.RIFT BASINS OF THE PASSIVE MARGIN: TECTONICS, ORGAN IC-R ICH LACUSTR INE SEDIMENTS, BAS I N ANALYSES

WARREN MANSPEIZER Department of Geology, Rutgers University Newark, New Jersey PAUL E. OLSEN Bingham Laboratories, Department of Biology, Yale University New Haven, Connecticut

Introduction in pull-apart lacust'rine basins. El sewhere platform carbonates The kinematic model provided formed as the Tethys waters by plate tectonics of the earth's transgressed across eroded Her- lithosphere is helpful in reveal- cynian and Acadian mesetas, and ing new hydrocarbon and mineral evaporites of salt and potash provinces. The distribution of formed where waters of the juve- these resources is largely related nile ocean became restricted in to the plate tectonic setting of narrow basins. In both deep marine the basin, i.e. proximity to plate and fresh water basins, oxygen- boundary, type of plate margin, deficient, toxic, near bottom and the nature of the substrate. conditions prevailed preserving Basins currently forming along organic matter as the progenitor divergent plate boundaries, e-g. of hydrocarbons. Some of these the Red Sea, are the sites of basins have characteristics of thick accumulation of hydrocarbons potentially important hydrocarbon and layers of salt, as well as of provinces. metalliferous sediments that were concentrated by hydrothermal pro- Lake Deposits and Hydrocarbon cesses. Provinces: A Brief Review The breakup of North America Today substantial petroleum in the Triassic-Liassic was accom- production comes from lacustrine panied by transform faulting, sequences in China, the Rocky igneous activity and the transgres- Mountains, Europe and Africa (see sion of Tethys into the proto- Ryder, 1980). Among the most in- Atlantic basin. Vast quantities of structive examples from the con- elastics were deposited on allu- text of this trip are those basins vial fans by ephemeral streams, that formed in a lacustrine set- while subaqueous fans and tur- ting during the early rifting bidites accumulated in deep-water phases of the south Atlantic, name- lakes along the border fault, and ly: The Gabon, Cabinda, Congo, subaqueous fissure flows erupted Brazzaville and Angola Basins of the West African Passive Margin Objectives of the Field Trip (Brice and other, 1980; and Brice and Pardo, 19801, and the Recon- Accordingly, this field trip cavo Basin of Eastern Brazil will focus on the following ques- (Chignone and E Andrade, 1970). tions: (1) What are the major While production in these basins trends in sedimentary and volcanic is mainly from Early Cretaceous facies?; (2) How can the sedimento- fluvial-deltaic sandstones and logic-volcanic and structural data non-marine carbonates flanking the be understood in terms of major margins of the basin, organic-rich features of Newark Basin genesis?; deep-water lacustrine sediments (3) How can we discriminate among provide the source for the hydro- the principal lacustrine models, carbons. such playa-lake-sabkha vs. the stratified-deep-lake model?; (4) Organic-rich lacustrine sedi- What are the causes of the ments also comprise a major part lacustrine cycles?; and (5) How of the Triassic and Jurassic can the concepts of energy dyna- sections in Newark-type basins of mics in modern lakes be related to North America and Morocco. In some the depositional history of Newark basins, lacustrine deposits con- Basin's Great Lakes and Potential tain up to eight percent organic hydrocarbon production? carbon (Manspeizer and others, 1981). Like the producing horizons Answers to these and other of the West African basins, these questions will be explored through beds formed in deep lakes with examination of Triassic-Jurassic perennial anoxic botton condi- stratigraphic sections along two tions. Laterally they may inter- traverses of the Newark Basin (Fi- finger with non-marine shelf gure 1). carbonates and turbidite-generated sediments from near-shore fan- NEWARK BASIN deltas and fluvial-deltaic com- plexes. Cyclical lacustrine se- Overview quences, recording the expansion and contraction of very large Resting with a profound lakes, characterize these beds. unconformity, in a series of about Like the Green River Shales, micro- 20 elongated basins. along the laminated sediment with well-pre- crystalline core of the Older served whole fish from the center Acadian and Alleghany Orogenes of the basin are widespread. Be- from Nova Scotia to North Caro- sides numerous species of fish, lina, is a thick section of con- these lake beds abound with amor- tinental elastics and igneous phous algal kerogen, zooplankton, rocks, termed the Newark Super- pollen and spores, and plant cut- group (Figure 2, Table 1). In icle (Olsen, 1980). These organic- general, the long axes of these rich micro-laminated sediments are basins parallel the fabric of the the result of depressed ecological basement rock (Rodgers, 1970; Van efficiency in enormous highly Houten, 1977). Rocks within these productive lakes. basins are overlain by post-Juras- sic sediments of the coastal Having formed in pull-apart Plain, Pleistocene deposits or basins on the passive margin, Recent alluvium and soils. these rocks display a variety of structural and stratigraphic traps The Newark Basin (Figure 3) and should be given serious con- is the largest of the exposed sideration in future exploration basins and covers about 7770 programs. square kilometers, stretching 220 km along its axis. The basin con- m); Oran e Mountain Basalt (maxi- tains the thickest sedimentary +20% m); Towaco Formation sequence of any of the exposed maximum 340 m); Hook Mountain basins and correspondingly con- Basalt (maximum 110 m); and Boon- tains the most extensive strati- ton Formation (maximum +500 m). graphic record. Each Formation is characterized by its own suite of rock types, the Precambrian and early differences being especially ob- Paleozoic rocks of the south- vious in the number, thickness, western prongs of the New England and nature of their gray and black Upland border the Newark Basin sedimentary cycles (or lack there- along its northeast and northwest of). margins (Figure 3). The south- eastern and southwestern portions Fossils are abundant in the of the Newark Basin overlie and sedimentary Formations of the are bordered by Paleozoic and Pre- Newark Basin and provide a means cambrian rocks of the Blue Ridge of correlating the sequence with and Piedmont Provinces. Newark other early Mesozoic areas. The Basin sediments rest with a pro- Stockton, Lockatong, and most of found unconformity on basement the Passaic Formation are Late rocks and most dip 5 - 25 to the Triassic (Middle and Late Carnian- northwest. The entire strati- Rhaetic) while the uppermost Pas- graphic column reaches a cumula- saic Formation (at least lc:~c-t.i?".;. tive trigonometrically calculated and younger beds appear to be thickness of over 10,300 m (the Early Jurassic (Hettangian and sum of the maximum thicknesses of Sinemurian) in age. The distribu- all the formations), although the tion of kinds of fossils is inti- total thickness of sediments mately related to sequences of actually deposited at any one spot rock types in sedimentary cycles. was probably much less. Red clas- The brief descriptions of these tics are the dominant sediments; formations, extracted from Olsen intrusive and extrusive tholeiites (1980a1, follows: are the dominant igneous rocks. Stockton Formation The oldest sediments are probably middle Carnian (early The Stockton Formation is the Late Triassic) in age while the oldest and most widespread depo- youngest appear to be Sineumurian sit, forming the basal beds of the (middle Early Jurassic) (Cornet, Newark Basin section everywhere 1977; Olsen, McCune, and Thornson, except along portions of the north- in press) (Figure 4). Cretaceous west border. The Stockton is thick- and younger Coastal Plain deposits est near the Bucks-Montgomery overlap Newark beds with an angu- county line in the Bucks-Hunterdon lar unconformity along the basin's fault block (Figure 3), where it eastern edge. The northern quarter reaches a calculated stratigraphic of the basin is mantled by Pleisto- thickness of 1830 m (Willard, et cene and recent deposits. al., 1959). Along its type section Table 2) along the shores of the Newark supergroup deposits of Delaware River near Stockton, New the Newark Basin (New York, New Jersey, the Formation is 1500 m Jersey and Pennsylvania) are thick (McLaughlin, 1945). Measured divided into nine formations from the base of the lowest conti- called ( from bottom up) : Stockton nuous black siltstone unit of the Formation (maximum 1800 m); Locka- overlying Lockatong formation, the tong Formation (maximum 1150 m); Stockton thins in all directions Passaic Formation (maximum 6000 from this central area (Kummel, 1897). The pre-deformational shape Lockatong Formation of the Stockton Formation litho- some is an asymmetrical lens with The beds of the Lockatong the thickest portion near the Formation rest conformably on the center of the Bucks-Hunterdon Stockton Formation over most of fault block. McLaughlin (in Wil- the Newark Basin. The Lockatong is lard, et al., 1959) presents evi- composed primarily of gray and dence that the Stockton Formation black siltstones arranged, as in the southern Newark Basin thins shown by Van Houten (1962, 1964, by a progressive onlap of younger 1965, 1969, 19771, in sedimentary Stockton beds onto basement. cycles. In the Bucks-Hunterdon fault block, near the Lockatong's Stockton lithology is di- type section along Lockatong verse. The dominant sediment types Creek, the Formation reaches its are gray and buff colored arkose maximum thickness of 1150 m (Fi- and arkosic conglomerate, and red gure 3 ) . The Formation thins in siltstone and arkosic sandstone. all directions away from this cen- In broad view, the Stockton Forma- tral area (Figure 5, passing into tion fines upward with the coars- Passaic and Stockton Formations est sediments near the base. As along exposed edges of the Newark noted by McLaughlin ( In Willard, Basin. et al., 1959) the Stockton coars- ens in the same direction it Van Houten (1962, 1964a,b, thins; thus conglomerate bodies 1965, 1969, 1977) recognizes two and coarse arkose are found high end-members to the range of short in the section along the eastern cycle types present in the Locka- edge of the basin. tong; he terms these detrital and chemical. In the Delaware River Red siltstones of the Stock- section of the Formation the detri- ton Formation are characteris- tal cycles are an average of 5.2 m tically intensively bioturbated by thick and consist of a lower platy roots and burrows, notably the black calcareous siltstone suc- arthropod burrow Scoyenia (see ceeded upwards by beds of dis- Olsen, 1977). Purple and Mauve rupted dark gray, calcareous silt- siltstone beds with a markedly stone, rippled-bedded siltstone, disrupted fabric occur near the and fine sandstone (Figure 6 ) . In middle and top of the formation. the same area, chemical cycles These beds are usually densely average 3.2 m. thick. Their lower penetrated by roots, but rarely beds consist of platy black and burrowed by Scoyenia. Beds of dark gray dolomitic siltstone, greenish-gray and brown carbonate- broken by shrinkage cracks, and rich pellets occur throughout the containing lenses of pyritic lime- Formation. These are often stone. The upper beds are massive associated with bases of buff gray or red analcime- and car- arkose beds. Well-bedded gray and bonate-rich siltstone, intensively gray-green siltstone beds are pre- and minutely disrupted. The mas- sent locally in the upper Stock- sive beds often contain pseudo- ton, and these beds are the source morphs af ter analcime and of most of the Stockton fossils glauberite. found so far. How these units, which are unusual compared to the In the central Newark Basin, build of the Stockton sequence, the two cycle types occur in fit in the overall facies pattern clusters; the center of each remains obscure. detrital cycle cluster is about 107 m from the next. Detrital Passaic Formation cycle clusters are separated by clusters of chemical cycles. The predominantly red Passaic Again, in vertical section, there Formation is the thickest coherent are more detrital cycles in the lithologic unit in the Newark lower than in the upper Lockatong. Basin, reaching a maximum calcu- Evidence gathered so far indicates lated thickness of over 6000 m that individual detrital cycles (Jacksonwald) Syncline. The Forma- can be traced for over 20 km. tion outcrops throughout the Judging from the outcrop pattern Newark Basin, although is upper of detrital cycle clusters in the beds are preserved only in the upper ~ockaton~and lower Passaic Watchung Syncline (Figure 31, in Formation, it seems likely that the smaller synclines preserved individual detrital cycles can be along the eastern side of the traced basin-wide. Chemical cy- Flemington Fault, and in the cles, on the other hand, are pre- Jacksonwald Syncline (Figure 3). dominantly restricted to the cen- In all other areas, the upper Pas- tral 97 km of the Newark Basin, saic has been removed by post- passing laterally into beds indis- Newark erosion. tinguishable from the Stockton and Passaic Formations. At the south- While in most areas the Pas- western end of the Newark Basin at saic Formation rests conformably Phoenixville, Pennsylvania, the on Lockatong Formation or, where Lockatong is 350 m thick; the that is absent, Stockton Forma- Formation consists of clusters of tion; in several areas on the detrital cycles separated by red western margin of the Newark Basin siltstone and some beds of gray the Passaic directly overlaps the sandstone. At the northeastern end step-faulted basement without any of the Newark Basin at Weehawken, intervening Stockton or Lockatong. the Lockatong is 150 m thick and In these areas (Figure 5) the consists of detrital cycle clus- thickness of Passaic Formation ters separated by beds of buff present below the Orange Mountain arkosic sandstone. The large num- Basalt is comparatively slight. ber of detrital cycles prevalent in the lower Lockatong in the cen- Facies patterns of the Pas- tral Newark Basin strongly sug- saic Formation are a modified gests that the Lockatong outside continuation of those of the Locka- of its thickest central portion tong, although red beds, not gray comprises only the lower 500 m of are the dominant lithology. As in the Lockatong or less (not includ- the Lockatong, periodically spaced ing the lower 30 m of red silt- clusters of detrital cycles (Fi- stone grouped here in the Stock- gure 5) occur through most of the ton). The thickness of the Locka- thickness of Passaic Formation tong decreases away from the cen- Van Houten, 1969). The great tral Newark Basin not only by majority of these non-red units, replacement of its upper beds by however, are not as laterally con- Passaic Formation but also by the tinuous as those of the Lockatong, thinning of individual detrital and as a general trend, it is cycles. While the mean detrital clear that the number of cycles cycle thickness is 5.2 m along the involved in these clusters de- Delaware River, for example, it is crease in frequency upwards 1.5 m along the Hudson River (see through the Passaic Formation. Olsen, 1980b) (Figure 5). Orange Mountain Basalt per flow is extensively pillowed and pahoehoe-like near the type The Orange Mountain Basalt is section (Fenner, 1908; Van Houten, the oldest Newark Basin Formation 1969) and locally at isolated thought to be wholly Early Juras- spots throughout the Watchung syn- sic in age, and like similarly cline. Subaqueous tissue flows and aged beds in the Newark Basin, the flow lobes are common in the Pater- main area in which the basalt is son area, and will be studied on preserved is the Watchung Syncline the field trip. (Figure 3). Smaller synclines preserve portions of the Orange Feltville Formation Mountain Basalt in several other regions. In the New Germantown and The sedimentary rocks above Sand Brook synclines, the overly- the Orange Mountain Basalt and ing Feltville Formation is pre- below the Preakness Basalt are served above the basalt. Correla- termed the Feltville Formation tion by palynomorph assemblages (Olsen, 1981). The Feltville con- and fossil fish of the overlying sists of red siltstone and sand- Feltville Formation (Cornet, 1977; stone, buff, gray, and white feld- Olsen, McCune, and Thomson, in spathic sandstone, and a thick, press) demonstrate the identity of laterally continuous non-red unit the underlying basalt. Taken to- containing a unique laminated lime- gether, these remnants of Orange stone (Figure 6). This formation Mountain Basalt suggest that is named for the old village of originally the basalt covered the Feltville, Union Country, New entire Newark, Basin, a minimum of Jersey, where the type section is over 7700 km . This is comparable located. to the extent of the Holy Basalt over the Hartford Basin and the The Formation averages about North Mountain Basalt over the 180 m in the Watchung Syncline, Fundy Basin. The Orange Mountain apparently thickening to 300 m in Basalt appears thickest in the the Sand Brook and 600 m in the

Watchung Syncline, varying between Germantown Syncline. More than 200 , 100 and 200 m. m seems to be present in the Jack- sonwald Syncline. Two thick flows are evident in most sections of the Orange The Feltville Formation is Mountain Basalt, at least in the distinguished from the underlying Watchung and New Germantown Syn- Passaic Formation and the younger clines. The lower flow is exposed Jurassic Formations of the Newark at the type section where it shows Basin by the presence of abundant a nearly complete Tomkeieff struc- beds of buff , gray, or white feld- tural sequence (Manspeizer, 1969). spathic sandstone interbedded with Other exposures of the lower flow red siltstone in fining-upwards are abundant. In most places the sequences (Olsen, 1981a); thus, lower and upper flows are sepa- much of the Feltville super- rated by a red volcanoclastic bed ficially resembles the Stockton which is generally less than a Formation. The lower half of the meter thick (Bucher and Kerr, Feltville contains a black to 1948; Johnson, 1957; Van Houten, white laminated limestone, cal- 1969; Faust, 1975). In the New carenite, and graded siltstone bed Germantown Syncline, however, the 0.4 - 3 m) containing abundant volcanoclastic bed is over 4 m fossil fish. This is sandwiched thick and has numerous beds of pur- between two beds (each 1-7 m) of ple, red, and gray ripple-bedded gray, small- to large-scale cross- and mudcrakced siltstone. The up- bedded siltstone and sandstone. As is true for the Formation as a (Manspeizer, 1980). In other areas whole, these beds are thickest in there are thick beds of angular the New Germantown Syncline (+I4 and vesicular basalt breccia m). resembling aa. In still other areas the thick massive lower flow Conglomerate occurs in the rests on the flat Feltville Forma- Feltville Formation at Oakland, tion surface (Lewis, 1908). New Jersey, about 15 m below the Preakness Basalt (Faust, 1975). Towaco Formation This conglomerate contains as much as 30% vesicular basalt clasts, in The name Towaco Formation is addition to cobbles and pebbles, applied to the red, gray and black slate, and limestone. Very little sedimentary (and minor volcano- of the section below this unit is clastic) rocks present below the exposed, and at this point it is Hook Mountain Basalt and above the impossible to say how much addi- Preakness Basalt in the Watchung tional conglomerate is present. Syncline (Olsen, 1981). Other beds of conglomerate crop out in the New Germantown syncline Laterally continuous symmetri- in association with the non-red cal sedimentary cycles charac- laminated beds. The available evi- terize most of the Towaco Forma- dence suggests that the Feltville tion (Figure 6). These consist of Formation, like the Orange Moun- a central black or gray micro- tain Basalt, originally occupied laminated calcareous siltstone the whole of the area of the bounded above and below by gray Newark Basin; the predeformational sandstone and siltstone beds shape of the Feltville lithesome arranged in fining-upwards cycles. seems to have been a wedge, thick- These symmetrical cycles are a est along the western border of mean of 35 m thick and bear a the basin. The data are not con- close resemblance to the East clusive, however. Berlin Formation (Hartford Basin cycles described by Hubert, Reed, Preakness Basalt and Carey 1976 1 . Towaco cycles are an order of magnitude thicker than Preakness Basalt consists of Lockatong or Passaic Formation the extrusive, tholeiitic basalt detrital cycles and differ from flows and interbedded volcano- the otherwise similar Feltville clastic beds above the Feltville Formation non-red unit in contain- Formation and below the Towaco ing predominantly clastic rather Formation (Olsen, 1981). Preakness than carbonate laminated portion Mountain is the local name of the (Figure 6). In total, six such second Watchung Mountain near cycles have been identified in the Franklin Lakes, New Jersey. upper half of the Towaco Formation and most of these have been traced Preakness Basalt is the thick- through the Watchung Syncline. est extrusive unit in the Newark Basin. The calculated thickness is Beds of conglomerate occur at 215 m at its northernmost outcrops numerous horizons through the at Pomptom and Oaklane, New Jersey. Towaco Formation at Pompton, New Jersey. Not only is conglomerate At its base, the Preakness present directly below the Hook Basalt is much more variable than Mountain Basalt in this area the Orange Mountain Basalt. Local- (Fault, 19751, but thick conglom- ly, there are thick sequences of erate beds also occur at intervals multiple basalt flows making up of about 120-150 my 160-170 my possible basalt foreset beds 185-195 my 205-229 my and 270-280 m below the Hook Mountain Basalt ferent colors and textures of (Figure 6 . these beds do not seem to be arranged in any obvious or con- Hook Mountain Basalt sistent cyclic pattern and resem- ble no other units in the Newark The uppermost extrusive unit Basin. Stratigraphically above in the Watchung syncline is called these lower beds is a sequence of the Hook Mountain Basalt (see well-bedded red siltstones and Baird and Take, 1959. The Hook sandstone beds (mean thickness 35 Mountain Basalt is the thinnest of m) alternating with thinner beds the three major extrusive Forma- of gray-green siltstones (mean tions of the Newark Basin. At its thickness 2 m). The uppermost beds type section, it is 110 m thick of the type section include a fos- and it retains this thickness sil fish bearing calcareous gray throughout the Watchung Syncline. microlaminated siltstone at least That this basalt extends in the one meter thick (Smith, 1900). subsurface across the gaps between This is the famous Boonton Fish Hook Mountain and Riker Hill, and Bed (Newberry, 1888; Schaeffer and between Riker Hill and Long Hill McDonald, 1978). Also in this sec- is shown by the bedrock topography tion are gray and brown conglom- maps of Nichols (1968) and the erate units up to 0.5 m thick. aeromagnetic data of Henderson, et Along the western edge of the al. (1966). In the area of Watchung Syncline, northeast of Bernardsville, New Jersey, what Morristown, New Jersey are thick has been mapped (Lewis and Kum- sequences of red-, gray-, and mell, 1910-1912) as part of the brown-matrix conglomerate and Preakness Basalt is in fact Hook breccia. The relationships of Mountain, as shown by unambiguous these units to the finer portions exposures of Towaco Formation of the Formation are unclear. between it and the underlying basalt . Diabase Instrusions Boonton Formation Large diabase and gabbro plutons and sills are emplaced The Boonton Formation is the through various portions of the youngest sedimentary unit in the pre-Orange Mountain Basalt section Newark Supergroup sequence of the of the Newark Basin sequence. The Newark Basin and consists of more areal extent, petrography and con- than 500 m of red, brown, gray and tact relationships of these masses black fine to coarse elastics and are, for the most part, well known minor evaporitic beds (Figure 6). (Darton, 1890; Kummel, 1897, 1898; Lewis, 1908; Lewis and Kummel, The stratigraphically lowest 1910-1912; Willard, et al., 1959; beds in the Boonton Formation are Hotz, 1952) and will not be de- well exposed near Bernardsville, scribed in detail here. These New Jersey. In this area, the Forma- bodies generally parallel the dis- tion consists of blocky to finely tribution of major bodies of gray bedded red, gray, brown and black, and black siltstones; thus the often dolomitic siltstone. This largest intrusives are broadly con- 104-meter thick lower unit is rid- cordant (but locally discordant) dled with hopper casts (pseudo- to the Lockatong Formation (i.e., morphs after gypsum, glauberite, Palisade, Rocky Hill, and Sourland and halite) which are common in Mountain sills) or the Perkasie sequences of all colors. Similar Member of the Passaic Formation beds are exposed along Packanack (Haycock Mountain, Coffman Hill, Brook, Wayne, New Jersey. The dif- and possibly the Cushe tunk Pluton). The general pattern is complex transtensional and trans- for these intrusions to be em- pressional structures, such as placed progressively higher in the en-echelon cojugate fractures and Newark Basin section viewed along folds, and isolated basins with an east to west section (Figure complicated unconformities and 5). Like most Newark Supergroup sedimentary overlap. deposits, Newark Basin beds are cut by a number of narrow, often What data can we cite to sup- straight and vertical diabase port this view of the Newark dikes which, in this area, trend Basin? The following is extracted north and northeast. The mapping from Manspeizer (1981, and ms): of the distribution of these dikes is still very incomplete (see 1) The fundamental structures of King, 1971, and May, 1971, for wrench tectonics, including en- reviews) . echelon folds, conjugate strike- slip faults, the main wrench fault BASIN TECTONICS zone, and en-echelon normal faults, are shown on Figure 3. Beginning with the studies of Note particularly the Hopewell and Rogers (1858) in Pennsylvania and Flemington faults, which are en- Davis (1886) and Barrel! (1915) in echelon right-lateral oblique Connecticut, Newark-type basins faults that may have up to 12 were considered grabens or fault miles of horizontal slip, and the troughs produced by extension at Chalfont fault, a possible major right angles to the rift axis. To- left lateral fault. day many of these same basins have been assigned to the initial phase 2) Syntectonic development of of the Atlantic tectonic cycle, both transtensional and transpres- and display tectonic structures sional structures occur along the and facies characteristic of border fault, leading to a complex rhomb-shaped pull-apart basins set of drag folds, unconformities that formed within transforms due and basins (see Ratcliffe, 1980; to horizontal shear (see and Manspeizer, 1980). Manspeizer, 1980; and 1981). 3) Moderately deep-water fissure As crustal plates move past eruptions with pillow lavas and each other along transform bound- volcanic flow lobes restricted to aries, different types of pull- rhombochasms (?) near the axis of apart basins may form in zones of the basin. crustal extension. In as much as the crust may have been heated by 4) Pronounced asymmetry of the hot spot activity (e.g. the White sedimentary basin and sedimentary Mountain Magma series), the walls facies with deep-water lacustrine and floors of these basins may deposits typically along the bor- have been stretched so that in der fault, and fluvial-deltaic time they sag and collapse forming sediments along the eastern Pied- basins. Where the basement has mont Province. been pulled apart creating rhombo- chasms, diapirs of magma may enter 5) progressive I I younging" of the basin floor in the form of Triassic and Jurassic sediments in dikes and flows. Differential the direction of the western mar- horizontal movement along an ac- gin of the basin. tive fault zone may create an asym- metric basin, as in the Dead Sea 6) The absence of a continuous Rift. Continuous wrench faulting system of faults along the margins along the transform may produce of the basin, indicating that the earliest phases of sedimentation (Manspeizer, 1969). These flows may have begun on a downwarped may have fractionated from a crust prior to faulting. typical Mid-Atlantic Ridge basalt magma (Puffer and Lechler, 1980). 7) The predominance of slicken- sides with a horizontal neat along Most of the lavas were em- the western border fault. placed as multiple flows through a series of lava tunnels and tubes IGNEOUS ROCKS that occasionally arched and pierced the overlying pahoehoe Tholeiitic basaltic lavas and shell. Some flows were emplaced as intrusives of Early Jurassic age deep-water (lacustrine) pillow clearly mark and distinguish the lavas, fissure eruptions and vol- upper part of the stratigraphic canic breccias in rhombochasms (?I sequence in the onshore and off- of pull-apart basins (Figures 8 shore basins of eastern North and 9). America. These rocks were emplaced over a vast area, perhaps 2500 km Pillow Lavas, Subaqueous Flow long and 1000 km wide, during an Lobes and Rhombochasms (?I episode of crustal extension and sea-floor spreading, and therefore One of the most striking fea- exhibit a variety of structures tures of moderately deep-water reflecting the complex history of Recent basaltic volcanism is its the basin at that time (Figure 7). abundance of pillow lavas (Jones, Some of these structures, studied 1966). Current investigations of on the field trip, are described the FAMOUS expedition (Heirtzler below. and Bryan, 1975; Choukrone and others, 1978) show that pillow While the intrusive sheets lavas and pillow rubble comprise such as the Palisades Sill and the an important component of the Mid- Rocky Hill-Lambertville sheets Atlantic Rift facies. While the extend collectively throughout main deeps of the rift are often much of the basin, the volcanics buried by considerable rubble, are restricted to the Jurassic sec- pillows form on adjacent highs tion (Figure 3). Paleoflow data away from the center of tectonic (Manspeizer, 1969) and geochemical activity from flows erupting from data (Puffer and Lechler, 1980; volcanic vents and fissures. and Puffer and others 1981) show that the First and Second lava Pillow lavas occur exten- flows, now preserved as erosional sively throughout the upper flow remnants in the north, originally unit of the Orange Mountain Basalt extended 80-150 km south to their and in the lower flow unit of the probable source in the eastern Preakness Basalt. They are best part of Pennsylvania. Field stu- exposed in several trap quarries dies also show that these lavas in the Paterson region, where extended west of the Ramapo border according to Fenner (19081, they fault. While First and Second formed in the lacustrine setting Watchung lavas erupted from of Lake Paterson. In the New sources in the southwestern end of Street Quarry of Paterson, long a the basin, vector means calculated favorite collecting site for mine- from pipe vesicles indicate that ral hobbyists, pillow lavas are the Third Watchung erupted from an abundant, occurring in two distinc- unknown area to the northeast of tively different facies: (1) a the basin and flowed to the south- subaqueous flow lobe, and (2) west in the direction of the bedded pillow lavas. (Figures 8 regional sedimentary paleopslope and 9 . The subaqueous flow lobe, is generally massive and only very sketched in (Figures 8 and 9) from slightly and minutely vesicular. the walls of two adjacent quarries Vesicularity and vesicle size, and a roadcut, is about 400 m long according to Moore (1965) and and 35 m high with an apparent Jones (1969), is an index of the long axis oriented east-to-west. depth of water in the formation of Its upper surface slopes gently pillows. The pillows of Lake Pater- westward 5' - lo0, while its dis- son have few microvesicles and may tal end and flanks are extremely have formed in moderately deep steep and slope 35 - 40. Its water. This avenue of research is shape is a broadly flat-topped currently being investigated. tongue or lobe that flares out along its distal end to the west. The absence of rubble is an The lobe overlies the vesicular important and notable attribute of and tuffaceous upper surface of the pillows suggesting that the the lower flow unit and appears waters of this basin were well- conformably overlain by an exten- agitated and that the finely com- sive horizon of bedded pillows and minuted clasts were washed into massive columnar basalt. the deeper part of the basin per- haps along the border fault. (See The distal western end of the Choukroune and others, 1978, Fi- flow lobe is overlain by the gure 6). Considerable volcanic younger set of subaqueous fissure breccia and fissure eruptions are eruptions which feed a younger set found at the Haledon Quarries of pillows. north of Paterson (D. Bello, Oral Comm. ) . Pillows of the bedded and lobe-type form interconnected Fenner (1908) determined that ellipsoidal masses that are dis- the minimum size of the lake basin torted, kneaded and flattened like was in the order of 8 km long, half-filled sacks in a tight struc- that is from Montclair to North tural framework without matrix but Haledon where the beds are con- with open interstices. The inter- cealed by glacial cover. Field stices have irregular shapes and data, however, show that similar are filled with small angular rifting and volcanism may have fragments of basaltic glass that occurred concurrently in isolated are completely surrounded by and basins from Ladentown, New York cemented with secondary zeolites, south to Feltville, New Jersey, a calcite and quartz. It is clear distance of about 75 km. The that the clasts were derived from presence of volcanic vents, suba- the glassy and checkered rind of queous flow lobes, moderately the pillows by circulating second- deep-water pillow lavas within ary solutions that displaced the down-dropped blocks causes us to glassy rind by their mineraliza- speculate whether a short-lived tions. In transverse section the juvenile ocean basin hadn't formed pillows are almost circular and for a brief moment here during the display well-developed radial Early Jurassic (Figure 10). and/or concentric joints. Concen- tric layering and blocky joint Zeolites patterns accompany longitudinal sections, which are markedly ellip- The trap rocks of the Pater- tical with long axes to short axes son region with their spectacular ratios in the order of 3:2. While array of zeolites and associated the exterior rind of the pillows minerals have been favored by are cracked in the form of check- mineralologists and hobbyists for ered glass selvage, the interior over 150 years. These minerals enrich museums and private collec- stices of pillows suggests that it tions throughout the world and was washed away, leaving open chan- their quality and diversity rank nels for subsequent mineralization with similar collections from Nova by ground water solutions. There- Scotia, Iceland and the Deccan of fore, it seems unlikely that the India (Mason, 1960). As early as zeolites formed in shallow water 1822 Nutall recorded the occur- playas. rence of prehnite, natrolite, chabazite, stilbite, and datolite Columnar Jointing from quarries in the first Watchung Basalts (Mason, 1960). A spectacular joint system, Among the zeolites, Bucher and marked by a lower and upper colon- Kerr (1948), report that stilbite, nade with a central entablature, analcime, natrolite, laumontite, is the single most consistent and thaumasite, chabazite and heulan- prominent feature of the lower dite are probably the most fre- flow unit of the First Watchung quently found, and that they occur basalts (Figure 7). It is remark- most often with quartz, calcite, able that this three-fold joint datolite, prehnite, pectolite and pattern may be observed for a dis- apopyllite. Of the sulphides, tance of almost 80 km along pyrite and chalcopyrite occur more strike. It marks a uniform flow frequently than galena and born- condition and cooling history over ite. Among the sulphates, gypsum a vast area, suggesting that the occurs rarely. lava was ponded. It is unlikely that these ponded lavas could have In the past, as basalt quar- reached far beyond the northern ries were actively worked for the limits of the current basin. First trap rock, good crystals could be described almost 100 years ago 'by found in newly opened quarry Iddings in 1886, these structures faces. Today there are no operat- are equal in prominence to those ing trap quarries in Paterson, described by Bailey (1924) of the therefore, mineral collecting is Mull Province, Tomkeieff (1940) of almost non-existent. the Devil's Causeway, and Waters (1960) of the Columbia River The presence of cavities and Basalts . pseudomorphs after glauberite and anhydrite within the pillow com- This joint system is most com- plex at Paterson and in the mud- pletely exposed along Interstate stones below the lavas led Route 280 in West Orange, near the Schaller (1932) to suggest that site of the O'Rourke Quarry de- the zeolites formed only when the scribed by Iddings in 1886 (Mans- second flow unit entered into a peizer, 1969). The structure, over- saline lake. Van Houten (19691, lying a fluvial red bed sequence however, suggests that the pil- of shales and sandstones, consists lowed lava and underlying vesi- of: (1) a lower colonnade; (2) an cular lava at Paterson were miner- entablature; and (3) an upper alized after burial by circulating colonnade. The lower colonnade, ground water, perhaps derived about 15 km thick, is composed of largely from the compaction and massive 4-5 or 6-sided polygonal dewatering of the underlying mud- subvertical joint prisms up to 13 stones. m high and 0.5 - 1.2 m wide. The entablature consists of long (20 Pillow lavas and pillow- to 30 m), slender, slightly un- derived debris are important rock dulating curved polygonal columns components in modern oceans. The that pinch and swell, and radiate absence of debris in the inter- from the aspices of wide-angle cones that form upright, inverted almost everywhere in the upper and oblique fans and chevron struc- colonnade may be the result of con- tures (see Spry, 1961, p. 195). vective heat loss near the upper Sheafs of curved downward radiat- part of the flow.Other explana- ing fans and chevrons are signi- tions offered for the origin of ficantly more abundant than upward the curvi-columnar jointing in the radiating structures by a factor entablature of the First Watchung of perhaps 10:1. Cross joints, basalts include: (1) an undulatory intersecting the radiating columns upper surface (Iddings, 1886; at high angle, appear concen- Manspeizer, 1969); (2) varying trically distributed about the rates of cooling at the upper con- apex of radiation. The density of tact (Iddings, 1886); (3) the joints, as manifested by the long occurrence of feeder dikes (Bucher slender prismatic olumns, is the and Kerr, 1948); (4) the effects key factor differentiating the of master joints upon stress in entablature from the colonnades. the entablature (Spry, 19711, and While the entablature of the First a fracture-controlled quenching Watchung is curvi-columnar, in the process whereby temperature and Second Watchung it is characteris- stress distribution are altered by tically composed of very long water introduced through joints (about 25 m) and fairly contin- (Justus and others, 1978). This uous, slender (about 10 cm in issue, and the observations by diameter), non-radiating parallel Ryand and Sammins (1978) are fur- columns that are perpendicular to ther discussed in the Road Log. the flow surface. Poorly developed blocky columns and massive basalt LACUSTRINE CYCLES of the upper colonnade overlie the entablature in most areas. Lockatong Formation, Detrital Cycles Petrographically (Manspeizer, 1980) the curvi-columnar joint pat- The Lockatong Formation is tern of the entablature is charac- composed almost entirely of well- terized by an increase in grain defined sedimentary cycles. Of the size, an increase in the abundance two short cycles described by Van and size of the interstitial Houten, chemical and detrital , glass, and the virtual restriction only the latter will be discussed of olivine to this zone (Figure here; they resemble not only 11). These relationships suggest cycles found higher in the Newark that although the rate of cooling Basin section, but also lacustrine of the hot flow interior may have sequences of other Newark Super- proceeded slowly, once a ground group basins. mass capable of transmitting stress was established the remain- As originally noted by Van ing silicate melt cooled almost Houten, Lockatong detrital cycles instantaneously. The greater rate clearly reflect the expansion and of cooling near the center of the contraction of lakes. Recent study flow would produce more fractures of these cycles shows that each per unit volume and a greater can be split into three lithologi- release of the total energy in the cally identified divisions (Figure system (Spry, 1961). The clarity 12) from the bottom up: 1, a thin of joint reflection from the lower (0.5 m) platy to massive gray silt- colonnade into the entablature stone representing a fluvial and indicates that joint propagation mudflat to lacustrine (transgres- proceeded along master joints, as sive) facies; 2, a microlaminated suggested by Spry (1961). The to coarsely laminated black to obscure joint pattern observed green-gray fine, often calcareous siltstone (0.1-1.0 m) formed dur- General Comments ing maximum lake transgression; and 3, a generally thickly bedded About 3150 m above the early or massive gray or gray-red silt- Late Triassic Lockatong Formation, stone or sandstone (0.5-4.0 m) is the first laterally extensive usually showing a disrupted fabric perennial lake sequence in the and current bedding and sometimes Early Jurassic (Hettangian) of the bearing reptile footprints and Newark Basin. The Feltville Forma- root horizons (regressive facies). tion contains a limestone-bearing sequence which bears a gross resem- If individual detrital cycles blance in vertical sequence to a can be traced over the extent of single Lockatong detrital cycle the Lockatong Formation, the area (Figure 6). It can be split into of division 2 of each cycle is a three basic divisions at most expo- measure of the average minimum sures as follows (Figure 13) (from size of the lake during maximum the bottom up): 1, a 0 to 3 m gray tr ns ression; this is about 7000 to red siltstone and fine sand- km9 . stone showing current bedding, root zones, abundant reptile foot- Vertical sections through prints, and carbonized megafossil Lockatong cycles show consistent plants (transgressive facies); 2, lateral trends in lithology and a 0.5 to 5 m black, gray or red paleontology. Detrital cycles and green-gray microlaminated to traced away from the geographic massive limestone and calcareous and depositional center of the siltstone with abundant fossil Newark Basin show changes in fish and graded to massive silt- faunal and floral assemblages due stone similar to division 1 but to deposition in progressively with fewer footprints (regressive shallower water. In addition to facies). Division 1 grades down lateral change in facies, there is into, and division 3 grades up in- a correlated change in cycle thick- to red and buff elastics. Like ness (see Figure 12). For in- Lockatong cycles, the Washington stance, along the Delaware River Valley member was deposited by the (at the geographic and deposi- expansion and contraction of a tional center of the basin), the large lake. mean thickness of detrital cycles is 5.2 m (Van Houten, 19691, while Lateral facies relationships in the northern Newark Basin this in the Washington Valley member thins to 1.5 m (Figure 11). The are very different from Lockatong microlaminated sediments of divi- detrital cycles despite the simi- sion 2 are made up of couplets of larity in vertical section (Figure laminae, one of which is more 14). On a small scale, the Washing- calcareous than the other (in ton Valley member shows lateral their unmetamorphosed state) (Fi- variation in thickness and lith- gure 12). Similar sediments are ology far outside the range of produced in a variety of modern Lockatong cycles. Thickness lakes; in most of the studied changes markedly along strike as cases the couplets are the result does color. Within 300 m in the of seasonal variation in sedimenta- Watchung Reservation (type area tion and are thus varves (Nipkow, for the Feltville Formation) the 1920, 1927; Kelts and Hsu, 1978; color of the limestone of division Tolonen, 1980) 3 changes from gray and black to white and green gray and the color Fletville Formation of fish bone changes from black to amber. Siltstones associated with Washington Valley Member - all three divisions change from gray to red in the same area, but gray clastic unit similar to divi- all the beds still retain palyno- sion 1 (regressive facies); and 4, morphs and black coalified plant a thick 20 - 30 m) red clastic remains. The thickness of the red sequence often composed of several siltstone between the Washington fining upwards cycles containing Valley member and the underlying abundant reptile footprints, root Orange Mountain Basalt varies horizons, mudcracked surfaces, and markedly along strike as well; at beds with numerous carbonate rich some localities division 2 rests nodules (fluvial, flood pain, and directly on the basalt (Figure flow basin facies). 14). We believe these lateral changes reflect an irregular Individual Towaco cycles depositional surface. resemble the Washington Valley mem- ber of the Feltville Formation in a larger scale, the Wash- lateral facies relationships ington Valley member ' thickens (Figure 16, again contrasting with towards the New Germantown Syn- the Lockatong [Figure 121). All cline, as does the whole of the divisions of the Towaco cycle ~eltville (Figure 14). This thick- coarsen towards the north, and the ening is in the same direction as microlaminated portion of division the mean paleocurrent vector for 2 thickens by more than an order the Formation which is southwest. of magnitude towards the Ramapo Presumably this indicates that the Fault. This microlaminated portion depositional center of the Felt- appears varved, similar to the ville, unlike that of the Locka- microlaminated portions of Lock- tong, was located near the present atong cycles and the Washington western edge of the Newark Basin. Valley member. Varve thickness increases in the same general In contrast to the Watchung direction as the entire micro- Syncline exposures, those of the laminated sequence (Figure 161, Oldwick Syncline contain little although only by a factor of five. massive siltstones. Instead, the The structures and fossils in siltstones are well bedded, often these varved beds are consistent sandy, sometimes conglomeritic, with the stratified lake model of and are usually made up of beds 1 deposition. However, the more mas- to 5 cm thick showing a distinct sive fine siltstone portions of graded pattern characteristic of division 2 are more consistent turbidi tes . with a model in which the lake experienced at least seasonal over- Towaco Formation Cycles turn; fossil fish are present in these beds but only as isolated The cycles of the Towaco bones and scales. Formation have a mean thickness of 30 m and can be broken into four At a number of exposures, basic divisions as follows (Figure division 2 of Towaco cycles con- 15 from the bottom up): 1, a 1 to tain beds which we interpret as 5 m gray siltstone and sandstone lacustrine turbidites of two (or conglomerate) often with root types. One series of turbidites, horizons, reptile footprints, and formerly exposed in the Roseland large to small scale crossbedding (Riker Hill) quarry, conform to (transgressive facies); 2, a 1 to the proximal-to-distal turbidite 5 m thick gray to black siltstone model developed originally for with a 0.1 to 5.0 m thick gray to marine flysche sequences by Allen black microlaminated calcareous (1969). The maximum thickness of portion often with numerous fish these Towaco turbidities increases (deep water facies; 3, a 3 to 6 m exponentially above the micro- laminated siltstones in division 2 Major Depositional Models for of the lower cycle, as might be Newark Basin Microlaminated Sedi- expected of such a channel ments approaching a site at a nearly constant rate (Allen, 1969). The Numerous authors have for slope of the approaching fan would decades interpreted organic-rich be the source of the slumped beds. mibrolaminated sediments as having In this model, water depth remains been deposited in a deep-water constant, but an alternative could anoxic environment such as the involve a decrease in water depth Black Sea or a stratified lake. resulting in the encroachment of (Bradley, 1929; David and Ludlam, the shore on the center of the 1973). Newark Supergroup organic- lake. The sense of rotation of the rich microlaminated sediments have folds in the slumped beds indi- been similarly interpreted cates transport from the east; (Cornet, Traverse, and McDonald, presumably this was the direction 1973; Hubert, Reed, and Carey, from which the channel fan ap- 1976; Olsen, et al., 1978; Olsen proached. A second series of turbi- 1980b). Recently, however, the dites is exposed in Towaco cycles proliferation of information on near the Ramapo Fault at Bernards- the sediments of arid environments ville and Wayne, New Jersey. These has led to a new model of deposi- are graded beds, 0.5 to 20 m tion. for many of these micro- thick, which occur throughout the laminated sediments; in this model otherwise microlaminated portions the microlaminated sediments form of division 2 and which resemble as living algal mats in very shal- the turbidites of the Washington low water. There is no doubt that Valley member in the New German- flat agal mat deposits closely town Syncline. Some of the thicker resemble microlaminated sediments turbidites are conglomeritic at formed in stratified lakes or their base and clearly scour the seas, especially in box cores or underlying microlaminated units. hand samples. Since many of the The pebbles found in these beds features explained by the algal are up to 3 cm in diameter and mat model are also explained by suggest a source from the west. the deep water mode, we can expect Thinner sandy turbidites often difficulty in deciding which model have casts of tool marks on their is applicable to any given depo- lower surface. These turbidites, sit. The ambiguity must be re- apart from their clastic composi- solved for Newark sediments or no tion, resemble units deposited by further analysis of the micro- turbidity currents in meromictic laminated units and the rest of Green Lake, Fayetteville, New York the sedimentary cycles will be (Ludlam, 1973). These turbidity possible. currents begin along the lake basin margin as slumps, which What specifically are the two slide down the basin slope, and models? In the algal mat model, liquify as they mix with water. microlaminated sediments are pro- duced by the continuous growth of The picture derived from a surface layer of living algae facies analysis is one compatible and bacteria in conjunction with with a model of a large perennial intermittent influxes of alloch- stratified lake which was wedge- thonous carbonate or clastic shaped in cross-section, deepest material (Buchheim and Surdam, near the Ramapo Fault, and receiv- 1977). The mats form only in very ing detritus primarily from the shallow water since the algae must east but with a significant west- have sufficient light to grow. The ern input at the western lake edge. laminated sediments thus formed are protected from wave action and Shilo, 1977). As a consequence of scour by the binding action of the this pattern, the algal-laminated algae and bacteria. In the strati- unit must be fundamentally dia- fied lake model, the laminations chronous and none of the indivi- are produced by seasonal changes dual laminae, or groups of laminae in the kind and amount of fine should be traceable across the material settling out of the water unit. column. The laminations are pro- tected by being below wave. base In the case of the stratified and in an oxygen-poor or toxic lake model, the microlaminated environment (i.e., an anaerobic units are deposited in the deepest hypolimnion) which excludes ben- parts of the water body. The model thic sediment-burrowing animals. is based on recent lakes and seas Both models successfully explain such as Fayettville Green Lake, the presence of organic-rich micro- New York (Ludlam, 19691, Lake laminated sediments themselves; Zurich (Nipkow, 19271, and the differences in corollaries of the Dead Sea (Neev and Emergy, 1969). models must be sought out or nei- The microlaminated unit expands ther model will be useful. Fea- and contracts with the depth of tures explained by both models and the lake. .In cross section the features unique to corollaries of microlaminated unit should form a each model are listed in Table 2. central deepest water facies sur- rounded in time and space by shal- The algal mat model is based lower water non-laminated sedi- on recent arid environments such ments. The unit as a whole should as bays and lagoons in Western be isochronous and individual Australia and the Red Sea (Logan, laminae should be traceable basin et al., 1974; Friedman, et al., wide and represent true time 1973) and lakes in the Sinai planes (Figure 17). (Cohen, et al., 1977; Krumbein, Cohen and Shilo, 19771, where a Algal mat deposits are un- diverse suite of algal mat types common today because they are exist including pinnacle blister, formed only where grazing by and flat mats. Only flat mats re- aquatic herbivores is reduced or semble the microlaminated sedi- absent (Golubic, 1973; Friedman, ments in question; but these et al., 1973; Logan, et al., 1974) occupy only a fraction of the usually due. to hypersalinity of total area in which mats grow. high temperatures. An indigenous Further, the algal mat zone itself fish population is essentially is restricted to a relatively nar- excluded, but fish may be washed row zone in shallow water (1-3m); onto the living mat from less hos- deeper and shallower water areas tile water. To be preserved whole, have no algal mats. As a lake or however, living algae would have bay deepens and shallows, a ring to cover these fish before they of algal mats presumably expands rotted on the super-oxygenated mat and contracts as the zone of appro- surface or before they floated priate water depth migrates later- away because of gas formation. ally. In cross section, the sedi- Such a process has never been ob- mentary record of such an advance served nor does it seem likely, and retreat shoiild be a deeper thus algal laminated sediments water non-mat unit surrounded in should not contain abundant whole time and space by ?he laminated fish. algal mat unit which in turn should be surrounded by a non- In the stratified lake model, laminated shallowest water unit however, the same features which ( Figure 17 ) ( Krumbei a, Cohen , and lead to the preservation of lamina- tions (i.e. deposition below wave Washington Valley Member) has been base and exclusion of burrowing traced from the southern Watchung organisms) lead to the preserva- Syncline to the Oldwich syncline tion of whole fish (Shafer, 1972). (Olsen, 1980b and 1980~).Through- Fish can be abundant in such water out these areas the lacustrine bodies since only the hypolimnion units contain a prominent micro- is anoxic. The increased pressure, laminated unit. The microlaminated lowered temperatures, and lack of beds in the Feltville, Towaco, and oxygen in deep water discourage Boonton Formations produce abun- gas formation and flotation of the dant whole fish, thus there is no dead fish (Shafer, 1972). The reason to prefer the algal mat organic-rich microlaminated sedi- model and good evidence to prefer ments produced according to the the deep water lake model for the stratified lake model should con- microlaminated units. tain abundant whole representa- tives of the indigenous fish popu- Demonstration that the micro- lations. laminated portions of the Lock- atong, Feltville, Towaco and Boon- In northern New Jersey (see ton Formations best fit the deep Stop 11, Olsen, (1980b) has traced water lake model does not imply a seses of microlaminated units that the associated non-micro- over 15 km. These units clearly laminated units were deoosited in form the deepest water portion of a deep lake. On the contrary, the Lockatong cycles and show every presence of reptile footprints, indication of being isochronous. abundant mudcracks, and occasional Data are still being collected and root zones in beds in the upper studied, but it is apparent that parts of some cycles attest to at least some individual laminae very shallow water deposition: can be traced the full extent of this should not, however, influ- the microlaminated unit. There is ence the interpretation of micro- no sign of associated pinnacle, or laminated units just a few meters blister mat-like structures. The below. Each characteristic deposit microlaminated units are sur- should be interpreted on its own rounded above, below, and to the merit and it should never be as- north by non-laminated units. Fi- sumed that any single depositional nally, the microlaminated units model should fit such a heteroge- contain abundant whole fish while neous formation. the surrounding non-laminated beds contain disarticulated fish. By The Eocene Green River Forma- these features, the algal mat tion of Wyoming, Colorado, and model may be discounted for these Utah is similar in many ways to portions of the Lockatong Forma- the Lockatong Formation of the tion. Newark Basin. Both deposits con- tain cycles of microlaminated, Because of the limited areas organic-rich beds and non-lami- of Jurassic strata which have nated evaporitic beds. In the escaped erosion (Figure 3) it will Green River Formation the micro- never be possible to trace the laminated units are in many cases lacustrine units of the Feltville, rich oil shales of great economic Towaco, or Boonton Formations importance. The current very ac- across the Newark Basin. Nonethe- tive debate on the environment of less, Towaco cycles have been deposition of the Green River Form- traced throughout the Watchung Syn- ation parallels and inspired the cline (Olsen, 1980~)~and the above discussion of Lockatong single thick lacustrine unit in microlaminated beds. the Feltville Formation (i.e. the There is presently no clear northern exposures north of the consensus on major depositional George Washington Bridge (Olsen, models for the Green River; some 1980b) a total of more than 20 km. workers (Surdam and Wolfbauer, Preliminary results from ongoing 1974; Eugster and Hardie, 1975; field work indicate that these Buchheim and Surdam, 1977; Buch- same cycles can probably be traced heim, 1978) adhere to a playa lake through the entire areal extent of model with a subsidiary algal mat the Lockatong. If so, the minimum origin for the microlaminated oil area of division22 of these cycles shale units, while others (Des- is near 7000 km . The lakes must borough, 1978) adhere to the strat- have been larger than the area of ified lake model. We see no rea- division 2 at their maximum extent sons why only one of these models and it seems likely some of the should be sufficient for such a largest lakes may have covered the complex assemblage of distinctive entire exposed extent of the units as the Green River. As we Newark Basin, some 7700 km2 see it, the playa lake model works (Olsen, 1980b). best for the microlaminated oil shale units. Non-microlaminated The areas occupied by the oil shale units need not fit in largest Jurassic lakes cannot be either model and may be best ex- approximated the same way as Lock- plained by a model based on Lake atong lakes because so little of Victoria as suggested by Bradley the original extent of the strata and Beard (1969) and Bradley, are preserved. However, the area 1970). over which the microlaminated por- tion of the Washington Valley Mem- Major Physical Features of the ber has been traced suggests a Lakes Which Produced the Micro- lake which 2must have been larger laminated Beds in New Basin Lacus- than 290km and the area over trine Cycles which Towaco cycles have been traced suggests lakes in excess of With the algal mat model of 990km . We believe that the lar- deposition excluded from the inter- gest Newark Basin Jurassic lakes pretation of the microlaminated may have been much larger in total beds of the Newark Basin lacus- area than the largest Lockatong trine cycles, we can proceed with Lakes. several more detailed questions: 1) How large in area were Newark Estimating the depth of any Basin lakes during their maximum ancient water body is speculative transgression; 2) How can the mini- and difficult. One trigonometric mum depth during maximum lake ex- method of calculating lake depth pansion be estimated; 3) What was is to use the distance to shore the cross-sectional shape of from the deepest part of the lakes Newark Basin Lakes; 4) What is the and an angle which describes the periodicity and cause of the lacus- average slope of the basin floor. trine cycles of the Newark Basin. If we assume that the deepest part of the Lockatong lakes was near The minimum area of Lockatong the geographic center of the lakes can be estimated by the area Newark Basin (see below), the of division 2 of Lockatong detri- shortest distance to shore during tal cycles. All of the individual maximum lake transgression would detrital cycles studied thus far be in excess of 20 km. If a con- in the Lockatong of Northern New stant slope toward shore is as- Jersey (see Stop 1) have been sumed the minimum lake depth would traced from the most southern ex- be 20 km X tan 0, where 0 is the posures at Hoboken to the most angle of the slope of the lake floor. This relationship is shown To use this equation to esti- in Figure 18. Unfortunately since mate the depths of Lockatong Lakes we have no real way of assessing we would need to know the greatest within several orders of magnitude wind speed which blew over Locka- (i.e. 0.001 to 1.5 seems reason- tong Lakes during the deposition able) our estimates of lake.depth of the microlaminated beds--a fact are similarly uncertain. A method we will never know. Nonetheless, which relies more on ' the character it seems reasonable to assume that of the sediments themselves would there were winds in the Triassic, be more useful. even strong winds; as the Triassic dune sands described by Hubert and Another, perhaps more reason- Mertz (1980) attest. The relation- able, way to estimate lake depth ship between depth of wave base can be derived from the familiar for fetches of 170 and 40 km and a relationship between lake fetch range of plausible wind speeds is and depth of wave base (as sug- given in Figure 20. It seems like- gested by Hubert et al., 1978). If ly that gale force winds (ca. we assume that the microlaminated 20mIsec) were occasionally fun- portions of division 2 of Lock- neled down the axis of Lockatong atong cycles were deposited below Lakes during the several thousand wave base, the minimum extent of years or more it took to deposit these units must approximate the each microlaminated bed, just as minimum area of the lake over powerful winds are funneled down which non-depth-limited waves the length of the African Rift Val- could be propagated by winds blow- ley Lakes today; Lake Tanganyika ing over the lake surface. The is often mixed to a depth of 100 major and minor axes of an elipse to 200 m by winds (Beadle, 1974). defined by the extent of the micro- These assumptions seem robust; if laminated units in the Lockatong so, Lockatong Lakes were probably Formation (Figure 19) can be used a minimum of 40 to 90 meters deep as minimum estimates of the great- during their high stands. No doubt est fetches for winds blowing even more powerful winds blew over along the axis of the Newark Basin the surface of Lockatong Lakes, or across the Newark Basin. In and we believe that these esti- this case these two fetches are mates are low minimums. 170 and 40 km. There is an empiri- cal relationship between wind Some information on the speed, fetch and wave length cross-sectional shape of Newark (Bretscheider, 1952; Smith and Basin lakes can be gained from Sinclair, 1972) given by the equa- variations in the thicknesses of tion (from Smith and Sinclair, lacustrine units over the basin. 1972, p. 389): If we assume that fine sediments reaching the Lockatong Lakes were preferentially distributed to the deepest parts of the lake, the Here g is acceleration by area in which Lockatong cycles are gravity (9.8 m/sec2), T is wave thickest represent the deepest period, w is wind speed in m/sec, part of the lakes and the deposi- and F is fetch in m. since for tional center of the Newark Basin deep water, wavelength ( X is during Lockatong deposition. The equal to 1.56 T amd wave base is thickest Lockatong cycles are approximated byX/2, the relation- found in the geographic center of ship can be restated interms of the Newark Basin in the Hunterdon depth of wave base as follows: Plateau Fault Block (see Stop 5, Sunday). In this area the mean thickness of Lockatong cycles is 4.2 m (Van Houten, 1964, 1969, areas along the Newark Basin's 1980) while around the edges of northwestern edge the micro- the basin the mean thickness of laminated units slice through cycles decreases to 2 to 1.5 m thick conglomerate beds and show (Olsen, 1980b). The area where no sign of ending within .5 km of Lockatong cycles are thickest also the Ramapo Fault (Olsen, 1980b). corresponds to the area where In these same areas the microl- chemical cycles are most abundant aminated beds themselves contain (Van Houten, 1964). In fact, out- thin graded conglomerate beds side of this central area, most which we interpret as lacustrine chemical cycles are replaced by turbidites. These features suggest red beds identical to typical red that Towaco and Feltville lakes beds of the Passaic Formation. The were markedly asymmetrical with cross-sectional shape of Lockatong their deepest portions near the lakes during their maximum extent, northwestern margin of the basin. can thus be inferred to have been During maximum transgression these a gentle dish, perhaps best approx- lakes may well have lapped well up imated by a very flat trapezoid. the scarps at the basin's edge. Of course this assumes that Lock- atong lakes ended somewhere near Van Houten (1962, 1964, 1969, the current limits of the Newark 1980) has estimated the duration Basin. If lake level rose so that of Lockatong cycles by assuming lake waters lapped against the that the microlaminated units of bordering highlands, the cross- division 2 are varved, and extra- sectional shape of the lakes could polating the rates of sedimenta- have approached a steep sided tion derived from varve thickness trapezoid or a rectangle. The ap- counts to the entire cycles. His parent termination of microlami- counts, based on the cycles in the nated siltstones of Lockatong center of the Newark Basin, sug- cycles within the basin (notably gest a periodicity of about 20,000 at the northeastern and southwest- years. As noted by Van Houten this ern ends) and the replacement of suggests control of the depth of these microlaminated units later- Lockatong lakes by precipitation ally by non-laminated siltstones in turn governed by the precession and finally by gray and buff ar- of the equinoxes. New data on kose and sandstone, suggests that varve counts (Olsen, 1980b) sup- the shores of Lockatong Lakes may port Van Houten's data for the cen- indeed have approximated the pre- tral Newark Basin. Where the cy- sently preserved edges of the cles thin to a mean of 1.5 meters, Newark Basin. The shallower cross as at Weehawken, much shorter dura- section, therefore, seems more tions for each cycles are indi- likely. cated, on the order of 5,000 to 10,000 years. This presumably indi- Towaco cycles and the Washing- cates significant bypassing or ero- ton Valley Member of the Feltville sion in the marginal areas (Olsen, Formation show a pattern of thick- 1980b) . nesses completely different from the Lockatong, and from this we Cycles nearly identical to infer a different cross-sectional Lockatong detrital cycles occur in shape for these ancient lakes. In the contemporaneous upper member both the Towaco and the Feltville of the Cow Branch Formation of the Formations, microlaminated units Dan River Group. Floral remains are an order of magnitude thicker from these cycles suggest changes along the northwestern edge of the in climate during the expansion Newark Basin than along their and contraction of the lakes which easternmost outcrops. In some produced the cycles (Olsen, et al., 1978). Floral remains are increased precipitation, although much less common in Lockatong the closure of the basin drainage cycles but studies of spores and system and the cross-sectional pollen are now underway by one of shape of the lakes were certainly us (Olsen). controlled by basin tectonics which in turn was under the same As Van Houten (1962, 1964, control as the volcanism. 1969, 1980) has described, Lock- atong cycles are arranged into The duration of Towaco cycles higher order cycles in the Newark cannot be estimated the same way Basin. Clusters of detrital cycles as the duration of Lockatong and of chemical cycles occur at cycles since the upper parts of about 25 m intervals. Very thick Towaco cycles are very much clusters of chemical cycles occur coarser and individual units show at 100 m intervals and this corre- extensive downcutting making extra- sponds to the thickness period- polation of varve counts to the icity of the alternations of red whole cycle unreasonable. If, how- and gray units higher in the Pas- ever, Towaco cycles were of the saic Formation. It is interesting same duration as Lockatong cycles, that each set of a cluster of deposition of the Towaco Formation detrital cycles plus the succeed- proceeded at roughly 6.7 times ing cluster of chemical cycles con- that of the Lockatong, that is at tains from five to six cycles; at an average rate of 1.5 mm/yr. 20,000 years per cycle this gives an average of 100,000 to 120,000 Notes on Ecological Dynamics in years for each 25 m larger cycle. Newark Basin Lakes Of course 100.000 years is the principle of the Obvious changes in total glacial-interglacial cycles of the organic carbon content follow the Pleistocene (Hays, Imbrie, and microscopic textural and bedding Shackleton, 1976), and finding an features and fossil content in obvious periodicity of similar Newark Basin lacustrine sequences. magnitude in the Lockatong Forma- These are easily seen in the color tion is very suggestive. The larg- of non-metamorphosed rocks; the est cycles of about 100 m have a few analyses done so far indicate calculated periodicity of about the following rough association of 44, 000 years Van Houten (1964). color and carbon content--red Cycles of this periodicity are the (0%), gray (0.5%), black (.508%). most obvious in the Passaic Forma- Thus sedimentary cycles such as tion and they comprise the gray those in the Lockatong show cor- and red units mapped by McLaughlin related cycles in total organic (1946) throughout the Hunterdone carbon. Many authors have con- Plateau Fault Block. sidered the amount of organic car- bon in sediments to be a good re- Ponding by lava flows has flection of the productivity of been suggested to account for the the lake ecosystem (Hutchinson and lacustrine units of the Jurassic Wollack; 1940; Deevey, 1942; Linde- strata of the Newark Supergroup man, 1942). A consideration of the (Krynine, 1947). It is not neces- large scale energy dynamics of sary to invoke this mechanism for lakes shows total organic carbon the Newark Basin since strata far content of sediments can be decep- below the extrusive units contain tive as an indicator ' of primary extensive lake deposits. Lacus- production but it also reveals trine units of the Feltville, some fundamental relationships Towaco, and Boonton Formations between a lake's ecological his- most likely developed because of tory, the production of organic sediments, and ultimate hydro- ference between the rate of produc- carbon production. The cycles in tion of reduced carbon by the eco- organic carbon seen in Newark system and the rate of loss by Basin lacustrine sequences can respiration is equal to the net probably be better understood in ecosystem productivity (NEP) and terms of changing energy dynamics it is this last quantity of carbon than simply as a record of chang- which can be preserved in the sedi- ing primary productivity. ments. The source of virtually all In a perfectly efficient eco- usable energy in ecosystems is system all of the energy captured primary production by plants. In by photosynthesis would be dissi- large lakes the bulk of usable pated by the rest of the organisms energy comes from photosynthesis of the ecosystem as CO and heat within the lake. Photosynthetic (Rsp = GP and Rs x 100 = 100%); plants fix carbon, and this re- there will be no^'waste." If this duced carbon is the source of perfect system were a lake there energy for all other organisms in would be no accumulation of or- the lake (chemosynthetic bacteria ganic material in the sediments are here considered to be ulti- (i.e. GP = NEP = 0). Of mately dependent on compounds re- course real Rs~ ecosystems must be sulting from photosynthesis--Cole, less efficient than this. This con- 1979). Consumer and decomposer cept of ecosystem efficiency organisms oxidize the reduced car- emphasizes that two equally impor- bon and thus obtain energy. tant factors (GP and RsE) contri- bute to the sedimentary record of Obviously, organic carbon in an ecosystem such as a lake, and sediments has its origin in pri- that the ratio of these two terms mary production. In lakes, the need not be constant. organic carbon locked in sediments represents a net loss of energy A demonstration of the cru- from the lacustrine ecosystem. cial role of ecosystem efficiency This relationship is what suggests is given by a comparison of a reading carbon content as a record tropical forest and a north temper- of productivity. But the loss to ate bog. The well-drained soils of the sediments depends on what pro- tropical forests are often very portion of the energy of primary poor in organic material; the sedi- production is dissipated by the mentary record of such a forest living ecosystem. soil might plausibly be a series of red beds riddled with root- The ratio of dissipation (by casts, much like portions of the respiration) of reduced carbon by Passaic Formation. The bog on the all the organisms of an ecosystem other hand, has a waterlogged soil (RsE) to the gross productivity of composed almost entirely of the reduced carbon of the ecosystem remains of dead plants. The sedi- (GP) (times 100) we can loosely mentary record of this soil might term the ecosystem efficiency: be a peat or coal. If sediment carbon content were "read" as a (Rs-E /GP) 100 = ecosystem efficiency literal record of productivity, - the peat or coal would be inter- This concept is suggested by preted as the product of an eco- Lindeman's (1942) development of system much more productive than the concept of ecological effi- that which produced the red- beds. ciency carried to the ecosystem This interpretation would be level and Wetzel's (1975) emphasis wrong; tropical forests are among on the role of detritus. The dif- the most productive ecosystems on earth while north temperate bogs bic decomposition then becomes are among the least. The important dominant at the lake bottom. difference lies in the high rate Anaerobic decomposition occurs at at which the well-drained tropical a slower rate than aerobic (Wet- soil recycles plant debris, and zel, 1975; Cole, 1979) and energy other dead organisms. The bog, on rich organic material accumulates the other hand, recycles at 'a low at an even faster rate. The pro- rate, tending instead to preserve cess of eutrophication thus lowers organic material. In this case the ecosystem efficiency (Lindeman, ecosystem efficiency of the tropi- 1942). cal forest is many times that of the bog. Physical Factors Similarly there is no reason Studies of two lakes in Michi- to postulate unusually high levels gan by Newcombe and Slater (1950) of primary production in the and Cole (1954) point up the role Carboniferous to account for the of physical factors, in this case abundant coal. Production levels water depth, in otherwise similar could have been lower than modern lakes (Cole, 1979). In the deeper environments if ecosystem effi- lake a permanently anoxic hypo- ciency was lower. The decrease in limnion is present and thus a frequency of coals above the Car- larger proportion of organic mater- boniferous might well be due to ial undergoes anaerobic decomposi- the evolution of soil organisms tion with presumably a corres- which increased the rate at which pondingly lowered ecosystem effi- organic matter was dissipated. ciency. There are three interrelated The Kind of Organisms Present controls on lacustrine ecosystem efficiency: 1) actual gross pri- Today, tubificid worms and mary productivity; 2) extrinsic chironomid fly larvae act to tran- physical factors such as basin sport material across an oxygen morphology, water depth, salinity, gradient at the sediment-water and wind conditions; and 3) the. interface (David, 1974) in highly diversity, abundance, and nature productive lakes with low oxygen of consumers and decomposers. As concentrations at the bottom. By detailed below all three of these irrigating sediments with water factors play roles in determining which is relatively more oxy- both differences between lakes and genated they increase the rate at changes in lakes through time. which organic material is meta- bolized. Essentially, they mine Cultural eutrophication of the sediment under conditions lakes is a process in which nutri- where nothing else can, and in the ents added by man, usually in the process they increase the eco- form of sewage, industrial waste, system efficiency. There are very or agricultural runoff, increase few reasons, however, for thinking lacustrine primary productivity that these groups were present in often with undesirable conse- the Triassic. If these organisms quences (Hutchinson, 1969). Pri- were absent from those ancient mary production usually increases lakes, with no replacements, a to a point where it exceeds the given level of primary production rate at which it can be balanced could be associated with a lower by aerobic consumption and decom- ecosystem efficiency and hence a position. A surplus of organic larger proportion of gross produc- material builds up which can ex- tion would end up in the sedi- haust the oxygen at depth; anaero- ments. The degree of bioturbation of lake sediments is thus an in- bon, both as particulate and dis- direct measure of lacustrine solved matter but not including efficiency; organic rich microlami- that part lost into the sediments; nated sediments showing no signs and 3) migration of reduced carbon of bioturbation indicate low eco- compounds into and out of the sedi- system efficiency while biotur- ments after deposition. The first buted sediments indicate higher of these, abiotic oxidation, seems efficiency. to be inconsequential in most lake' systems compared to the magnitude In the stratified lake model of loss by biological processes of the production of microlami- (Wetzel, 1975). Allochthonous im- nated sediments, bioturbating ports and direct outflow can be organisms are excluded by the very important in small or very perennial presence of an anoxic shallow lakes (Wetzel, 1975) but hypolimnion ( Bradley, 1929; these factors are presumably of Twenhofel, 1932; David and Ludlam, less importance in large lakes. 1973; Cornet, Traverse, and Mc- Carbon compound migration is of Donald, 1973; Olsen, Cornet, great importance to geologists and Remington, and Thornson, 1977; palaeoecologists for it distorts Olsen, 1980b and Wilson, 1980). our ability to read the record of If, however, such organisms as carbon losses to the sediment. It tubificids and chrinomids were is also the process of hydrocarbon absent in the distant past, many migration. The search for the ori- lakes with low ecosystem effi- gin of hydrocarbon source rocks ciency but without a perennial must therefore concentrate not hypolimnion, could produce micro- only on environments of originally laminated sediments (Olsen, 1980b). high primary production, but also environments of low ecosystem Shallow lakes can be just as efficiency. productive as deep lakes if not more so (Cole, 1979; Beadle, 1974; Newark Supergroup deposits, and Wetzel, 19751, and there are in general tend to have thicker no reasons for supposing that the accumulations of organic rich shallower lakes which deposited sediments in the more southern division 3 of Lockatong cycles, or basins (Olsen, McCune, and Thom- the terrestrial and fluvial son, In Press; Hubert and Mertz, systems which deposited division 4 1980; Cornet, 1977). Several of Towaco cycles were any less Basins south of the Fundy Group productive than the lakes which contain very thick (500-2000 m) deposited division 2 of the same sequences of organic-rich sedi- cycles. The change in carbon con- ments that can plausibly be re- tent through these sedimentary garded as hydrocarbon source cycles probably reflects changing rocks. These deposits represent ecosystem efficiency .through time the accumulated net loss of energy as the lake changed in depth (see from periodically cycling lacus- Figure 32). trine ecosystems. Many of the se- quences show resemblances both in There are three factors of fossil content and facies patterns possible importance not considered to the Eocene Green River Forma- in the above discussion: 1) loss tion. A major difference, however, of reduced carbon by abiotic oxi- is that most, if not all, Newark dation in the water column, in the Supergroup sequences have been sediments during deposition, and buried to a depth of from 1000 to as part of later diagenesis; 2) 6000 m and thus hydrocarbon migra- addition of allochthonous carbon tion has already occurred (Hunt, and direct outflow of reduced car- 1979). Indeed, few Newark Super- group deposits contain beds that could be considered oil shales; most of the organic-rich sediments are too mature. But, are there reservoir facies and suitable traps? Certainly the prevailing monoclinal nature of most Newark Supergroup strata is not encourag- ing. However, Newark facies rela- tionships and structure are com- plex, and Newark Supergroup strata should not be overlooked in the search for hydrocarbons. Finally, we know virtually nothing about the offshore Newark Supergroup equivalents. If they are similar to the onshore souther basins they may contain large volumes of suitable source rocks perhaps in favorable migration and accumulation settings. However, as long as they are thought of as "barren Triassic red bed se- quences" we will never know. ROAD LOG (Saturday) tic. During the time the lake existed more than 200 feet of varved clays were Mileage deposited. Over 2,500 varves have been counted from this horizon. About 3,000 to Rutgers University, Newark, New Jer- 5,000 years ago, rising sea level accom- sey. panying the melting of the ice sheets exposed the river to the tides. Estuarine Left turn onto Warren Street, leav- conditions extend north into the Hacken- ing University parking lot. sack River Valley, producing the salt marsh environment that has existed into Left turn onto Washington Street. the present.

Turn left onto Broad Street. The Meadowlands is one of the most in- tensely used land areas in the world. As Right turn onto ramp leading to we travel across the region for the next N.J. 58E and interstate 280E. 11 miles, we will observe the diverse utilization of the land in the form of Bear left, taking N. J. Turnpike high-rise condominiums, town houses, North towards G.W. Bridge. sanitary landfills, industrial and recrea- tional parks, the Sports Complex, mari- Snake Hill, a Triassic volcanic nas, Liquid Natural Gas Storage Faci- neck, appears to the east. lities, Sewage Treatment Plant, generat- ing plant, and so forth (see Agron, 1980). The low-lying cliff to the west is the site of the historic Schuyler Sanitary landfill to the west. Copper Mine, where copper was ini- tially discovered in 1712 or 1713, Harmon Cove Development, Hartz Moun- and mined in 1739. The cupriferous tain Industries with high-rise minerals at the mine are chalco- apartments, town houses, marinas, cite, chrysocolla, minor amounts of etc. malachite and azurite, and rare particles of cuprite and native cop- New.Jersey Complex with race track, per. Chalcocite is the only poten- Giant's Stadium, etc. tial ore mineral. The origin of the ore is explained by hydrothermal Two LNG storage tanks to the north- solutions that accompanied the in- east. trusion of small diabase dikes (probably ~urassic) found below the View of the backslope of the Pali- ore body. While the mine has had a sade Sill to the east. long history, it has produced lit- tle since the Revolutionary War Granton Quarry, exposes the lower (see H.P. Woodward, 1944, for an Lockatong Formation and the over- enlightening account of copper min- lying sill (see Van Houten, 1969; ing in New Jersey). Olsen, 1980).

Hackensack Meadowlands. Agron Bergen Generating Station, P.S.E.& (1980) reports that this region was G. Co. to the west; Bergen County covered by at least three glacial Sewage Treatment Plant to the east. advances in the Pleistocene. About 15,000 years ago, the entire region Crossing the Hackensack River. was submerged by proglacial Lake Hackensack, which was impounded be- Climbing the backslope of the Pali- hind the terminal moraine to the sades Sill. south. About 10,000 years ago the terminal moraine was breached, and Palisades Sill in contact with the the lake was drained into the Atlan- Lockatong hornfels in roadcut. 17.7 Bear right, exiting at "last exit Palisade Sill. in New Jersey"; continue east on Bridge Plaza Square Road. Park in lot then walk up stone steps up the hill (west) to the 18.2 Right turn at "T" intersection onto road at the level of the circle Hudson Terrace. (River road in Park) and walk north along road to exposures of the 18.4 Stop sign; continue traveling south Lockatong (Figure 22). on River Road. Proceed north along road walking 18.5 Left turn into the entrance of the slowly down section. All ten of the Palisades Interstate Park. Follow detrital cycles exposed here (Fi- park road around to north. A signi- gures 22 and 23) have been traced ficant portion of a large phytosaur more than 15 km to the south (01- skeleton was found in upper Stock- sen, 1980b). These cycles are infor- ton beds near here in 1911. The mally designated 0, l', 1, 2, 3, 4, skeleton, named Rutiodon manhat- 5, 6, and a, by c. Cycles l', 1, 2., tanensis by Friedrich von Huene is 5 and 6 contain beds which are not really generically determinate prominantly microlaminated. Cycles because it lacks a skull. It is now a, b, and c are not microlaminated on display at the American Museum here but become so in the exposures of Natural History in New York. further south (Olsen, 1980b). Cy- cles 2, 5 and 6 contain numerous Reentrant in Palisade escarpment at fossil fish (see Figures), and cy- this point is due to a few east cle has produced scattered remains dipping normal faults. of the little lizard-like reptile Tanytrachelos (Figure 24). At Kings 18.6 Olivine zone of palisade Sill on Bluff, 15 km south a team of Yale left. Diabase on left has a dis- paleontologists opened a quarry in tinct finely laminated appearance. cycles 5 and 6 and recovered over 4,000 fish and reptile skeletons in 19.0 Irregular contact of Palisade Sill the years 1978-81. At these more with Lockatong Formation on left southern outcrops the fossil fish (Figure 21). are more abundant and tend to be better articulated than to the 19.1 Pass under George Washington Bridge. north. The gradual facies changes from Kings Bluff to the George Wash- 19.2 Additional exposures of the contact ington Bridge in cycles 5 and 6 are between the Lockatotig Formation and show in Figure (25). Note decreas- the Palisades Sill. Here the con- ing frequency in the presence of tact is conformable. On the right, articulated reptiles and fish. The at the base of the hill, is a foot- detailed differences in lithology path along which there are good and faunal content allow for rela- exposures of buff arkose and red tively easy cycle-by-cycle correla- and purple siltstones of the upper tion. Stockton Formation. At these exposures, cycles 3 and 4 Circle in park road at base of have been replaced by buff, cross- shear face of Palisades Sill. Take bedded arkose and the upper parts road which veers off on right of cycles 5 and 6 have developed towards Ross Dock. calcareous and nodular beds resembl- ing caliche. Athick bed of arkose STOP 1. Ross Dock, palisade Inter- cuts down into cycle a, nearly cut- state Park. Extensive exposures of ting it out. The mean paleocurrent detrital cycles of Lockatong Forma- direction for these arkose beds is tion and irregular lower contact of N 59W (based on 8 readings). Cycle a is penetrated by numerous 24.2 Open cut in Palisades Sill and Lock- burrows called Scoyenia. Scoyenia atong hornfels. According to Van type- - burrows are extremely abundant Houten (1969), hornfels include in Triassic Newark Basin strata and grossularite-andradite, prehnite, seem to be the work of a small and diopside varieties. The Lock- arthropod, perhaps a crayfish atong cycles are fossiliferous, as (Olsen, 1977). These Scoyenia bur- usual, and may tie in with Granton rows are not present in this same' Quarry cycles. . cycle to the south. We are clearly in the shallow water facies of cy- 24.8 Veer right onto exit for Route 80. cles a-c at this point but only just leaving the deep water facies 25.3 Beginning of type section of Pas- of division 2 in cycles 2, 5, and saic Formation. 6. Cycle a shows a well developed facture cleavage in division 1. 33.0 Garrett Mountain visible on left Cleavage dips 25' to 30' W and (south), Passaic Falls is on the strikes S 78 W. The cleavage is right (north). The upper Passaic strata-bound but discontinuous, Formation of Rhaetic age (latest passing laterally into breccia or Triassic) has produced near here a non-cleaved beds. What is the signi- series of well preserved skeletons ficance of these structures? of the highly specialized procolo- phonid reptile Hypsognathus (Col- The facies trend in the Lockatong bert, 1946). About one skeleton or from Kings Bluff to this stop is skull is found per decade. from a more central basin facies to a more marginal fades. The mono- 33.7 Contact of Passaic Formation with tony in horizontal continuity in overlying Orange Mountain Basalt on detrital cycles gives way laterally left (south). Columnar basalts of to heterogeneity (Figure 25). Those the lower flow unit are well ex- cycles with the best developed posed in the roadcut. A series of microlaminated units and the best faults cut the Orange Mountain preserved fish' in division 2 are Basalt here, some of which are those which persist the longest visible in the cut on the left, with the least change to the north. just west of the Passaic-Orange Mountain Basalt contact. Triassic- Note that the horizontal distribu- Jurassic boundary is somewhere with- tion and faunal content of the in a few meters below contact. microlaminated portions of division 2 of cycles 2, 5, and 6 are incom- 34.0 Beginning of the upper flow unit patible with an algal mat origin. with its characteristic ropy pahohoe-pillowed surface. 20.9 Return to park entrance. Leave park and turn right. 34.2 Transverse cross-section of sub- aqueous flow lobes. Note the 21.0 Turn left onto Main Street (Bergen arcurate pattern of the pillow lava County Route ll), proceed west. complex. These structures will be examined in the lower and upper New 21.5 Turn right onto Lemoine Avenue, Street Quarries at Stop 2. continue north crossing over west portal George Washington Bridge. 34.5 Exit at Squirrel Woods Road, bear- ing left at exit. 21.8 Turn left (west) onto Cross Street. Keep left. 34.6 Bear left at road signs onto Route 80 overpass. (Do not enter Route 23.2 Veer left onto entrance ramp for 80). Route 95-80. Proceed on Route 95 S. 34.8 Left turn into New Jersey Bank park- eroded pillows along the contact ing lot. Drive east through the indicates that they are confor- lot, exiting on New Street. mable. Note the manner in which the younger pi 1 lows cascade off the 35.5 Left turn onto New Street. Park in flow lobe, building up slopes of the Richardson parking lot. about 40. In general, the pillow buds are very dense with radial STOP 2. Orange Mountain Basalt: joint structures and few minute Upper Flow Unit, New Street Quarry. vesicles, indicating that they formed in deep water. The absence Our objective at this stop is to of pillow-derived debris within the examine subaqueous volcanic struc- interstices of pillow complexes tures including: pillow lavas, flow indicates that the debris was lobes, fissure eruptions, a vol- washed out of these pockets in a canic cone (?), and zeolite mineral- well-agitated lake. The occurrence ization. Caution should be exer- of interstitial angular basaltic cised in the quarry and partici- fragments (surrounded with quartz, pants should not climb the upper calcite, prehnite and other zeo- quarry walls. lites) indicates that the fragments were derived from the checkered The walls of this quarry and an exterior rinds of the pillows by adjacent quarry, long favorites of circulating fluids, perhaps ground mineral collectors for their beauti- water. The original debris was ful and diversified suite of zeo- probably redeposited in a deeper lites, also exhibit a splendid ar- part of the basin, along the border ray of subaqueous volcanic struc- fault. The flow lobe appears to tures (see Figure 8). Participants flare out and to plunge westward, should first examine the structures where it may be studied in the of the east (or far) wall, noting walls of the lower New Street Quar- the amygdaloidal and vesicular up- ry. At some appropriate time we per contact of the lower flow unit shall enter that quarry as a group. and the overlying Tomkeieff se- Figure 9, a field sketch of its quence, which is overlain by bedded east wall, shows three distinct pillow lavas and a second Tomkeieff episodes of vulcanism: sequence. Note also spiracles in (1) an older episode of flow lobe: the lower colonnade and cross- (2) a medial phase of massively sections of polygonal-joint sets of bedded, moderately coarse-grained the entablature. Follow the struc- igneous rock that slopes away from tures along the south wall, walking a central point and overlaps the west, and note the increase in pil- distal and advancing end of a flow low lavas with a concomitant de- lobe; and (3) a younger zone of crease in massive basalt. On the bedded pillow buds that overlie west wall we may observe the charac- both the steep slope of the suba- teristic concave-downward arcuate queous volcano (?) and the flow form of overlapping flow lobes in lobe. The origin of these features transverse section. Pinching and should encourage a lively discus- swelling pillow buds elongated N-S sion. in arcuate bundles distinguish the flow lobes from the overlying bed- . 35.5 Turn right leaving the parking lot. ded pillows which appear to be stacked one on the other and elon- 35.6 Turn right into New Jersey Bank gated E-W. parking lot. Drive west through the lot exiting onto Squirrel Wood Road. Although the contact between the two types of pillows appears to be 36.1 Turn right out of Bank lot on comformable, the absence of the Squirrel Wood Road. Turn right into Route 80 E; note mineralization (chrysocolla and the pillow lavas in the roadcut. malachite.) Petrographic and paleo- ccurent studies along this highway, Exit onto Route 20 South towards and elsewhere in this stratigraphic the Garden State Parkway horizon, indicate that the sediment was derived from a deeply weathered Bear left, entering the Garden metamorphic terrane to the north State Parkway. and east, and transported to the basin across a broad southwest- Exit the Garden State Parkway at sloping pediment. exit 145, taking Interstate 280 East towards Newark. 51.5 Continue on I 280 westbound

Exit in Newark, making a left turn 54.2 Dike intrusion and offset into at llT1lintersection. fluvial channel sandstones of the upper Passaic Formation. Left turn at light. 54.5 Cuts in uppermost Passaic Formation Enter Interstate 280 West. here have produced phytosaur foot- prints called Apatopus and the pos- Alternating beds of red sandstone sible crocodilio-morph tracks and mudstone with a few thin inter- called Bactrachopus. The Triassic- beds of gray siltstone and dark Jurassic boundary lies somewhere gray to black micaceous shale, within the upper few tens of meters occurring below the first overpass. of the Passaic Formation here. These siltstones yield a probable Upper Norian palynoflora and occur 55.0 STOP 4. Orange Mountain Basalt; about 1100 m below the First Watch- lower flow unit. Our objective here ung Mountain Basalt (Cornet and is to examine a Tomkeieff sequence Traverse, 1975, p. 27). Sporadic of colonnades and entablatures near exposures of sandstones and mud- the classical site of OIRourkels s tones with fining-upward se- Quarry. quences, characteristic of meander- ing streams, occur along Interstate When built in 1969, this road cut 280 for the next 4.4 miles. was the deepest federally-financed highway cut east of the Mississippi Bear right for the Garden State River. About 33 m deep, the cut Parkway. exposes a complete section of the lower flow unit of the Orange Park in service lane approaching Mountain Basalt, and a broad array East Orange, Exit, and walk west to of joint patterns that formed as outcrop in exit ramp. the basalt cooled. The large "basin" structure on the southeast STOP 3. Passaic Formation: Central wall was first described about 100 Basin"'Facies years ago by J.P. Iddings (1886) of the U.S. Geological Survey in John Figure 26, a stratigraphic section OIRourkels Quarry, about 300 m of this stop, shows characteristics south of the roadcut. While such of the f ining-upward sequence, complete structures have not been namely: cut-and-fill channels, chan- observed elsewhere in the Watch- nel lag concentrates, cross-bedded ungs, similar joint structures, arkosic sandstones, overbank depo- e.g. chevrons, oblique and reverse sits of reddish-brown mudstone with fans and rosettes (terminology of calcrete paleosols, gray-green to Spry, 1962) may be studied in this green shales with plant fragments, roadcut and in almost every quarry Scoyenia, roots, (?) and copper along strike for a distance of 80 to 100 km. Sanunis (1978), and Justus and others (1978) at this site show This structure (about 33 m thick) that the striations are records of conformably overlies a fluvial red discrete thermal events, charac- bed sequence of shales and sand- terized by sudden periods of crack stones and, when first exposed, advance in the cooling basalt. displayed a complete Tomkeieff se- Features such as chisel marks, quence of: (1) a lower colonnade pinch and swell and kink structures (10-15); (2) entablatures (20-30m); on the curvi-columnar joints may and (3) an upper colonnade (1-2 m) also represent an episodal cooling (Fig. 17). While the lower colon- history. Each of these features may nade is composed of massive 4-5 or be observed on the walls of the 6-sided polygonal and subvertical highway cut. prisms, the entablature is composed of long (25-30 m) slender narrow The striations reported by Iddings joint prisms that radiate from an (1886) show up on joint surfaces of apparent focus. Several juxtaposed the lower colonnade as cyclical bundles or sheafs of radiating bands of smooth and rough zones, prisms may be observed in the road- about every 5-7 cm. Ryand and Sam- cut, comprising fan and chevron- mis (1978) report that as the crack like features. Cross joints, inter- growth proceeds, the first formed secting radiating prisms at high zone is smooth and associated with angles, are prominent and appear to a thermal shock event; the second be concentrically arranged about zone is rough, has positive relief, the apex of radiation. An incom- and is associated with the halting plete section of pseudo-columns of each crack advance. Joints of overlie the entablature. the entablature are also cut by concave-upward "dish-like" joints Petrographic studies (Figure 11) that are cut by strike-slip faults. show an increase in grain size, an While the origin of this structure increase in the abundance and size is debatable it trends N 50' E and of the interstitial glass, and an evidently formed after the basalt increase in the olivine content in cooled and before faulting occurred. the entablature. This suggests that although cooling may have proceeded 55.7 Backslope of the first Wachung lava very slowly from the sediment- flow; outlines of pahoehoe toes may volcanic interface, once a ground- be studied in roadcut. mass capable of transmitting stress was established the remaining melt 56.7 Contact of the Second Watchung lava cooled almost instantly. The ob- flow with the underlying Feltville scure joint pattern in the upper Formation. Note the fine-textured colonnade may form from convective joints of the entablature, and the heat loss near the upper part of large number of strike-slip (left- the flow. The early cooling history lateral) faults with little or no of the magma is manifested by well- dip-slip offset. When exposed, dur- developed horizontal striations ing road construct ion, the forma- observed on the joint surfaces of tion consisted of cross-bedded the lower colonnade. While Iddings feldspathic sandstone (10m) under- (1886) may have been the first to lain by thin stringers of coal with report horizontal striations on underclay. A similar section may be joint surfaces (from 0'Rourke' s studied in the parking lot of the quarry), James (1920) speculated Daughters of Israel Nursing Home, that these striations represent suc- 1155 Pleasant Valley Way, West cessive stages or pulses in which Orange (about 314 mile south). the rock broke and the columns formed. Recent studies by Ryan and 57.4 Backslope of the Second Watchung lava flow. Coarse-grained diabasic entering park. texture may be examined near upper part of the exposure. As it stood in 1975, the Roseland Quarry occupied 55 acres, exposed 59.0 Looking west across the Passaic 95 m of upper Towaco Formation-- River Valley you can observe the including two complete Towaco cy- low hills of the Third watchung cles, and exposed about 50 m of the lavas, the New Jersey Highlands on overlying Hook Mountain Basalt the horizon, and the lake bed of (Figure 27). The quarry became very Glacial Lake Passaic. The lake well known in the late 1960's and formed when the meltwaters of. the early 1970's for its prolific dino- Wisconsin Glacier became empounded saur footprints. Because of the between the N.J. Highlands on the scientific and educational poten- west, the Second Watchungs to the tial of the site the then owners, east and south, and the moraine to Walter Kidde and Co., Inc. donated the south. At its maximum extent, the most productive 15 acres to the the lake was 30 miles long, 10 Essex County Park Commission. The miles wide and 240 feet deep (Kum- site now awaits development. mel, 1940). Before the other 40 acres were 60.0 Exit I 280 at Eisenhower Parkway developed as the Nob Hill develop- South. Continue south on the ment, the following features could Parkway. be seen:

61.1 Excellent exposures on left (east) 1, lateral changes in facies within of contact between Towaco Formation division 1-3 of the lower cycle and Hook Mountain Basalt in Nob (Figure 28). The microlaminated Hill Apartment Complex (former east beds of division 2 produced many half of Roseland Riker Hill Quar- fossil fish, all ~emiinotus,as did ry). Two flows of Hook Mountain a number of the thinner (30 cm) Basalt visible here .(cumulative turbidites. thickness 110 m). 2, two upwards coarsening turbidite 61.4 Turn left onto Beaufort Avenue. sequences, the lower being by far Take Beaufort Avenue south follow- the larger. The lower sequence ing along the back slope of Riker shows large scale slumped beds Hill. resembling "wild flysche" associa- tions. Some of the "roll overqq 61.8 Turn left into entrance road for structures are 2 to 3 m in dia- Riker Hill Park of Essex County meter. Transport was from the east. Department of Parks, Recreation, and Cultural Affairs (former Essex 3, abundant dinosaur footprints in County Park Commission). Follow possible crevasse splay (in divi- road up dip slope of Hook Mountain sion 3) of channels about 70 m to Basalt. Follow signs to Geology north of tracks. Orientation of Museum. trackways proved to be parallel to paleocurrent directions derived 62.2 STOP 5. Geology Museum and Walter from ripple marks within the foot- Kidde Dinosaur Park (former west print-bearing bed and oriented side Roseland Riker Hill Quarry). plant debris in overlying beds. Park in lot and look over exhibits at Geology Museum. Then take access 4, Series of 7 fining-upwards cy- path from Geology Museum over the cles of division 4 of the lower crest of Riker Hill and down, Towaco cycle in the Quarry. Middle through wooded area into Dinosaur 3 cycles had extensively developed Park. Always get permission before dolomitic nodules and deeply mud- cracked beds. Second fining-upwards similar to those seen in the Lock- cycle from the bottom with lami- atong at Stops 1-4. Microlaminated nated silty beds (? flood basin) beds locally involved in dishar- with abundant clay filled root monic folds. Like the beds of divi- casts, many of which are surrounded sion 1, these portions of division by dolomitic nodules. 2 look exactly the same in the . Chatham exposures. In the presently exposed beds the following can be seen: 4, casts of salt present in coarse siltstone beds above microlaminated 1, uppermost fining-upwards cycle portion of division 2. of lower Towaco cycle still exposed along eastern boundary of park. The 5, massive fine gray siltstone in upper and middle parts of this cy- upper parts of division 2 have cle have the best reptile foot- well-preserved conifer foliage, prints in the quarry and hold the pollen and spores, individual fish key to the park's development. Foot- scales (Semionotus), and rare in- prints are especially abundant in sect fragments. interbedded sequences of possible crevasse splay sandstone and flood 6, complex series of sandstones and basin siltstone. Basal sandstone siltstones of division 3 showing portions of cycle are usually deep- features suggestive of both later- ly down cut into underlying beds ally migrating channels and prograd- and contain beds of mud-chip con- ing deltas. glomerate and casts of tree limbs and roots. Uppermost portions of 7, lowest fining-upwards cycle in the cycle consist of fine siltstone division 4 (Figure 49) shows slip- transitional into the lower parts off faces of point bar and beds of of division 1 of the upper Towaco intraformational conglomerate with cycle. Transitional beds with numer- coprolites, fish scales, reptile ous red siltstone roots surrounded bone fragments, and abundant dino- by greenish halos. saur footprints. The latter fea- tures could represent a dinosaur 2, exposure of complete Towaco cy- "wallow". cle. Division 1 contains prominent fine sandstone beds with large 8, 10 successive fining-upwards cy- calcareous concretions which cles of division 4. Rill marks very weather out to form limonite filled well developed in bank portions of cavities and extensive large (1-4 one of the middle cycles. These cm) coalif ied roots which probably sorts of rill marks, typical of belong to confier trees. Crevasse channels with rapidly dropping splay beds in division 1 covered water levels, have long been con- with little dinosaur footprints. fused with plant remains (it is Identical beds occur in division 2 easy to see why) and have received of this cycle exposed in Chatham, the name Dendrophycus (Newberry, New Jersey, 13 km south of here. 1888).

3, microlaminated portion of divi- 9, unique small reptile footprints sion 2 has very well developed with structure highly suggestive of white-black microlaminae, however advanced mammal-like reptiles or no fish have been found here yet. mammals are present in upper fin- Upper parts of microlaminated beds ing-upwards cycles. If they do contain distinctive nodules of represent mammals, they will be the black chert. The black, coally-look- oldest North American record. ing siltstone surrounding the chert bed has several bedding thrusts 10, very badly weathered "tuff" between normal Towaco Formation and lished by glacial scour, con- Hook Mountain Basalt. This unit is glomeratic structures are displayed enigmatic but very widespread at in great detail.. Cyclical and later- this stratigraphic position. Fresh ally continuous beds of poorly exposures were described by Lewis sorted debris flows' grading upward in 1908 and Olsen, 1980a. into cross-bedded. and -ripple marked sheet-flood deposits are charac- Leave Walter Kidde Dinosaur Park teristic of the section (Figure and Riker Hill Park returning to 29). Many of the cycles are incom- Beaufort Avenue. Turn right (north) plete, having been partiallyeroded onto Beaufort. by a subsequent debris flow. Each section is about 2 to 3 cm thick Turn right off Beaufort onto Eisen- and occurs within larger cyclical hower Parkway heading north. units of about 1.5 m thick. The clast population has a graphic Enter I 280 westbound. (Folk, 1974) mean size of -3.3 phi,, and an inclusive graphic standard Crossing the Passaic River. For deviation (Folk, 1974) of 2.2 phi approximately the next 6 miles we (Figure); it is, therefore, very will be crossing the lake beds of poorly sorted. In general, the Glacial Lake Passaic. grains are angular and primarily composed of a quartzite, gneiss and Merge with Interstate Route 80 west- vesicular basalt with subordinate bound; bear right, follwoing signs amounts of amphibolite, slate and for Interstate 287, Boonton. greenstone schists. They appear to have been derived from a local Enter Interstate 287 northbound, source. following signs for Boonton. Take Interstate 287 to the end of the Some of the primary structures seen highway. at the section include: ripple drift cross-lamination, dessication Right turn at exit onto Route 202. cracks, cut-and-fi 11 channels, nor- mal and inverse grading, sand At Montville Inn, bear left and waves, parting lineations, anti- enter onto River Road. Caution-- dunes (?), random fabric, sand sha- this is a dangerous intersection! dows, dreikanters and oriented clasts. Park car on "paper" street on left- hand side of road (opposite Dahl Particle orientation was determined Ave.). Walk east to outcrop. from clasts having a length to width ratio of at least 1.3:l. The STOP 6. Boonton Formation (Fan- prevailing long axis orientation is glomerate). Marginal Border Facies west-to-east with clast imbrication (Figure 29). to the west. This is incompatible with a preliminary paleocurrent Objective: To examine an alluvial study showing that the clasts were fan facies within a fan delta se- transported to the basin by east- quence (Figure 30). flowing streams. The occurrence of aligned vertifacts indicates that Background: Field descriptions and the wind was an effective agent of photographs of this section are erosion, and may explain the defi- included in the text under, "Boon-- - ciency of fine sand and clay size ton Formation: Marginal Border particles on the alluvial fan. Fades.'' Turn around and go back to 202 Because the section has been po- . northbound (right-turn at Montville

59 Inn). Enter Route 287, southbound. ROAD LOG (Sunday) Boonton Formation pebbles along . roadbank. Note: The sunday field log begins 2.5 miles north of Milford, N.J., along N.J. Boonton Reservoir on left~siteof Route 29 at RR milepost 37. Our trip from famous Boonton fish fossils. New Hope, Pa. to Miford, N.J., via Pa. Route 32 north, takes us through the Continue on Interstate 287 and the scenic and historic Delaware River Val- route 202 south to New Hope, Pa., ley. We will be traversing the Triassic via Sommerville, Flemington and Province, going up-section. Descriptions Lambertville, N.J. of field stops 1-3 are taken directly from Van Houten (1980) End of Day One 0.0 STOP 1. Hammer Creek Conglomerate, Pebble Bluffs at culvert.

0.5 STOP IB. Conglomerate in steep road- cut at RR milepost 37 (0.5 mi s). Southward projection lobe of quart- zite-rich fanglomerate dipping 10-15' NW. Most clasts are imbri- cated. Bedding is very poorly developed; cross-bedding is vir- tually absent.

The poorly sorted detritus is ar- ranged in crudely fining-upward sequences about 7-9 m thick with a scoured base, multi-storied units of conglomerate, and calcareous patches and nodules (calcrete pale- osol) in the upper sandier part.

Significant items:

1. Outcrop less than 5 mi. from border fault.

2. Source probably less than 25-30 mi. to N.

3. Clasts and matrix derived from Paleozoic rocks now stripped from the uplands.

4. Fining-upwards sequence and cal- Crete common in alluvial fans.

5. Lensing and channeling well- displayed at south end of bluffs.

6. Rapid gradation southward into distal, finer-grained fades.

7. Fault- in ravine between two major outcrops. 1.1 STOP 2. Long roadcut in essentially stone. Gray units consist of black, horizontal middle Brunswick Mud- pyritic platy muddy limestone and stone south of Spring Valley Road. calcareous mudstone. .The Perkasie Bright reddish-brown mudstone in Member apparently is about 1400 m patterned sequences about 950 m below the 1st Watchung flow. Inter- above base of formation (Picard and vals of reversed magnetic polariza- High, 1963) tion have been identified below both the Perkasie and L and M Items along 0.2 mi traverse: units, as well as just below and above the Graters Members lower in 1. Normal fault at E end of expo- the Formation (W.C. McIntosh). sure down to E. conspicuous joint- ing. 2.5 Milford. Turn E on Main Street, then S at traffic light on Rt 627. 2. Succession of about 30 massive mudstone and hackly claystone al- 4.5 STOP 3. Middle Brunswick Mudstone, terations averaging 1.5-3 m thick roadside excavation. Well-displayed (Picard and High, 1963). Few units bedding surface markings, including with persistent 1-2 cm beds of silt- several sizes of shrinkage crack- stone. patterns, burrows, and small tracks and trails, many probably made by 3. Abundant burrowing has destroyed small crustaceans (Boyer, 1979). lamination in mudstone. Absence of bedding in claystone may be result 6.1 Frenchtown. Turn E on Main Street, of small-scale physical disruption. than S on N.J. 29.

4. Distinct 2-6 cm layers filling 9.5 Gray units E and F exposed in abandoned channel (Figure 6 1. Fine- ravine and along side road. Gray to-medium grained feldspathic sand- units G and H above 100 m higher in stone in lower part of each layer section constitute the Graters Mem- derived from Southeastern Na-feld- ber (40 m thick). spar rich source areas. Some layers are graded. Tops are marked by bur- STOP 4. Warford Creek exposures of rows and shrinkage cracks. Aban- member D of the Passaic Formation. doned channel may have been part of interfluvial drainage of extensive The gray members of the Passaic For- alluvial plain (Allen and Williams, mation mapped by McLaughlin (1946) 1979) or a shallow waterway in a consist for the most part of bun- clay-flat playa. dles of short sedimentary cycles very similar to detrital cycles of 5. Hammer Creek tongue of dark the Lockatong Formation (Van reddish-brown Paleozoic quartzite- Houten, 1969; Olsen, l980a, 1980~). clast lithic-rich sandstone 3 m The exposures along Warford Creek above road E and W of ravine and consist of one complete cycle culvert. (Figure 31). On the basis of the same criteria as are used for Lock- 1.8 Dark gray Perkasie and L and M mem- atong detrital cycles, this Passaic bers of Brunswick Formation 930 m Formation cycle can be cut into above Lockatong Formation. These three divisions. At these expo- are highest of 8 recurring gray sures, the organic rich lower parts units in the Delaware Valley re- of division 2 are microlaminated gion, centered at 120-137 m inter- although this is obvious only in vals. Several have been traced to thin section. These microlaminated NE into Hammer Creek Conglomerate, beds contain poorly preserved part- as well as 25 km to SW where they ly articulated Semionotus and very interfinger with reddish-brown mud- small conchostracans. The lower pa,rts of : division 3 contain Byram diabase sheet and about 450m Scoyenia - type burrows, numerous above the Stockton-Lockatong con- tool marks and possibly very poor tact. According to Van Houten reptile footprints. The lateral ex- (1969) nepheline is. absent above tent of individual short cycles the 11-foot mark and cancrinite and within Passaic Formation gray mem- albite diminish while analcime and bers is unknown. thomsonite increase towards the 370-foot mark. 10.7 Lowermost Brunswick Formation, Tum- ble Falls. Ravine and high roadcut Large abandoned quarry is at 150- in lowest reddish-brown unit and to 300-foot mark. Exposures consist lowest gray unit C (40 m thick) of cancrinite hornfels principally about 75 m above base of Formation. in chemical cycles (Van Houten, 1969). Two well developed detrital Top of Lockatong Formation (top of cycles are exposed at the north end gray unit B). Base of Brunswick of the quarry. The section between Formation has been placed arbi- 300 to 1020 feet is especially well trarily below the lowest thick exposed showing very clearly alter- reddish-brown unit even though its nating bundles of detrital and lower part is more like upper Lock- chemical cycles. atong deposits than the upper part of the Brunswick Formation. Chemical cycles are on the average 5 meters thick and consist of two 11.4 Double Red unit exposed in creek to major varieties. One type resembles East is uppermost reddish-brown detrital cycles in having a lower sequence of analcime-rich chemical black or gray platy siltstone. cycles assigned to the Lockatong Generally, however, fissility is Formation. The reddish-brown inter- not as well developed in this unit vals of this sort are the most as in division 2 of detrital cy- analcime-rich and recur in a cles. And even the darkest silt- 105-120 m pattern of long cycles in stone units contain tan weathering phase with thick reddish-brown dolomitic beds (Van Houten, 1969). units in the Brunswick Formation. The middle parts of these cycles contain more massive dolomite beds 12.0 Triple Red unit in abandoned build- and the upper parts contain even ing-stone quarry to East about 1000 more massive beds of gray very hard m above base of Lockatong Forma- and blocky siltstone (argillite) s- tion. Red units were favored for peckled with analcime and dolomite. building blocks because of their more interesting variegated colors. The other variety of chemical cycle has a lower platy gray to gray- STOP 5. Long road cut in upper Lock- green often dolomitic siltstone atong Formation and Byram diabase which is usually disrupted by numer- sheet, a section described in de- ous shrinkage cracks. This basal tail in Van Houten (1962, 1964, unit grades upward into a deep 1969). Well marked patterns of mauve, blue-gray, or red massive detrital and chemical cycles and siltstone with abundant analcime. their groupings into 25 m and 100 m These sorts of chemical cycles are higher order cycles can be easily most common in the upper part of seen here. (Figure 32). Van Houten this section (Figure 32) and these (1969) has marked cumulative strati- red chemical cycles make up the graphic thicknesses on the outcrop 'first thin red" unit mapped by starting at the 0 mark on the south- McLaughlin. This type of chemical ernmost exposures of this section. cycle passes laterally into typical Base of section in Figure is about Passaic Formation red beds outside 21 m above faulted contact with of this central area. Some of the thicker chemical cycles which have that the cycles exposed and mapped a lower black siltstone, lose their in northern New Jersey correlate analcime laterally and so become with detrital cycles in the lower detrital cycles. parts of the Lockatong along the Delaware. Detrial cycles are an average of 4.5 to 6 meters thick at this sec- 17.5 STOP 6. Active quarry in upper part tion. Each cycle can be divided of Prallsville Member of the Stock- into three divisions. (Figure 32). ton Formation. Section is about 61 The lower massive to platy dark rn thick and begins about 760 rn gray silt stones of the previous above the base of the Formation cycle. Prominent, easily weathered (Van Houten, 1969, 1980). laminated black siltstone (division 2) is sometimes microlaminated Four major sediment types are ob- (only once in this section). In vious at these outcrops: non-microlaminated parts of divi- 1) massive, well sorted medium sion 2, very small burrows and grained gray to buff arkose with delicate shrinkage cracks are com- faint to prominent large scale mon. Division 3 is more massive and cross bedding. consists of feldspathic siltstone and fine grained sandstone. The 2) massive to crudely cross bedded siltstones are almost always inten- thin (2 m) arkosic conglomerate sively disrupted by shrinkage units some of which are locally cracks and also show a variety of kaolinized. sole marks including reptile foot- prints. These divisions record the 3) well bedded red coarse silt- development, maintenance, and ex- stone, intensely and obviously bio- tinction of very large lakes. turbated.

Above Van Houten's 720-foot mark 4) blocks and massive red siltstone (Figure F) is the only cycle in resembling much of the Passaic this section with a well developed Formation. microlaminated division 2. As is the case with virtually all micro- The intense bioturbation seen in laminated bed in the Newark Super- the red coarse siltstone clearly ex- group, this one is rich in organic tends into the massive arkose as carbon, whole fossil fish (in this can be seen on the lower surfaces case, Turseodus), coprolites, and of the arkose beds. Two main types conchostracans. A small rock fall, of bioturbation are dominant. One apparently from division 3 of this is the arthropod burrow Scoyenia, cycle has exposed several poor and the other is large and small phytosaur footprints (Figure 33). roots. Large roots are especially Some bedding planes in this shrink- abundant in the massive arkose beds age cracked unit are covered with where they are replaced by an iron- small concostracans. rich carbonate mineral which weathers to limonite. All of the The lower part of the Lockatong sediments at this exposure show (very poorly exposed in this area) roots. has a much higher frequency of detrital cycles (Van Houten, 1964) Both the roots and the abundant bur- with many more microlaminated rows attest to high productivity in units, and more fossils than the a very shallow water or terrestrial upper part of the Lockatong. Some environment. Presumably this repre- of the lower beds of the Lockatong sents a fluvial to deltaic environ- are exposed in small ravines fur- ment in which all the sediments be- ther to the south. It seems likely come soils sooner or later before burial. The complete lack of or- ganic carbon in all the sediment is a testimony to the high ecosystem efficiency of this primarily ter- restrial ecosystem.

Return to bus and travel to the Stockton Inn for a fine lunch and good cheer.

END OF FIELD TRIP Figure 1 Map of the Newark Basin showing route of field trip and field stops. SCALE (km)

- EXPOSED INFERRED

Fig. 2 Newark Supergroup of eastern North America. Key to numbers given in Table 1. The Newark Basin is 11. Data from Olsen, 1978. me. 3 The Newark Basin. A. Geologic map showing distribution of formations, normal, it is clear many, if not all of them, have some conglomeritic fades (irregular stipple), and major clusters. component of strike slip, although the significance of this of deirital cycles in Passaic Formation (parallel black lines) component is unclear. Symbols for the names of structural - abbreviations of formations and diabase bodies as features used in this paper are as follows: A, Montgorncry- follows: B, Boonton Formation; C, Coffman Hill Diabase; Chester fault block; B, Bucks-Hunterdon fault block; C. Cd, Cushetunk Mountain Diabase; F, Feltvillc Formation; Sourland Mountain fault block; D, Watchung syncline; E, H, Hook Mountain Basalt; Hd, Haycock Mountain New Germantown syncline; F, Flernington syncline; G, Diabase; Jb, Jacksonwald Basalt; L, Lockatong Sand Brook synche: H, Jacksonwald synchne; 1, Rarnapo Formation; 0. Orange Mountain Basalt; P. Passaic fault; J, braided conncctoin between Rarnapo and Formation; Pb. Preakness Basalt; Pd, Palisade Diabase; Hopewell faults; K, Flernington fault; 1, Chalfont fault; Pk, Perkasie Member of Passaic Formation; Rd, Rocky M, Hopewell fault. Hill Diabase; S, Stockton Formation; Sc, carbonate Fades of Stockton Formation; Sd, Sourland Mountain Diabase; Data for A and B from Kiirnrncl, 1897; Lmis and Kurnrnel, T, Towaco Formation. 1910-1912; Danon. 1890. 1902; Danon. et a!., 1908; Glaescr, 1963; Sanders, 1962; Van Houten. 1969; B. Structural features of the Newark Basin. Faults are all Mclaughlin. 1941. 1943. 1944. 1945, 1946a, 1946b: drawn as normal with dots on the down-thrown side; Bascorn, el a!.. 1909; Willard, el at., 1959; Faille, 1963; portions of basin margin not mapped us faults should be Manspeizcr, pcrs. comm.; Olsen, in press, and personal regarded as onlaps. While ¥Ithe faulu arc mapped here as observation. Table 1

Key Rock-stratigraphic term Basin name Age range Figure 1 Carnian-PNorian 1 Chatham Group Deep River Basin (Late Triassic)

2 undifferentiated Davie County Basin ?Late Triassic

?Carnian (Late Farmville Basin 3 undifferentiated Triassic)

4 small basins south PCarnian (Late "4 undifferentiated of Farmville Basin Triassic)

Dan River and Danville Carnian-?Norian -5 Dan River Group Bas ins (Late Triassic)

Tuckahoe and Richmond Basin and Carnian (Late Chesterfield Groups subsidiary basins Triassic) 1 Norian-'{Sinemurian 7 none Culpeper Basin (Late Triassic- Early Jurassic)

I Carnian (Late Taylorsville Basin 8 none Triassic)

Scottsville Basin and ?Late Triassic- undifferentiated 9 I 2 subsidiary basins Early Jurassic Carnian-Het tangian 10 none Gettysburg Basin (Late Triassic- Early Jurassic) Carnian -Sinemurian Newark Basin (Late Triassic- Early Jurassic)

?Late Triassic- 12 none Pomperaug Bas in 1 1 Early Jurassic

Hartford Basin and Norian-?Bajocian 13 none subsidiary Cherry (Late Triassic- Brook Basin ?Middle Jurassic) ?Norian- ?Toarcian 14 none Deerfield Basin (Late Triassic- Early Jurassic) k 4 ?Middle Triassic- Fundy Group Fundy Bas in I l5 I Early Jurassic 1 ------Chedabucto Format ion Chedabucto Basin ?Late Triassic- ("Eurydice Format ion?) I l6 I (-Orpheus Basin?) I Early Jurassic 1 Southern China European Europe Africa tandard Stagel

cave @per Sandstone Lufeng Sinemurian

LiJI Upper Towaco FIB. ~ed~eds

Lower Lufeng

upper ha Rhaetic Ithaft ian ------Colorçdo Lower lower LOB st*inÑrge1 Red Beds Colorados Morian keuper

1 ?

Carnlan Lockacong b. ~schigulasto rç Molten0 Stockton Fm /

Fig. 4

A. Distribution of most abundant vertebrate and invertebrate B. Correlation of the formations of the Newark Basin with fossils in the Newark Basin; a, taxa thought to be other Mesozoic sequences. biostratigraphically important; b, taxa thought to be of little or no stratigraphic value. Letters in parenthesis--(f), Data for A and B from: Cornet (1977); Olsen (in press; (r), (a), (t)--indicate nature of fossils: (a) amphibians; (f) Olsen and Galton (1977); Olsen, McCune, and Thomson (in fish; (r) reptiles; (I) reptile footprints. press); Olsen, Baird, and Salvia (MS); and Olsen and Colbert (MS). Fig. 5 Cross-section of the pre-Orange Mountain Basalt portion Orange Mountain Basalt and to the immediate left the of the Newark Basin: A, position of section in Newark Flemington Fault; d, Hopewell Fault; e, Orange Mountain Basin; B, present cross section--note that the vertically Basalt of Watchung syncline; L, Lockatong Formation; P ruled band represents diabase and gabbro sills and plutons; Passaic Formation; P;. Perkasie Member of Passaic C, reconstructed section with Passaic Formation-Orange Formation; S, Stockton Formation. Note that the Mountain Basalt contact as horuontal--note thinning to trigonometrically calculated thickness of Passaic east and ramping to west. Formation east of the Watchung syncline has been reduced Abbreviations as follows: a, Haycock Mountain Pluton; b, by 25% as a correction for dip slip faults. Coffman Hill Pluton; c, Flemington syncline outlier of Loclcatong Fm. Passaic Fm. Feltville Fm. Towaco Fm. Boonton Fm.

4 A tz

gray-matrix conglomerate gray siltstone reptile stromatoliti massive \crossbedded A footprints around tree red-matrix conglomerate contorted fabric" articulated gray siltstone reptiles I plant remail red sandstone dark gray poorly spores and massive \crossbedded laminated siltstone A pollen gray sandstone calcareous siltstone massive \ crossbedded laminite f whole fish roots red siltstone rn massive \ crossbedded limestone laninite 0 fish scales @ conchostract

~i~.6Major types of sedimentary cycles of the formations of the Member (i.e., Member G) and are characteristic of most of Newark Basin. Note that the approximate center of the the detrital cycles of the Passaic Formation. The upper symbols for the major types of fossils found is placed about cycle develops a dark gray siltstone a kilometer to the where they occur in the section to the left. Note the change south. Feltville Formation section measured along East in scale (in meters) from section to section. Branch of Middle Brook, Martinsville, New Jersey--there is only one such "cycle" in the Feltville Formation. Towaco Lockatong Formation section measured at Kings Bluff, ti^^ section measured along stream 2 km southwest Weehawken' three detrital New Jersey and represents of Oakland, New Jersey; three cycles are shown. Boonton cycles. The Passaic Formation section measured along Formation section is upper part of type section (see Figure Nishisakawick Creek and Little Nishisakawick Creek, don not cyclic, northeast of Frenchtown, New Jersey; the two cycles shown represent the lower portion of McLaughlin's Graters PALEOFLOU D

AYYGilALOIilAL 6 VESICULAR FLOW TOPS

PALAGONITE FORSET BEDDIh

PAHOEHOE LOBES

TUMUL I

DELTAIC FORSET BEDDING SUBAQUEOUS FANS SHELF CARBONATES INTRUSIVES

BEDDED PILLOM BUDS

SUBAQUEOUS FLOW LOBES

SPIRACLES

UPPER COLONNADE

LOWER COLONNADE PIPE VESICLES 6 AHYGDALOID

FLUVIAL SANDS

Fig. 7 Schematic diagram of the volcanic and sedimentary structures to be studied on the field trip. , WEST

^^^.*... TALUS COtONKADES PAHOEHOE TOES WSSIVE BASALT -: ,* AfWSDAlOLDRL FLOW SURFACE BEDDED PILLOW BODS OF OLDER FLOW UNIT ENTABLATURE UBAOUEOUS VOLCAN IC VENT W^ SPIRACLES CROSS SECTIONS OF FLOW LOBE PILLOtfS ENTABLATURE COLUMNS

Figure 8 Field sketch of volcanic structures studied in the second flow unit of the Orange Mountain Basalt in the Upper and Lower New Street Quarries and along 1-80; note: longitudinal section of the subaqueous flow lobe, volcanic vent, bedded pillow lavas, an overlying Tomkeieff sequence and underlying amygdaloidal flow top. 0 50 100 OS) BEDDED PILLOW BUDS tttfte MASSIVE BASALT PAHOEHOE TOES COLUMNAR BASALT

Fig. 9 Field sketch of the lower New Street Quarry, showing transverse section of the subaqueous flow lobe, volcanic vent, and overlying bedded pillow lava.

Fig 10 Schematic block diagram illustrating volcanic structures and paleogeography of the Newark Basin diiriny the extrusion of the First and Second Watchung lavas. STRUCTURE STRUCTURE METERS APPARENT MODAL CLASS SIZE (mn) PYROXENE PLAGIOCLASE GLASS' OLIVINE

Ill1 oooog +(M<¥à w trac e

IÃ trac e

trac e

Fig. 11 Plot of mineral and glass content and texture against the Tomkeieff sequence of colonnades and entablature, Orange Mountain Basalt, 1-280, West Orange. Phoenixvll!e, Pa.

black and gray =microlaminated siltstone black and gray L laminated siltstone vertical scale gray siltstone (meters) Y buff arkose

red siltstone

Scovenia

roots

Fig.12 Generalized fades relationships of Lockatong detrital (Stockton, New Jersey), which in turn, is 27 krn from the cycles (horizontal distances not to scale); Phoenixville is 50 northern corner of the plateau and 105 krn from km from the southern portion of the Hunterdon Plateau Weehawken, New Jersey. ^'^/gray fissile siltstone laminated black limestone red crudely laminated siltstone laminated while limestone basalt breccia black calcarenite Orange Mountai~Basan white calcarenite dinosaur loot~mts folded black limestone a-t.culated fish black topTkrbne gray limeslone Conglomerite fish scales black bonedmbr bow crudely bedded gray s~ltstone ostracods '"drayf ine siltstone megafossil plants reddray sandstone pollen and spores cross bedded coarse sandstone roots

Fig. 73 Small scale lateral change in Washington Valley Union and Somerset Counties); D, outcrops along Green member: A, outcrop along East Branch about 145 m Brook north of (c) above and about 2001~1,south of the northwest of Vosseller Road near intersection with Roberts Plainfield Avenue bridge over Green Brook; E, two Road, Somerset County, New Jersey; B, banks of small combined sections, 400m apart, one on the south, one on stream running parallel to and on the southeast side of the north side of Blue Brook about 1.9km and 2.3 km Valley Road, 1.6 km north of Watchung, New Jersey rotary respectively, upstream from the crossing of Sky Top Drive (Somerset County). Elsinore Drive crosses this stream over Blue Brook, Watchung Reservation, Union County, 80-100 m down stream from locality; C, bluffs and pool New Jersey - type section of the Feltville Formation; F, exposures along Green Brook about 400m northeast of outcrops in bluff of small tributary of Blue Brook, 260111 intersection of Plainfield Avenue, Valley Road, and Bonnie south of Lake Surprise, Watchung Reservation, Union Burn Road and about 618m down brook from overpass of County, New Jersey. Plainfield Avenue over brook (outcrops at boundary of New Germantown (Oldwick) kilometers

I'.*''...I

black laminated limestone, siltstone, and calcarenite white laminated limestone and calcarenite

sandstone and siltstone of 'turbidite facies"

crudely bedded gray siltstone

gray siltstone and sandstone with footprints, roots, and megafossil plants red siltstone and gray. buff, and red sandstone with roots and footprints

ORANGE MT. BASALT

LNE

~i~J4Lateral facies relationship in Washington Valley member. cycle divisions

Generalized Towaco Formation cycles. Description in text. Pompton

black or gray laminated siltstone A

- Fig. 16 Lateral facies relationship within divisions 1-3 of Towaco cycles. Table 2

Features explained by both the algal mat model and the stratified lake model

1. production and preservation of microlaminated sediments 2. laminations composed of carbonate plus organic-rich couplets 3. organic component of laminae algal in origin at least in part

Features unique to each model

A. Algal mat model

1. laminations of limited extent laterally 2. few if any fish 3. shallow water microlaminated zone surrounds in time and space a deeper water non-laminated zone 4. associated blister and pinnacle mats

B. Stratified lake model

1. laminations traceable over large area 2. abundant whole fish 3. laminated lithesome is deepest water deposit and lacks a central non-laminated port ion 4. blister and pinnacle mat structures absent Figure 17 Diagram contrasting lakes conforming to the Agal Mat Model and the Stratified Lake Model (A) and the shape of the sediment lithosomes they should produce (B) after one episode of expansions and contraction of the lake. For construction of the shapes of the lake sediment lithosomes the shape of the lake basin was held constant throughout sedimentation as water level changed. Each "time line" marks off equal thicknesses of sediment deposited during a constant unit of time and marks off a plane deposited over the lake simultaneously.

Note that in the Algal Mat Model lithosome "time lines". are discontinuous while in the Stratified Lake lithosome they are continuous. In the Stratfield Lake Model "time lines" can be considered microlaminae or varves. 20 ism

Figure 18

The relationship between lake depth and the angle of slope of the basin floor assuming a 20 km distance from the deepest part of the lake to the shore and a triangular cross section of the lake. Figure 19

Elipse encompassing most of the known distribution of the microlaminated beds in the Lockatong Formation. The major and minor axial diameters are 170 and 40 km respectively, which correspond to the greatest and least possible fetches for winds blowing across the part of the lake which is assumed to be deeper than the depth of wave mixing. 20 wind speed- Cw) m/sec.

Figure 20

Graph of the relationship between wind speed (W) and depth of wave base (A/2) for the greatest and least fetches of Figure 19. broad levelf 1 BUFF ARKOSE LAMINATED SILTSTONE =BEDDED SILTSTONE a DIABASE

Fig. 2 1 Exposures of discordant contact of Palisade Diabase Bridge on road from River Road to Ross Dock in Palisades and Lockatong Formation, south of George Washington Interstate Park, Fort Lee.

NE DIABASE

J Fig. 2 2 Exposures of Palisade Diabase and cycles 0-d west of Ross Dock, Palisades Interstate Park, Fort Lee. Figure 23 Section west of Ross Dock, Palisades Interstate Park, Fort Lee showing distribution of major fossils and paleocurrent data (n-7) for crossbedded buff arkose between cycles 6 & a.

87 Fig. 24 Lockatong Formation vertebrates and reptile footprints Grallator sp., left pes: H, Gwyneddichnium minore, right from the upper Stockton, Formation (for repository pes; I, Rhynchosauroides brunswicki, right manus and pes; abbreviations see Olsen, this Fieldbook) (From Olsen. In J, Chirotherium cf. eyermani, right manus and pes; K, prep.); A, Tanytrachelos cf. ahynis, reconstruction; B, Carinacanthus jepseni, reconstruction; L, Turseodus sp., Rutiodon carolinensis, reconstruction; C, Eupelor durus. reconstruction; M, Synorichthys sp. reconstruction: N reconstruction; D, Icarosaurus siefkeri, reconstruction; E, Cionichthys sp., reconstruction; 0, semionotid of the "deep tailed swimmer", tentative reconstruction; F, "Semionotus brauni group", reconstruction; P, Diplurus Apatopus lineatus, composite right manus and pcs; 0, newarki, reconstruction. Scale 2 cm. microlaminated gray laminated gray laminated white folded microlaminated siltstone siltstone siltstone siltstone Fig. 25 Comparison of section of cycles 5 and 6 showing Tanytrachelos; TU, Turseodus; Sy, Synorichthys; S, distribution and preservation style of fish: A, Kings Bluff, Semionotus. Open column under abbreviation of taxon Weehawken; B, Gorge and River Roads, Edgewater; C, stands for presence of dissarticulated fish while solid "old trolley route". Fort Lee, D, west of Ross Dock, column indicates the presence of complete specimens. Palisades Interstate Park, Fort Lee. Lithogic symbols as in Figures 29 and 30 except as Abbreviations for fossils as follows: D, "deep tailed shown. swimmer"; Dp, Diplurus; C, Cionichthvs: T, CALCITE CONCRETIONS

CALICHE CLASTS RIPPLE DRIFT CROSS-LAMINATION

CALCITE CONCRETIONS GRAY SILTSTONE WITH WORM BURROWS

CUT-AND-FILL CHANNELS

VARIEGATED SHALE GREEN-GRAY SHALE

PLANT DEBRIS GREEN-GRAY MICACEOUS SILTSTONE CALICHE CLASTS WORM BURROWS CALICHE CLASTS

GRAVELLY SAND. -4U to -t>W PLANAR-to-LOU-ANGLE CROSS-BEDS

RED SILTSTONE

ARKOSE SANDSTONE CHRYSOCOLLA GRAY-GREEN SHALE

26 .Columnar section through part of the Passaic Formation, an inferred fluvial-playa sequence; 1-280, East Orange. $ rept ile footprints

/ reptile bone fragments

# articulates fish

fish scales

1 insect fragments

9 "megafossil' plants

pollen and spores

A roots

laminated black st ltstone - ,c..,.-'- slump depos t and turbidites

stone

idstone

Figure 27

Section at Roseland Quarry. Only cycle A and Hook Mountain Basalt are presently exposed. cycle laminated black sillstone clists Oivisons m ibl*ck sitls~onematria TJ gray poorly sorted coarse siltstone ,' / t-' with black siltstone clists

black poorly bedded siitstone

sandy proximal turtioiles (gray)

silly distal IurWiles (black)

k-3 k-3 gray line SanaSIone grayslltstone d~scontinuously and sanaslone loifled an0 gray

poorly toned siltslone

j lining-upwards gray sillstone

1-1 1-1 gray massive sinstone

# articulated fish

& pollen an0 spores

A roots

Slump movement azimuths N

fr- -; meters

Section along strike of upper part of division 1, all division 2, and lower division 3 of cycle B Roseland Quarry. Fig. 29 Stratigraphic section through that part of the Boonton Formation inferred to represent an alluvial fan prograding eastward from the western border fault. CENTRAL BASIN FACIES -4- MARGINAL RIFT FACIES ~-* + BORDER OF DEPOSITIONAL BASIN

Fig 30 Fan delta sequence, showing the distribution of facies in the basin. Figure 31

Short cycle comprising a part of McLaughlinls Member D of the Passaic Formation. Exposures are along Warford Creek (Stop 4). 0i-o iff "i za¥" $5 uQ %'E 0-2 ^->-->" $6 '"(_e 8-c-E 3's- $ g3 ?j gs i-# ?- P8 Lg y cz ? color SfP 3"-A< D< p $ - - + -T '& PT ^ 5 il

Figure 32 Detailed section above Van Houten's (1969) 600 foot mark (Stop 5 of this guide book) and detail of a single detrital cycle. Note that this detrital cycle is Lhe only one in the section known to have whole fish and a well developed microlaminated unit. Figure 33 Footprints from division 3 of the single detrital cycle detailed in Figure 32. These are very poor footprints appar- ently belonging to the footprint-genus Apatopus and were probably produced by a swimming phytosaur in shallow water. About 10 cm above this bedding surface is a unit with irregular parting planes covered with small conchostracans. REFERENCES CITED

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