaty rocks interbedded with dis­ rupted feldspathic sandstone horizons (Fig. 1, Stop 4). This relationship suggests that the disruption has been produced during the sedimentation rather than tectonically. The tectonic deformation produced particularly chaotic structures as is also seen at Stop 6 . Price's Neck formation - In the Main Outcrop of Newport (Fig. 1), the Price's Neck formation consists of three units, from bottom to top: Unit 1. Agglomerate breccias (in part at least representing lahars) conglomerates, and associated soft sediment deformed coarse tuff. Unit 2. Thinly bedded tuff and laminated sediments with possible rhyolite flows. Unit 3. Graded beds of aquagene tuffs fining upward into siltstones and slates. At Sachuest Point and Gould Island (Fig. 1) a thick unit of essentially volcanogenic conglomerates appears to fine downward into Unit 3. Thus, these conglomerates appear to represent a higher Unit 4 of the sequence. Minor Intrusions In many localities the Price's Neck formation is crosscut by felsic dikes. In the central part of the Main Outcrop a large number of dikes seem to form a stockwork of felsic intrusive bodies that was probably a feeder to the vol canogenic rocks. All formations are cut by later mafic dikes (Moore, 1975). At Locality D on Jamestown (Fig. 1) these dikes crosscut first folds and are folded by the second folds. Therefore, these dikes are post-F1 and pre-F2 . Newport Granite - The intrusive contact of the Newport granite is well exposed in at least three localities: 1) on Cliffwalk between Sheep Point and Lands End, 2) on Cliffwalk at BaileyTs Beach, and 3) near Rogers High School (Loc, E, Fig. 1). The Newport granite, which at Cliffwalk intrudes the olistostrome of the Fort Adams member of the Newport formation, is responsible for widespread contact metamorphic hornfelsing or spotting of both the Newport and Price’s Neck formations of Cliffwalk, and the Price’s Neck of the Main Outcrop. The spotting decreases westward so that most of the metasedimentary rocks of west­ ern Newport are not appreciably contact metamorphosed. The granite, therefore, is later than all the bedded rocks of either the Newport formation or the Price’s Neck formation. The Newport granite is a coarse granitic rock varying in composition betw een true granite and adamellite. In places it is coarsely porphyritic. Internally the pluton is cross-cut by aplites and quartzo-feldspathic pegma­ tites and relatively smaller bodies of fine-grained granite. The intrusion is appreciably deformed and is particularly affected by faults of several ages (Stop 6). It has a whole rock Rb/Sr date of 595+ 12 Ma (Smith, 1978), and in Fort Wetherill, it is cut by mafic dikes of northwest to southeast trend. STRUCTURE The Newport and Price’s Neck formations are involved in two principal fold-generating deformations.
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