apparently it is missing in northern Connecticut and Massachusetts. In most of southern Connecticut, the Talcott is a single basalt flow of variable thickness (30-75 m). Sanders (1970) has shown that within the Gaillard Graben, which is restricted to the southeastern part of the basin, the Talcott Formation exists as four lava-flow units interbedded with three sedimentary units, totaling about 305 m. The Gaillard Graben has been interpreted as a post-depositional structure (Sanders, et al., 1963, p. 11). However, the existence outside the Graben of only one (the lowest?) lava flow suggests that penecontemporaneous erosion removed much of the once continuous Talcott Formation before deposition of the overlying Shuttle Meadow Formation, and the Talcott was preserved in the graben as a result of downward displacement of sediments in the graben before the erosional cycle began. On the other hand, the absence in northern Connecticut and Massachusetts of basalt units referable to the Talcott might indicate only that the basalts did not extend that far north. However, it seems reasonable that 300 m of superimposed volcanic cones in Mt. Hitchcock in northern Massachusetts (Bain, 1941) may be related to the lava flows of the Gaillard Graben, judging from stratigraphic position and thickness.

The Shuttle Meadow Formation, like the Talcott Formation, varies considerably in thickness and in extent over the basin. In the southernmost part of the basin, within the Gaillard Graben, the Shuttle Meadow Formation reaches its maximum thickness of about 270 m (Sanders, 1970). The formation steadily decreases in thickness northward: 170 m in North Guilford, Conn.; 94 m near Middletown, Conn.; 94 m at type section, New Britain, Conn.; 30 m in Farmington, Conn.; 15 m near Simsbury, Conn. (Krynine, 1950; Lehmann, 1959; Schnabel, 1960). The upper part of the formation appears to be the most extensive. North of Simsbury the Talcott basalt disappears, and the Shuttle Meadow Formation, if it continues north, would be recognized as the uppermost part of the New Haven Arkose in northern Connecticut and Massachusetts.

The Holyoke lava-flow unit conformably overlies the Shuttle Meadow Formation in Connecticut, and the New Haven Arkose and Hitchcock volcanics in Massachusetts. This unit, consisting of at least two lava flows, ranges in thickness from 120 to 170 m over most of the basin, but it has been recorded under 92 m near the eastern and northern edges of the basin (Bain, 1941).

The East Berlin Formation conformably overlies the Holyoke lava-flow unit, and appears to thicken both northward and southward from its minimum thickness near Avon, Conn.: 326-458 m in the Gaillard Graben, Branford, Conn.; 170-180 m near Middletown, Conn.; 140-150 m near Avon, Conn.; 250 m near Westfield, Mass. (Krynine, 1950; Lehmann, 1959; Schnabel, 1960; Colton and Hartshorn, 1966; Sanders, 1970). In the northern part of the basin, the upper part of the East Berlin Formation interfingers with the Granby Tuff and local lava flows (Brophy et al., 1967). These volcanics and pyroclastics contain at least one flow that apparently is continuous with the Hampden lava-flow unit (Bain, 1941).

The Hampden lava-flow unit conformably overlies the East Berlin Formation and ranges in thickness from 18 to 60 m. Much of this variation in thickness seems to be the result of differences in the number of internal units or flows, which varies from two to eight (Chapman, 1965). In southeastern Connecticut a 12 m sedimentary unit has been found separating two flows (Sanders, 1970).

The Portland Formation, which conformably overlies the Hampden lava-flow unit and interfingers with some of the Granby Tuff (Bain, 1941), has a maximum thickness of more than 2000 m in Massachusetts. The "Chicopee shale" and "Longmeadow sandstone" are here considered as local members, at present recognized only in Massachusetts. In Connecticut, where reported thickness rarely exceeds 920 m, post-depositional faulting and erosion are responsible for removing much of this formation.

DESCRIPTIONS OF PALYNOFLORULE LOCALITIES

Of the 13 palyniferous localities thus far discovered in the Hartford Basin (Text-fig. 2, 3), 4 have been selected as palynoflorule localities for purposes of formal description in this paper. Samples from the 9 remaining localities have yielded the same species of palynomorphs that are found at the formally described localities.

Palynoflorule Locality No. 8

Formation: Upper New Haven Arkose.
Stratigraphic position: 116 ± 6 m below Holyoke lava-flow unit.
Geographic location: Massachusetts; Hampden County, 2.5 km south of Mt. Tom, just west of Holyoke; roadcut on Southampton Road, 2.65 km east of junction with Country Road.
Palyniferous horizon: Tan to dark gray siltstone, .3-m-thick fossil plant bed situated within a 4.7+-m-thick sequence of orange to tan coarse sand stone and conglomerate.
Remarks: Plant bed has produced dozens of well-preserved Clathropteris meniscoides Brongniart fronds and Equisetites stems.

Palynoflorule Locality No. 1

Formation: Shuttle Meadow Formation.
Stratigraphic position: 100 ± 6 m below Holyoke lavaflow unit.
Geographic location: Connecticut; New Haven County, North Guilford; stream outcrop on east side of Totoket Mountain, .825 km north of Bluff Head.
Palyniferous horizons: Thin layers of gray micaceous silty shale just below and .5 m above l-m-thick lake bed containing abundant fossil fishes; additional layer 4.5 m above lake bed, consisting of variegated greenish gray to red, poorly bedded silty claystone interbedded within a red siltstone and silty shale sequence.
Remarks: See Cornet et al. (1973), for more detailed description of section.

Palynoflorule Locality No. 5

Formation: Lower Portland Formation.
Stratigraphic position: 257± 6 m above Hampden lava-flow unit.
Geographic location: Connecticut; Middlesex County, just west of Cromwell; neat top of ravine, overlooking Chestnut Brook and Connecticut Route 9.
Palyniferous horizon: 8-cm-thick lens of greenish gray, silty shale, which is part of a micaceous, arkosic sandstone sequence with numerous dinosaur foot-prints.
Remarks: Palyniferous horizon apparently thickens to 38 cm about 100 m upstream in Chestnut Brook.

Palynoflorule Locality No. 11

Formation: Middle Portland Formation.
Stratigraphic position: 1100 ± 6 m above Hampden lava-flow unit, provided no major faults exist.
Geographic location: Massachusetts; Hampden County, Agawam; cliff exposure on south bank of Westfield River, next to Bridge Street bridge.
Palyniferous horizons: 6 beds of dark gray siltstone and shaly siltstone interbedded with brown-red siltstone and sandstone.
Remarks: Cliff sequence measures 16 m thick, with an average interval of 2.3 m between palyniferous horizons.

SYSTEMATIC PALEONTOLOGY

Samples were prepared using standard HF-maceration and ZnCl₂ separation. Glycerin jelly was used as mounting medium. Type specimens are deposited in the palynological collection at the Pennsylvania State University. The assignment of specimens to species previously described in the literature is based on 5 or more specimens. If less than 5 specimens are described, and comparison with an established species indicates affinity, our specimens are compared to that species. (The notation "cf." is used in such cases. However, "cf." also is used in some instances where more specimens are available but doubt as to exact affinity still exists.) A new species is proposed only if 10 or more specimens are described and if the specimens constitute a coherent group distinct from any already in the literature. If less than 10 specimens are described for a new form, it is given a reference number; for example, sp. 1 or Spore A. The median rather than the mean is given for unimodal and relatively non-skewed site ranges. For skewed or very broad size distributions, mean and mode are also given. Abundance of a species at a given locality is indicated by the following terms: rare (less than 1%), scarce (1-3%), common (4-10%), abundant (11-40%), and dominant (41-100%). A question mark indicates that rare, poorly preserved specimens are present, or that at a certain cited locality there is some doubt as to affinity of the specimens concerned. Location of type specimens is given with reference to an "X" scratched on the upper surface of the slide, per Traverse (1958).

The terms intrastructure and intrastructural are used in descriptions for internal features of exines because "infrasculpture" confuses structure (internal) and sculpture (external), and "infrastructure'' has been used in other senses.

 

Genus Anapiculatisporites Potonié & Kremp 1954
Type species: Anapiculatisporites isselburgensis Potonié & Kremp 1954

Anapiculatisporites cf. A. dawsonensis Reiser & Williams 1969
Plate 2, figure 9

Description: See Reiser and Williams, 1969, p. 3.
Remarks: One specimen measures 44 pm in diameter.
Locality: Portland Fm. 11 (rare).

 

Genus Converrucosisporites Potonié & Kremp 1954
Type species: Converrucosisporites triquetrus (Ibrahim 1933) Potonié & Kremp 1954
Basionym: Verrucosisporites triquetrus Ibrahim 1933

Converrucosisporites cameronii (de Jersey 1962) Playford & Dettmann 1965
Plate 2, figures 3-8

Verrucosisporites cameronii de Jersey, 1962, p. 6, P1. 2, fig. 2, 3.
Triletes hungaricus Venkatachala & Góczán, 1964, p. 210, P1. 1, fig. 10-14.
Conbaculatisporites densus Mädler, 1964, p. 175, Pl. 1, fig. 9.
Converrucosisporites cameronii (de Jersey) Playford & Dettmann, 1965, p. 136, Pl. 12, fig. 11-13.
C. luebbenensis Schulz, 1967, P· 561, P1. 2, fig. 15-17; P1. 25, fig. 1.
C. minor Pocock, 1970, p. 47, P1. 8, fig. 4, 5, 7.

Emended description (more than 500 specimens): Isospores radial, trilete. Amb usually subaiangular with broadly rounded apices and sides slightly concave to slightly convex; amb sometimes subspherical. Laesurae extend almost to, but rarely reach, equaterial margin, and are usually bordered by narrow, slightly elevated lips. Kyrtomes prominently to weakly developed, not always present. Laesurae frequently bordered by arcuate folds concave toward proximal pole. Exine variably sculptured with a mixture of rounded or blunt-topped verrucae, large and small bacula, broad and narrow-based coni, rate clavae, and grana (grana comprising less than 50% of sculpture: compare description of Granulatisporites infirmus (Balme) comb. nov.). Sculpture comprehensive, although usually more scattered and reduced proximally. Distal and equatorial sculpture randomly spaced, distance between larger elements frequently greater than their diameter. Bases of sculptural elements usually joined to form a low, imperfect ridge system or incipient reticulum. When elements are large and closely spaced, many are fused into elongate, irregular tugae. Sculpture usually dominated by 1 type: verrucae 0.8-1.8 um in diameter and height, bacula 0.8-1.4 um high, coni 0.5-1.0 um high, and clavae about 1.0 um high. Exine 0.4-0.8 um thick (exclusive of sculpture), single-layered. Equatorial diameter (60 specimens) ranges from 33 um to 51 um (median 42 um), 90% of grains between 36 um and 49 um.

Remarks: Specimens of this study compare very closely with C. cameronii from Australia, as well as with the spore of Clathropteris meniscoides Brongniart figured by Harris (1931, Pl. 18, fig. 3). The largest sculptural elements of the Australian form differ slightly from those of specimens from the Hartford Basin in being taller and conate rather than blunt and verrucate. The list of synonyms contains species that appear to be largely dominated by one type of sculpture: Triletes hungaricus with broadly based coni, Conbaculatisporites densus with closely spaced bacula, Converrucosisporites luebbenensis with verrucae and "truncae," and Converrucosissporites minor with broad verrucae. Numerous specimens from locality 8 closely compare with these species. Rather than divide what appears to be a natural species into 6 morpho-species, all of which would overlap in size and sculptural variation, 2 species are used that encompass the wide variation in sculpture with the least amount of overlap: Granulatisporites infirmus (Balme) comb. nov. and Converrucosisporites cameronii.

Affinity: See discussion under affinity of G. infirmus.

Localities: Portland Fm., 5, 11 (rare to scarce); Shuttle Meadow Fm. 1, 3, 4, 12 (rare to common); upper New Haven Arkose, 8 (abundant to dominant).

 

Genus Convolutispora Hoffmeister, Staplin & Malloy 1955
Type species: Convolutispora florida Hoffmeister, Staplin & Malloy 1955

Convolutispora klukiforma (Nilsson 1958) Schulz 1967
Plate 1, figures 1-3

Description: Isospores radial, trilete. Amb usually subspherical, occasionally subuiangular. Distal and equatorial sculpture composed of large irregular verrucae, basally joined to form a large reticulum; lumina of reticulum 5-6 um in diameter. Verrucae generally aligned in 2 roughly perpendicular directions, one axial, the other equatorial. Proximal sculpture similar but reduced in height and broader, forming a flat contact area flanking the laesurae. Radius of laesurae 27-51% (median 34%) of equatorial diameter. Exine thickness 1.7-5.l um. Equaterial diameter (53 specimens) 44-75 um (median 59 um), 90% of specimens between 48 um and 71 um.

Remarks: Contignisporites dunrobinensis (Couper 1958) Schult 1967 compares somewhat with this species, but axial sculptural lineation weakly expressed, equatorial ribs well developed. C. klukiforma may be conspecific with Striatella jurassica Mädler 1964. Species most prevalent in lake bed at Locality 1.

Affinity: Schizaeaceous fern?

Localities: Shuttle Meadow Fm., 1, 12 (rare).

 

Genus Deltoidospora Miner 1935
Type species: Deltoidospora hallii Miner 1935, designated by Potonié 1956.

Remarks: For generic synonymy, see Pocock, 1970, p. 27.

Deltoidospora hallii Miner 1935
Plate 3, figure 6

Deltoidospora hallii Miner, 1935, p. 618, P1. 24, fig. 7, 8.
D. cascadensis Miner, 1935, p. 618, Pl. 24, fig. 9-12.
Tripartina variabilis var. glabra subvar, gradata Malyavkina, 1949, p. 50, Pl. 7, fig. 10, 12, 14.
Leiotriletes gradatus (Mal.) Bolkhovitina, 1953, p. 19, Pl. 1, fig. 10-12; Pl. 7, fig. 10.
Deltoidospora gradata (Mal.) Pocock, 1970, p. 28, P1. 5, fig. 2.

Description: Isospores, trilete. Amb subtriangular in polar view, with sides nearly straight to moderately convex. Laesurae extend to, sometimes ending short of, equatorial margins. Laesurae may or may not be bordered by narrow raised lips; kyrtomes absent. Exine single layered, psilate, 0.8-1.0 um thick. Size range (14 specimens): 20-39 um in diameter (median 31 um).

Remarks: The site range of our specimens completely overlaps the size ranges of species listed in the synonymy. Miner (1935) separated D. hallii and D. cascadensis on the basis of shape, but our specimens contain gradational types between spores with straight sides and ones with convex sides. The presence or absence of narrow, raised lips is not a significant difference -- lips may be variable in development as they are with the spore types referable to Clathropteris meniscoides Brongniart.
Locality: Portland Fm., 11 (rare).

 

Genus Dictyophyllidites Couper 1958
Type species: Dictyophyllidites harrisii Couper 1958

Dictyophyllidites paramuensteri n. sp.
Plate 3, figures 4, 5, 8

Holotype: Plate 3, fig. 5, size 63 um; Slide BS2, coordinates 23.2 x 116.2, ref 16.1 x 119.6.

Description: Isospores radial, trilete. Amb subtriangular with broadly rounded apices, and sides slightly concave to slightly convex. Laesura extends almost to, rarely reaching, equatorial margin, sometimes bordered by narrow, slightly elevated lips. Proximal side flattened, sometimes appearing slightly concave in lateral compressions; distal side strongly convex. In lateral compressiqns depth of spore equal to or greater than width. Kyrtomes usually weakly developed, sometimes strongly developed in polar compressions, frequently not evident in lateral comptessions. Exine psilate to vaguely punctate, single layered, 0.6-0.8 um thick. Equatorial diameter (252 specimens) ranges from 26 um to 110 um (median 68 um), 90% of grains between 41 um and 101 um.

Remarks: The distribution curve is very broad and basically unimodal. Three slight peaks occur at 60 um, 68 um, and 85 um, but are not distinct enough to warrant the creation of more than one organ species. If this species were derived from one source, the extreme variation in size suggests some sort of environmental stress or adaptive significance. The size range completely overlaps the ranges of Dictyophyllidites harrisii Couper 1958 (36-56 um), D. mortonii (de Jersey) Playford & Dettmann 1965 (28-45 um), Deltoidospora minor (Couper 1958) Pocock 1967 (26-56 um), D. australis (Couper 1958) Pocock 1970 (58-90 um), and the spores (26-47 um) of the fern Dictyophyllum nilssonii (Brongniart) Goeppert (quoted from Harris, 1944, by Couper, 1958). Dictyophyllum muensteri (Goeppert) Nathorst is the only Rhaeto-Liassic fern known to produce spores of the Dictyophyllidites type of a size similar to D. paramuensteri n. sp. The average size of these spores given by Harris (1931) is 65 um. Harris' illustration of one such spore (Harris, 1931, Pl. 14, fig. 3) measures 76 um at the given magnification. These 2 figures agree with the median of 68 um for D. paramuensteri n. sp.; hence, the implied relationship.

Comparison of this species with Deltoidospora Miner 1935 reveals some close similarities in shape. Many of our specimens appear to lack kyrtomes, but cannot be separated by other characteristics from the specimens that possess them. The thin, flexible exine of this species contrasts with the more rigid exine generally found in Deltoidospora (synonym: Cyathidites).

This species is most prevalent in the lake bed at Locality 1.

Affinity: Probably Dictyophyllum muensteri, in part, but the size range could include some spores of other ferns.

Localities: Portland Fm., 11?, 13 (rare); Shuttle Meadow Fm., 1, 12 (rare to scarce); upper New Haven Arkose, 8 (rare).

Dictyophyllidites cymbatus Venkatachala & Góczán 1964
Plate 1, figures 11, 12

Remarks: Specimens from the Hartford Basin agree well with this species, particularly in the strong development of kyrtomes. Fifteen specimens range from 31 um-5l um (median 42 um) in equatorial diameter. Exine 0.5-0.9 um thick.

Localities: Portland Fm., 5, 11 (rare).

Dictyophyllidites harrisii Couper 1958
Plate 1, figures 7, 8

Remarks: Eight specimens from the Hartford Basin range from 37 um to 51 um (median 43 um) in equatorial diameter. This species is present in a mottled gray brown claystone, 5 stratigraphic m above the lake bed at Locality 1, and appears to be separable from D. paramuensteri n. sp at this horizon by its lighter color and more restricted size range. Dictyophyllidites spp. from the lake bed horizon do not show a similar bimodal distribution in size.

Localities: Portland Fm., 5, 11 (rare); Shuttle Meadow Fm., 1, 12 (rare); upper New Haven Arkose, 8?.

 

Genus Dictyotriletes Naumova 1939
Type species: Dictyotriletes bireticulatus (Ibrahim 1932) Potonié & Kremp 1955 (designated by Potonié & Kremp, 1955)
Basionym: Sporonites bireticulatus Ibrahim 1932 in Potonié, Ibrahim, and Loose, 1932.

Dictyotriletes Naumova 1939.
Ischyosporites Balme 1957.
Klukisporites Couper 1958.

Dictyotriletes sp. 1
Plate 1, figures 5, 6

Description: Isospores, trilete. Amb subtriangular in polar view, strongly convex distally. Proximal face psilate; laesurae extend almost to equatorial margins. Distal side sculptured with a large, predominantly complete reticulum, which extends slightly proximal to equatorial margin at apices, generally ending at equatorial margin between apices. Muri of reticulum 2-7 um wide; lumina of reticulum 1.7-5.2 um in overall diameter. Exine doublelayered, 1.7-3.0 um thick, increasing to 4.0 um at apices; endexine thinner than ektexine, but not clearly delimited. Size (2 specimens): 44-48 um in polar-view diameter, one specimen measuring 51 um in depth.

Remarks: This species is similar to Ischyosporites marburgensis de Jersey 1963 (recorded from the Liassic of Australia), which differs in having a slightly thicker exine and more uniform distribution and shape of lumina. Dictyotriletes sp. 1 has also been recovered from our Licking Run locality near Midland, Va., where several distinct species of Dictyotriletes are present (Pl. 1, fig. 4).

Locality: upper New Haven Arkose, 8 (rare).

PLATE 1

1 Convolutispora klukiforma (Nilsson) Schulz. Locality 1, 53 um.
2 C. klukiforma. Locality 1, 56 um.
3 C. klukiforma. Locality 1, 63 um wide.
4 Dictyotriletes sp. Locality on Licking Run, near Midland, Va., 70 um wide.
5 Dictyotriletes sp. 1. Locality 8, 44 um wide.
6 Dictyotriletes sp. 1. Locality 8, 48 um wide.
7 Dictyophyllidites harrisii Couper. Locality 1, 44 um.
8 D. harrisii. Locality 5, 42 um.
9 Murospora sp. 1. Locality 11, 37 um.
10 Murospora sp. 1. Locality 11, 26 um.
11 Dictyophyllidites cymbatus Venkatachala & Góczán 1964. Locality 5, 39 um
12 D. cymbatus. Locality 5, 43 um.
13 Foveosporites agawamensis n. sp (Holotype). Locality 11, 46 um (under oil).
14 F. agawamensis n. sp. Locality 11, 25 um (under oil).
15 F. agawanzensis n. sp. Locality 11, 41 um.
16 Gleicheniidites cf. G. nilssonii Pocock. Locality 5, 41 um.

PLATE 2

1 Granulatisporites infirmus ( Balme) comb. nov. Locality 8; part of spore mass found in close association with Clathropteris meniscoides Brongniart; grain on far left, 42 um.
2 G. infirmus. Locality 8; S.E.M., 41 um.
3 Converrucosisporites cameronii (de Jersey) Playford 8 ( Dettmann. Locality 8, 46 um.
4 C. cameronii. Locality 8, 42 um.
5 C. cameronii. Locality 8; S.E.M., 41 um wide.
6 C. cameronii. Locality 8; S.E.M.; part of spore mass probably derived from Clathropteris meniscoides Brongniart; central grain, 37 um wide.
7 C. cameronii. Locality 8; S.E.M., 45 um.
8 C. cameronii. Locality 8, 56 um.
9 Anapiculatisporites cf. A. dawsonensis Reiser & Williams. Locality 11, 46 um.
10 Perotriletes cf. P. pseudoreticulatus Couper. Locality 11, 54 um.
11 Leptolepidites cf. L. major Couper. Locality 11; focus on sculpture to Fig. 12.
12 Leptolepidites cf. L. major. Locality 11, 54 um.
13 Todisporites rotundundiformis (Malyavkina) Pocock. Locality 11; 54 um.
14 T. rotundiformis. Locality 11; 46 um.
15 T. rotundiformis. Locality 11; 36 um.

Genus Foveosporites Balme 1957
Type species: Foveosporites canalis Balme 1957

Foveosporites agawamensis n. sp.
Plate 1, figures 13-15

Holotype: Plate 1, fig. 13, size 46 um; Slide AGA6-1, coordinates 52.8 x 111.2, ref . 28.5 x 111.6.

Description: Miospores, trilete. Amb subspherical, rarely subtriangular. Laesurae margins slightly thickened, sometimes as narrow conspicuous lips. Radius of laesura 35-46% of overall diameter of spore. Exine 0.6-0.8 um thick, proximally covered with densely to sparsely spaced pits, 0.3-0.4 um in diameter. Pits more closely spaced near laesura, decreasing in number equatorially; distal side generally lacking pits. Size range (11 specimens): 25-52 um (median 41um).

Specific epithet refers to Agawam, Mass.

Locality: Portland Fm., 11 (rare).

 

Genus Gleicheniidites Ross 1949
Type species: Gleicheniidites senonicus Ross 1943

Gleicheniidites cf G. nilssonii Pocock 1970
Plate 1, figure 16

Description: See Pocock (1970, p. 32).

Remarks: The uniqueness of this species necessitates some description: our specimens compare very closely with G. nilssonii, but have a slightly thicker exine (about 2.6 um thick between apices, decreasing to about 2.1 um at apices). A distal triangular area of thickening is delimited by 3 arcuate ridges, intersecting at the apices. Two specimens measure 41 um and 43 um in diameter. The small number of specimens permits only tentative assignment at this time.

Locality: Portland Fm., 5 (rare).

 

Genus Granulatisporites Ibrahim 1933 emend. Potonié & Kremp 1954
Type species: Granulatisporites granulatus Ibrahim 1933

Granulatisporites infirmus (Balme 1957) comb. nov.
Plate 2, figures 1, 2

Concavisporites infirmus Balme, 1957, p. 21, Pl. 2, fig. 32, 33 (Basionym).
Trachysporites asper Nilsson, 1358, p. 39, P1. 2, fig. 3.
Granulatisporites cf. G. asper (Nilsson) Playford & Dettman, 1965, p. 135, Pl. 12, fig. 10.

Emended description (more than 500 specimens): Isospores radial, trilete. Amb usually subtriangular with broadly rounded apices, and sides slightly concave to slightly convex; amb sometimes subspherical. Laesura extends almost to, rarely reaching, equatorial margin, usually bordered by narrow, slightly elevated lips. Kyrtomes prominently to weakly developed, not always present. Laesurae frequently bordered by arcuate folds concave toward proximal pole. Exine sparsely to densely sculptured with grana and small verrucae, mixed with a few bacula and coni, all of which are frequently joined at their bases by a low, imperfect ridge system or incipient reticulum. Sculpture is comprehensive, but usually proximally scattered and more reduced; sculpture ranges from predominantly small grana and verrucae, 0.1-0.8 um in diameter (always more than 50% of sculpture), to a mixture of grana, verrucae, bacula, and coni; occasionally either low coni or bacula dominate the larger sculptural elements. Exine 0.4-0.8 um thick (exclusive of sculpture), single layered. Equatorial diameter (100 specimens) ranges from 22 um to 62 um (median about 40 um), 30% of specimens between 33 um and 43 um. A few abnormal monolete and dilete (chevron) grains observed.

Remarks: Playford and Dettmann (1965) considered Concavisporites infirmus Balme (equatorial diameter 35-46 um, mean 40 um) to be distinct from Trachysporites asper Nilsson (size 38-41 um) and their specimens, since C. infirmus possesses kyrtomes and a finely rugose sculpture. However, Balme's illustrations bear remarkable resemblance to specimens of the present study, most of which have some degree of kyrtome development. The illustrated specimen of T. asper (Nilsson, 1958, Pl. 2, fig. 3) also has raised arcuate folds flanking the laesurae. The finely rugose sculpture in the illustrations of C. infirmus is not obvious (the sculpture appears to consist of discrete grana and verrucae); a basal incipient reticulum could be described as finely rugose, because closely spaced sculptural elements would be united to give an apparent lineation pattern (S.E.M. photomicrograph, Pl. 2, fig. 2). The lack of obvious distinction between C. infirmus, T. asper, and our specimens favors uniting these forms under the earliest name, C. infirmus. This species conforms to the generic requirements of Granulatisporites ibrahim emend. Potonié & Kremp, which has priority over Concavisporites Pflug and Trachysporites Nilsson.

Granulatisporites infirmus grades into Converrucosisporites cameronii (de Jersey) Playford & Dettmann in our samples, but for practical reasons the two forms are separated by gross sculptural differences. Granulatisporites subgranulosus (Couper, 1958) Fisher 1972 differs from G. infirmus by having a much thicker, double-layered exine (l.5-3.0 um thick).

Affinity: Granulatisporites infirmus has been recovered by the first author from sporangia of Clathropteris meniscoides Brongniart at Locality 8. Associated spore masses in sporangial preparations contain C. cameronii. Some dispersed spore preparations from the megafossil plant layers are dominated by C. cameronii, while others are dominated by G. infirmus, although both forms are invariably present in the same preparation. Specimens of Equisetites spp. are the only other megafossils present in the plant bed. Probable roots and rhizomes of C. meniscoides and Equisetites are preserved in situ. Only one species of Clathropteris appears to be present, although it exhibits a wide range in frond site.

Localities: Portland Fm., 5, 11 (rare to scarce); Shuttle Meadow Fm., 1, 3, 4, 12 (rare to common); upper New Haven Arkose, 8 (abundant to dominant).

 

Genus Harrisispora Pocock 1970
Type species: Harrisispora mollis (Bolkhovitina 1956) Pocock 1970
Basionym: Adiantum mollis Bolkhovitina 1956

Remarks: See Pocock (1370, p. 38, 39) for generic description and generic synonymy.

Harrisispora sp. 1
Plate 3, figure 3

Description: Miospores, trilete. Amb subtriangular with slightly convex sides. Radius of laesura about 30% of diameter of spore; laesura occupies for nearly its entire length a narrow zone or groove (1.6-3.0 um wide) of exinal thinning where ektexine and endexine apparently separate. Both endexine and ektexine participate in forming the laesura. Narrow, raised lips present on surface of endexine in groove. Adjacent to the narrow zone of thinning, a band of exine (67 um wide) is inaapunctate and thickened on each side of laesura. Exine double layered, psilate, about 1.4-1.6 um thick (exclusive of proximal area of thickening); ektexine 1.0 um thick, endexine 0.4-0.6 um thick. Size (1 specimen): 80 um in diameter.

Affinity: Possibly ferns related distantly to Lygodium (Pocock, 1970).

Locality: Portland Fm., 11 (rare).

 

Genus Leptolepidites Couper 1953
Type species: Leptolepidites verrucatus Couper 1953

Leptolepidites cf. L. major Couper 1958
Plate 2, figures 11, 12

Remarks: Two specimens, measuring 46 um and 54 um, agree with L. major in size, and in having verrucae frequently in contact. However, the verrucae of our specimens are much smaller (1.0-2.5 um high; 1.0-3.0 um in diameter), agreeing in size and in number around the edge with Leptolepidites bossus (Couper) Schulz. Our specimens appear to be intermediate between L. major and L. bossus.

Locality: Portland Fm., 11 (rare).

 

Genus Murospora Somers 1952
Type species: Murospora kosankei Somers 1952

Murospora sp. 1
Plate 1, figures 9, 10

Description: Miospores, trilete. Amb subcircular to subtriangular in polar view; equatorial outline of cingulum generally parallels that of central body. Laesura extends almost to, sometimes reaching, equatorial margin of central body. Radial apices occasionally protrude beyond general outline of central body, producing a bulge on the cingulum. Laesura usually bordered by narrow, raised lips. Exine double layered, psilate. Ektexine extends over whole surface, including cingulum. Endexine generally restricted to central body, occasionally extending as lobes into, sometimes to outer margin of, cingulum. Exine 0.9-1.0 um thick, ektexine about 0.4 um thick, endexine about 0.6 um thick. Size range (7 specimens): 26-53 um in overall diameter (median 37 um); diameter of central body 22-41 um; width of cingulum 3-7.0 um.

Locality: Portland Fm., 11 (rare).

 

Genus Perotriletes Couper 1953
Type species: Perotriletes granulatus Couper 1953

Perotriletes cf. P. pseudoreticulatus Couper 1953
Plate 2, figure 10

Description: Miospores radial, trilete. Amb subtriangular in polar view. Laesura extends almost to equatorial margin, flanked by narrow, raised lips. Exine (exclusive of perispore) about 0.6 um thick; both proximal and distal faces sculptured with irregular, occasionally anastomosing, ridges, 1-2 um high. Perispore closely fitting, densely covered with small grana, 0.1-0.4 um high; perispore attached only at laesura margins. Overall site (2 specimens) 55-56 um, about 52-53 um in diameter, excluding perispore.

Remarks: The presence of grana on the perispore might be sufficiently different from the type description to warrant the creation of a new species. However, because of the small number of specimens, a tentative assignment is made until further information can be obtained. Our specimens differ significantly from other described species of Perotriletes.

Locality: Portland Fm., 11 (rare).

 

Genus Todisporites Couper 1958
Type species: Todisporites major Couper 1958

Todisporites rotundiformis (Malyavkina 1949) Pocock 1970
Plate 2, figures 13-15

Cyclina pseudolimbata var. rotundiformis Malyavkina, 1949, p. 53, P1. 9, fig. 13.
Leiotriletes rotundiformis (Mal.) Bolkhovitina, 1956, p. 30, P1. 1, fig. 42b.
Todisporites minor Couper, 1958, p. 135, P1. 16, fig. 9, 10.
T. rotundiformis (Mal.) Pocock, 1970, p. 30, P1. 5, fig. 15.

Description: See Couper (1958, p. 135).

Remarks: Our specimens are very similar to T. minor, but have a thinner exine (0.4-0.7 um) and a distribution curve skewed toward smaller size. Measurement of 32 specimens from Locality 11 gives a size range of 29 um to 54 um (median 39 um, mean 40 um, mode 35 um). However, these differences are not significant. Pocock (1970) gives a size range of 38 um to 46 um, Couper (1958) gives 32 um to 50 um (mode 45 um), Malyavkina (1949) gives 30 um to 40 um. Some of our larger specimens are subtriangular in shape, but invariably these have major folds.

Affinity: Couper (1958) compared T. minor with the spores of Todites princeps (Presl) Gothan, which are smaller (20-40 um) and have a mean (32 um) close to our mode.

Localities: Portland Fm., 10, 11 (rare).

 

Genus Verrucosisporites Ibrahim 1933 emend. Potonié & Kremp 1954
Type species: Verrucosisporites verrucosus Ibrahim 1933

Verrucosisporites cheneyi n. sp.
Plate 3, figures 1, 2

Holotype: Pl. 3, fig. 1, size 73 um; Slide BS3, coordinates 40.5 x 122.7, ref. 56.2 x 126.2.

Description: Isospores, radial, trilete. Amb circular to subcircular, proximal face less convex than distal side. Exine densely sculptured with verrucae and a few grana, 0.9-3.4 um high, 1.5-2.8 um wide. Verrucae sometimes in contact with one another, occasionally fused into larger elements. Radius of laesurae variable, 26-78% of equatorial diameter. Exine (exclusive of sculpture) approximately 0.8 um thick, single layered. Equatorial diameter (41 specimens) 58-83 um (median 70 um), 90% of grains between 59 um and 79 um.

Remarks: This species compares closely with the Permian Verrucosisporites trisectus Balme & Hennelly 1956b, but differs somewhat in size range (V. trisecatus: 65-135 um), and in the degree of suture development (laesurae of V. trisecatus frequently extend onto distal surface of spore). The sculpture of both species is very similar.

Species most prevalent in lake bed at Locality 1.

Species named after Jane Cheney, director emeritus of the Children's Museum of West Hartford, Conn., in recognition of her efforts to preserve the natural history of the Connecticut Valley.

Affinity: Osmundaceous fern?

Localities: Portland Fm., 6, 11, 13 (rare); Shuttle Meadow Fm., 1 (rare); upper New Haven Arkose, 8 (rare).

 

Spore A
Plate 3, figure 7

Description: Miospore, trilete. Amb triangular in polar view, apices rounded. Radius of laesura about 30% of diameter of spore. Laesura open, bordered by a kyrtome consisting of narrow bands of exinal thickening. Distai side extended, equatorially strongly concave, forming triradiate fold centered at distal pole. Exine double layered; endexine 0.7 um thick; ektexine 1.0 um thick, loosely attached along triradiate fold. Size: 98 um in diameter.

Locality: Portland Fm., 11 (rare).

 

Genus Pilasporites Balme & Hennelly 1956a
Type species: Pilasporites calculus Balme & Hennelly 1956a

Pilasporites allenii Batten 1968
Plate 4, figure 11

Description: See Batten (1868, p. 638).

Remarks: Our specimens agree closely in all respects with P. allenii Batten from the Lower Cretaceous of England, except in exine thickness, which is not a significant difference for the creation of a new species. Measurement of 72 specimens from Locality 8 gives a size range of 30 um to 54 um (median 39 um, mean 39 um), indicating a slightly larger average size than that of the type description (mean 36.7 um; Batten, 1968). Exine of our specimens is 0.5-0.8 um thick as compared with 1.25-1.75 um given by Batten. Slightly irregular distribution in the size-range curve of our specimens suggests more than one source plant, as is also indicated by megafossils.

Affinity: Equisetites cf. E. sarranii Zeiller (abundant in layers containing P. allenii), as well as possibly two other species of Equisetites, present at Locality 8.

Localities: Portland Fm., 5, 2 1 (rare); Shuttle Meadow Fm., 1 (rare in lake bed); upper New Haven Arkose, 8 (rare to scarce).

 

Genus Araucariacites Cookson 1947
Type species: Araucariacites australis Cookson 1947

Remarks: Cookson (1947), following the suggestions of Erdtman (1947), created the "sporotype" names Granulonapites (± = form-generic name) and Araucariacites (± = organ-generic name), as alternative names to be combined with the epithet, australis. The 1972 I.C.B.N. restriction on the use of alternative names is retroactive only to January 1, 1953. Consequently, we consider subsequent attempts to validate one of the two generic names (Couper, 1953, Nilsson, 1958) unnecessary, since Cookson's monotypic species was validly published. Her sporotypes and sporomorphs are handled normally in all respects as genera and species, respectively. Our choice of the generic name, Araucariacites, is based on the fact that Cookson does not accept the name Granulonapites in her publication: wherever the generic concept is given a single name, that name is always Araucariacites.

Araucariacites punctatus (Nilsson 1958) comb. nov.
Plate 6, figures 14, 15

Granulonapites punctatus Nilsson, 1958, p. 70, Pl. 5, fig. 22.

Description: Pollen grains inaperturate, spherical to oval, frequently folded. Exine 0.5-0.7 I~m thick, densely sculptured with small grana, 0.2 um or less in diameter. Size range (50 specimens): 28-63 um (median 44 um) in maximum width or diameter, 90% of specimens between 34.0 um and 56.8 um.

Remarks: This species agrees in all morphological respects with Araucariacites australis Cookson, but has a smaller mean and smaller site distribution than generally recognized for A. australis. Couper (1953) reported grains of similar size under the name A. australis from Jurassic-lower Oligocene strata of New Zealand. Nilsson (1318) described one specimen (upon which A. punctatus is based) from the middle Keuper of Scania.

This species is generally much more common than A. australis in our samples.

Localities: Portland Fm., 5, 6, 7, 9, 10, 11, 13 (rare to scarce); Shuttle Meadow Fm., 1, 12 (rare).

 

Araucariacites australis Cookson 1947
Plate 6, figure 13

Remarks: This species is distinguishable from A. punctatus (Nilsson) comb. nov. by its larger size and usually darker color. Range in size for 26 specimens: 54-94 um (median 73 um). Our specimens compare well in shape and in manner of folding to grains of Brachyphyllum mamillare Brongniart as illustrated by Couper (1958, Pl. 27, fig. 1, 2). Species is more frequently encountered in the Portland Fm. than in older strata. Some specimens assigned to this species may be unsplit examples of A. fissus Reiser & Williams.

Localities: Portland Fm., 5, 11 (rare); Shuttle Meadow Fm., 1 (rare).

 

Araucariacites fissus Reiser & Williams 1969
Plate 7, figures 6, 7

Description: See Reiser & Williams (1969, p. 17).

Remarks: The size distribution (17 specimens) indicates a larger average size than that given by Reiser & Williams (1969), being 58-110 um (median 85 um) rather than 34-95 um (?mean 57 um) for the Australian forms. The indicated Early Jurassic age for A. fissus Reiser & Williams agrees well with  the proposed age for the Portland Fm. This species becomes more frequent in younger strata. The largest forms are more common at Locality 5.

Discussion of relationship of A. fissus to Triangulopsis: Our specimens (esp. P1. 7, fig. 7) from Locality 11 compare well in overall shape, manner of splitting, and size range to Triangulopsis discoidalis Döring 1961, recorded from the Upper Jurassic of Germany and western Canada. However, T. discoidalis apparently has a much thicker, double-layered exine, separable into an outer envelope and an internal body (Pocock, 1970, p. 74). Döring considered T. discoidalis to be microplanktonic, while Pocock's study of a large population of this species indicated morphological affinity with vascular plants. Döring considered Zonalapollenites to be synonymous with Triangulopsis, suggesting a similar basic structure. It is possible that A. fissus is related to Triangulopsis discoidalis, lacking only the development of a distinct endexine.

Localities: Portland Fm., 5, 10, and 11 (rare).

 

Genus Perinopollenites Couper 1958
Type species: Perinopollenites elatoides Couper 1958

Perinopollenites elatoides Couper 1958
Plate 4, figures 12, 13

Description: See Couper (1958, p. 152).

Remarks: One specimen from~locality 11 clearly shows a pore (Pl. 4, fig. 12). Other specimens possess a highly folded "perine," which may simulate a crude reticulum (Pl. 4, fig. 13). Specimens from Locality 5 generally have a slightly smaller body, giving the appearance of a relatively larger "perine." Six specimens range in maximum diameter from 34 um to 52 um; diameter of central body 28 um-43 um.

Localities: Portland Fm., 5, 11 (rare).

 

Genus Callialasporites Sukh Dev 1961
Type species: Callialasporites trilobatus (Balme 1957) Sukh Dev 1961 (designated by Sukh Dev, 1961)
Basionym: Zonalapollenites trilobatus Balme 1957

Zonalapollenites (in part) Pflug in Thomson and Pflug, 1953, p. 66, 67.
Callialasporites Sukh Dev, 1961.
Applanopsis Döring, 1961.
Triangulopsis (in part) Doring, 1961.
Pflugipollenites Pocock, 1962.
Applanopsipollenites Levet-Carette, 1964.

Description: See Sukh Dev, 1961, p. 48; Balme, 1957, p. 32.

Remarks: Sukh Dev (1961) and Pocock (1970) discuss the synonymy of Zonalapollenites and Tsugaepollenites, and differences between these two genera and species now placed in Callialasporites.

Callialasporites cf. C. dampieri (Balme 1957) Sukh Dev 1961
Plate 4, figure 10

Description: See Balme (1957, p. 32).

Remarks: Three specimens range in overall diameter from 60 um to 77 um; body 56 um-59 um in diameter. Sculpture of saccus is finely granulate. Endexine of body is about 1.3 um thick. A slightly darkened area is present on the central part of the body. One specimen has saccus folded back on body, resembling a similar condition found in C. segmentatus (Balme) comb. nov.

Affinity: Gamerro (1965) found grains of C. dampieri and C. trilobatus (Balme) Sukh Dev in male cones in organic connection with leaves of the gymnosperm Apterocladus lanceolatus Archangelsky.

Locality: Portland Fm., 11 (rare).

 

Callialasporites segmentatus (Balme 1957) comb. nov.
Basionym: Zonalapollenites segmentatus Balme 1957, p. 33, Pl. 9, fig. 93, 94.

Remarks: A formal transfer is made of this species here, although no specimens definitely referable to it were found.

 

Callialasporites trilobatus (Balme 1357) Sukh Dev 1961
Plate 4, figure 4

Description: See Balme (1957, p. 33).

Remarks: This species is larger than our specimens of Callialasporites dampieri, 7 specimens measuring 78 um to 104 um in overall diameter; diameter of body 46 um-84 um. Exine of body is 0.8-1.1 um thick. Saccus is densely covered with small grana, 0.2-0.8 um in diameter. The shape of the body ranges from oval to subtriangular, with 3 lobes well developed on forms with subtriangular bodies. Forms with oval bodies tend to possess sacci without indentations. Sukh Dev (1961) described a new species, Callialasporites monoalasporus, that closely resembles our forms with oval bodies. More specimens are needed to determine if a significant distinction exists between our forms resembling C. monoalasporus Sukh Dev, and C. trilobatus. In addition, C. monoalasporus may be conspecific with C. turbatus (Balme) Schulz 1967.

Affnity: Gamerro (1965) illustrates grains of C. trilobatus and C. dampieri, as well as forms resembling C. monoalasporus, which he found associated with Apterocladus lanceolatus Archangelsky. Reiser & Williams (1963) found in their study forms of Callialasporites gradational between different species of this genus, suggesting that many of them are derived from one source plant.

Locality: Portland Fm., 11 (rare).

 

Genus Alisporites Daugherty 1941 emend. Nilsson 1958
Type species: Alisporites opii Daugherty 1941

Alisporites thomasii (Couper 1958) Nilsson 1958
Plate 4, figure 5-7

Pteruchipollenites thomasii Couper, 1958, p. 150, P1. 26, fig. 10, 11.
Alisporites thomasii (Couper) Nilsson, 1958, p. 83, P1. 8, fig. 1.

Description: See Couper (1958, p. 150).

Remarks: Our specimens compare closely with A. thomasii in overall size and shape, as well as exine structure and sculpture. Twenty-one specimens range from 48 um to 77 um in overall breadth (median 69 um); breadth of body 20 um-46 um (median 36 um); length of saccus 36 um-57 um (median 40 um). Some specimens, not included in the above measurements, have bodies compressed more or less obliquely with pendantly attached sacci, producing forms suggestive of pollen of extant Pinus. More study is needed to determine whether these unique forms should be included in A. thomasii.

Localities: Portland Fm., 5, 11 (rate).

 

Genus Pityopollenites Reissinger 1950 emend. Jansonius 1962
Type species: Pityopollenites pallidus Reissinger 1950

Vitreisporites Leschik 1956 (imprint date, 1955).
Caytonipollenites Couper 1958.
Vitreisporites Leschik emend. Jansonius 1962.

Remarks: Pityopollenites was validly published by Reissinger in 1950, and was monotypic at the time of publication. Vitreisporites, as originally described by Leschik in 1956, required a faint laesura and a size of the central body under 20 um. Jansonius (1962) removed these characteristics from the generic description, considering them either not convincingly demonstrated or too restrictive. For further discussion, see Dunay (1972).

Pityopollenites pallidus Reissinger 1950 emend. Nilsson 1958
Plate 4, figures 2, 3

Pityopollenites pallidus Reissinger, 1950, p. 105), P1. 15, fig. 1-5.
Vitreisporites signatus Leschik, 1956 (imprint date, 1955), p. 53, P1. 8, fig. 10.
Caytonipollenites pallidus (Reissinger) Nilsson, 1958, p. 78, P1. 7, fig. 12-14.

Description: See Nilsson (1958, p. 54).

Remarks: Twenty-one specimens of this study range fiom 22 um to 33 um in overall breadth (median 27 um); breadth of body 7 um-15 um (median 27 um); length of saccus 14 um-22 um (median 17 um). Specimens from Locality 5 are generally smaller than those from Locality 11.

Locatities: Portland Fm., 5, 11 (rare).

 

Genus Platysaccus Naumova 1939 emend. Potonié & Klaus 1954
Type species: Platysaccus papilionensis Potonié & Klaus 1954

Remarks: Platysaccus was validly published by Naumova in 1939 (p. 355, fig. 1), although no type species was designated, which is not required by the I.C.B.N. before 1358. Potonié and Klaus (1954) designated their new species, P. papilionensis, as type, and emended the genus.

Platysaccus cf. P. lopsiensis (Malyavkina 1961) Pocock 1970
Plate 4, figure 1

Podocarpus lopsiensis Malyavkina in Samoilovich et al., 1961, p. 130, Pl. 35, fig. 9a,b.
Platysaccsus lopsiensis (Mal.) Pocock, 1970, p. 85, Pl. 18, fig. 6, 7.

Description: See Pocock (1370, p. 85).

Remarks: Two specimens compare closely with P. lopsiensis, measuring 56 um to 59 um in overall breadth (grains not completely expanded); breadth of body 26 um-27 um ; length of saccus 26 um-46 um.

Locality: Portland Fm., 11 (rare).

 

Genus Podocarpidites Cookson 1947
Type species: Podocarpidites elliptica Cookson 1947 (designated by Potonie', 1958)

Remarks: This generic name was validly published by Cookson (1947) under circumstances similar to those described above under Araucariacites Cookson.

Podocarpidites sp. 1
Plate 4, figure 14

Description: Pollen grains, bisaccate. Body of grain generally longer than broad; sacci strongly distally pendant, rarely expanded, usually highly folded. Distal surface traversed by an elongate sulcus, about 20 um long, flanked by basal attachment of sacci. When expanded, saccus measures about 36 um in length, 50 um in breadth. Proximal surface of body covered by a closely adhering cappa, 1.4-2.6 um thick, tightly folded to form a verrucose and rugose surface. Exine of body about 0.9 um thick. Sacci possess fine reticulum with lumina 0.2-0.3 um in diameter. Size of body (5 specimens): 40-46 um long; 31-34 um broad. Sacci generally about 30 um in diameter (folded). Overall breadth approximately 50-60 um, but highly dependent on shape of sacci.

Remarks: Bisaccates are generally rare in the Shuttle Meadow Fm. However, they increase slightly in abundance in the lake bed and underclay at Locality 1. A similar florule from Licking Run near Midland, Va. (see Discussion), contains as much as 15% bisaccates in certain lacustrine horizons. Most bisaccates from floras dominated by Corollina meyeriana compare best with Podocarpidites and Pityosporites, although examples of Alisporites have been found. Generally poor preservation of most of the Shuttle Meadow bisaccates prevents description of several other types present.

Localities: Shuttle Meadow Fm., 1, 12 (rare); upper New Haven Arkose, 8?

 

Circulina-Corollina-Classopollis

Nomenclatural problem: Circulina and Corollina were validly published as generic names by Malyavkina (1949), even though her generic and specific descriptions have been regarded as vague and inadequate for validation (Pocock and Jansonius, 1961; Reyre, 1969; Traverse, Ames and Spackman [CCFSP, 1974, in press: 38-103, 38-128]). Classopollis is generally regarded as the acceptable generic name, but was originally described as tricolpate by Pflug (1953). Subsequent emendation of Classopollis by Pocock and Jansonius (1961) and Couper (1958) largely corrected the description of this pollen type, but Chaloner (1962) and Pettitt and Chaloner (1964) provided the most accurate description, clarifying the structure of the exine with electron micrographs of well-preserved grains. Klaus (1960) emended the description of Circulina and Corollina, providing Hilfstypus -- better called neotype, which is admissible under 1372 I.C.B.N., Guide for Determination of Types, p. 76, for establishing taxonomic validity. However, Klaus chose to distinguish Circulina from Corollina, making Classopollis a junior synonym of Corollina.

S. Samoilovich (Institute of Petroleum, Leningrad, USSR; pers. comm. to A. Traverse, 1973) has indicated that Malyavkina's type material was not preserved. She provided photographs (Pl. 4, fig. 9; Pl. 5, fig. 10) of "neotypes" (chosen by Zauer, supplied to Klaus, and chosen by him as Hilfstypus) for species of Circulina and Corollina, derived fiom the same Lower Jurassic stratigraphic horizon as studied by Malyavkina (from the same locality, a borehole 80 km to the west of the settlement of Sagiz). Even though the assignment of these "neotypes" by Zauer is subjective, it is perhaps the only way to obtain stability of nomenclature and to avoid personal preference for the name Classopollis.

It is interesting to note that the "neotype" of Corollina compacta Malyavkina (Pl. 5, fig. 10) compares well with Classopollis in exinal structure, even though a well-developed distal pseudopore is not present, and equatorial striations are questionably present. Thus Klaus was apparently correct in making Classopollis synonymous with Corollina rather than with Circulina, It is further significant that the "neotype" of Circulina simplex Mal. closely resembles Malyavkina's illustrations, lacks a well-developed ring tenuitas (rimula) and distal pseudopore, and resembles specimens of Spheripollenites Couper and endoexinal bodies of Classopollis more than it does Circulina meyeriana (Mal.) Klaus, raising the question of the correctness of Klaus's emendation of Circulina.

Reyre (1969) considers Circulina Mal. emend. Klaus as "an exceptional case within the genus Classopollis, corresponding to the coincidence of the limiting cases of the two characters, equatorial thickening and ornamentation of the intrastructure." He describes two species, Classopollis quezeli and C. kieseri, with a typical Classopollis intrastructure, but without equatorial striations or with only vaguely defined striations (pseudostriations). These two species closely resemble grains that have been erroneously assigned to Corollina meyeriana (Klaus) Venkatachala & Goçzán (Schulz, 1967, P1. 22, fig. 6) or Circulina meyeriana Klaus (Geiger and Hopping, 1968, P1. 4, fig. 32). In fact this confusion suggests that there is really no clear generic distinction between grains with a massive intrastructure and no equatorial thickening or striations, and grains with a structured exine, equatorial thickening, and striations.

Consequently the only valid genetic characteristics are those that Circulina emend. Klaus and Classopollis have in common: frequent occurrence as tetrads, spherical shape, size range (18-60 um), proximal trilete mark, distal pseudopore, and subequatorial furrow or rimula. Since the intrastructure of the exine ranges from massive through various types (Reyre, 1969), equatorial striations vary in number and completeness, particularly in some species, for example, Classopollis torosus (Reissinger) Balme and C. kieseri Reyre, and because the amount of equatorial thickening is variable, even in a single species, these characteristics are best reserved for specific distinction.

It is therefore clear that Circulina (as emended by Klaus) and Corollina should be combined into a single genus, with Classopollis as a junior synonym. Circulina Malyavkina may not be identical with Circulina Mal. emend. Klaus (the status of which is also confused). Corollina was monotypic when published, whereas Circulina was not. Thus, Corollina does not present problems of generic typification and is therefore chosen to embody all of the common generic characters.

PLATE 3

1 Verrucosisporites cheneyi n. sp. (Holotype). Locality 1, 73 um.
2 V. cheneyi n. sp. Locality 1, 85 um wide.
3 Harrisispora sp. 1. Locality 11, 80 um.
4 Dictyophyllidites paramuensteri n. sp. Locality 1, 65 um wide.
5 D. paramuensteri n. sp. (Holotype). Locality 1, 63 um.
6 Deltoidospora hallii Miner. Locality 11, 27 um.
7 Spore A. Locality 11, 98 um.
8 Dicryophyllidites paramuensteri n. sp. Locality 1, 53 um.

PLATE 4

1 Platysaccus cf. P. lopsiensis (Malyavkina) Pocock. Locality 11, 58 um.
2 Pityopollenites pallidus Reissinger. Locality 5, 22 um.
3 P. pallidus. Locality 5, 26 um.
4 Callialasporites trilobatus ( Balme) Sukh Dev. Locality 11, 90 um.
5 Alisporites thomasii (Couper) Nilsson. Locality 5, 58 um.
6 A. thomasii. Locality 11, 63 um.
7 A. thomasii. Locality 11, 73 um.
8 Circulina simplex Malyavkina. Locality I, 25 um.
9 C. simplex Malyavkina (Neotype). Locality indicated under description, about 22 um.
10 Callialasporites cf. C. dampieri ( Balme) Sukh Dev. Locality 11, 75 um.
11 Pilasporites allenii Batten. Locality 8, 44 um.
12 Perinopollenites elatoides Couper. Locality 11, 41 um.
13 P. elatoides. Locality 11, 44 um.
14 Podocarpidites sp. 1. Locality 1, 58 um.

 

Genus Corollina Malyavkina, 1949 emend.

Corollina Malyavkina 1949.
Circulina Malyavkina (in part), 1949.
Classopollis Pflug 1953.
Classopollis Pflug emend. Couper 1958.
Corollina Mal. emend. Klaus 1960.
Circulina Mel. emend. Klaus 1960.
Classopollis Pflug emend. Pocock & Jansonius 1962.
Monilapollis Chang 1963.
Pagiophyllumpollenites Chang 1963.
Classopollis Pflug emend. Reyre 1969. [Also the species listed below referred to "Pollenites" by Thiergart and by Reissinger.]

Generic type: Corollina compacta Malyavkina, 1949, p. 124, Pl. 46, fig. 10. (Liassic).

Holotype: Malyavkina, 1949, P1. 46, fig. 10, 11.

Neotype: Plate 5, fig. 10. Designated by Zauer, photograph supplied by Samoilovich, 1973.

Stratigraphic position and locality of neotype: Borehole Kozhegali K36, 466.8 m-471.9 m, Lower Jurassic, 80 km west of Sagiz near Caspian Sea.

Species assigned to genus: Circulina funifera Malyavkina, 1949, p. 123, P1. 46, fig. 6; Bennettiteae-Pollenites reclusus Thiergart, 1949, p. 11, P1. 2, fig. 14, 15, P1. 3, fig. 6; Pollenites torosus Reissinger, 1950, p. 115, P1. 14, fig. 20.

Emended generic description: Pollen grains distally pseudoporate, proximally trilete, spherical to ovoid, or compressed, acorn shaped; occur as tetrads or isolated grains; exine two layered, with distinct endexine and ektexine. Endexine comprises a spherical, internally separate body, which frequently may be poorly developed and difficult to distinguish, or well developed, sometimes occurring as separate bodies from rupnued grains. Ektexine (modified from Reyre, 1969) composition variable on different parts of the grain; composed of inner structured layer, comprising inuastructure, and outer tegillum, which is continuous over entire grain and covered with outer sculpture uniformly distributed over whole surface. Intrastructure massive, alveolate, punctate, vermiculate or pseudovermiculate, reticulate or pseudoreticulate, but can be heterogeneously organized: reduced, or thickened, in parts of the grain; reduced at distal pole (pseudopore) or only along circular line surrounding it, reduced along a subequatorial furrow (ring tenuitas or rimula) on distal side of equator, and sometimes reduced at proximal pole (triangular area). Intrastructure generally thidcened in equatorial zone on proximal side of furrow or rimula, but never thinner than ektexine proximai to equatorial zone or belt; intrastructurai elements within this equatorial zone may or may not be organized into more or less continuous circumequatorial striations; they are absent if intrastructure of this zone is massive.

Remarks: Endexinal body may or may not possess a poorly developed trilete mark; it infrequently possesses a distal area of thinning or tenuitas. The neotype of Circulina simplex Malyavkina (our P1. 4, fig. 9) and illustrations by Malyavkina (Pl. 46, fig. 7-3) strongly resemble separated endexinal bodies of Corollina, and therefore do not possess sufficient characteristics to place C. simplex in Corollina. Circulina funifera Mal. (Pl. 46, fig. 6), on the other hand, appears to possess a subequatorial furrow (border sharply differentiated from the body, narrow, double), and exinal intrastructure (border covered with fine, radially directed, straight lines), which possibly place it in Corollina.

 

Corollina torosus (Reissinger 1950) Klaus 1960 emend.
Plate 5, figures 2-3, 14

Pollenites torosus Reissinger, 1950, p. 115, Pl. 14, fig. 20.
Classopollis classoides Pflug, 1953, Fig. 4, J-M, P1. 16, fig. 20-25, 229-37; emend. Pocock & Jansonius, 1961, p. 443, P1. 1, fig. 1-3.
Classopollis cf. C. torosus (Reissinger) Balme, 1957, p. 37, Pl. 11, fig. 114-119.
C. torosus (Reissinger) Couper, 1958, p. 156, Pl. 28, fig. 2-7; Nilsson, 1958, p. 74, Pl. 7, fig. 68.
C. torosus (Reissinger) Balme; Chaloner, 1962, p. 13, fig. 2, Pl. 11, fig. 1, 2; emend. Burger, 1965, p. 65, P1. 1, fig. 1, 2.
Monilapollis hsui Chang, 1963, p. 435, 439, P1. 1, fig. la-lc, 2a-2c.
"Classopollis torosus" Pettitt & Chaloner, 1964, P1. 1, fig. 1-5.

Emended description: Isolated pollen grains or occurring as atrads; spherical to ovoid, or acorn-shaped; diameter in equatorial view (100 grains): 18-41 um (median 32 um), 90% of grains between 24 and 37 um (Couper, 1958, notes range 24-46 um, mode 32 um). Diameter in polar view 24-37 um (diameter of subequatorial furrow 83-88% of overall diameter). Distal pseudopore variable in size, even for grains of same size: 4.3-8.5 um in diameter, frequently distorted and widened in equatorial view. Proximal triangular area of thinning, which sometimes contains trilete mark, 6.8-13.6 um high. Exine two layered; ektexine divisible into outer tegillum, continuous over whole surface of grain, and inner structured layer, which is thickened in equatorial region to form a band or belt. Endexine variably distinct to indistinct, spherical, frequently scabrate, occasionally with a small proximal trilete mark. Structure of equatorial band ranges from pseudoreticulate, to vaguely striate with aligned intrastructural columellae (pseudostriations), to distinctly striate, with columellae fused to form more or less parallel bands, the number of striations frequently varying from one part of band to another. Sometimes combinations of grains with all degrees of striation development occur in same tetrad. When striations are well developed, maximum number per grain ranges from 6 to 10. Width of equatorial band, which frequently ranges from 5 um to 13 um at its maximum, usually decreases in one area to 4-10 um, and striations decrease in number to 4 or 5 through anastomosis or disintegration of more proximal striations into discrete intrastructural elements. Exine thickness varies with grain size, and presumably also with preservation; it is thickest in equatorial band: 1.3-2.4 um (Couper, 1958, records 3.0 um), decreasing gradually toward proximal pole: for example, 2.l um down to 0.9 um; thickness on distal side of equaterial furrow (range 0.7-1.7um) generally slightly less than that proximal to equatorial band. Intrastructure of ektexine mostly pseudoreticulate, with positive elements largest on proximal side of equatorial furrow, particularly if equatorial band is pseudoreticulate; pseudoreticulum on distal side of grain usually finer in pattern, occasionally becoming punctate. Sculpture of tegillum variable (perhaps owing to preservation); light microscope indicates roughened surface; S.E.M. indicates microscabrate sculpture, mixed with microverrucae and microconi (Pl. 5, fig. 14; see also Pettitt and Chaloner, 1964, p. 614); sculpture distinctly less well developed than in species figured by Reyre (1969), perhaps less well developed than in forms described under Classopollis torosus (Reissinger) Couper emend. Burger 1965.

Remarks: The emended description of Classopollis classoides Pflug by Pocock and Jansonius (1961) is not adequate and conflicts with our present knowledge of the exine structure of this genus. We find no distinction between C. classoides and C. torosus, these species agreeing in exinal structure and variation in striation development (Pocock and Jansonius, 1961, Pl. 1, fig. 1-9). The size ranges overlap widely, but the mean equatorial width for C. classoides (29 um) is somewhat smaller than that of C. torosus (32 um). However, Harris (1957) noted a still smaller mean in his samples (25 um) for grains placed by Pettitt and Chaloner (1964) in C. torosus. These differences may result in part from preservational states and preparation techniques. The mean diameter for C. torosus from Locality 11 is 32 um, while it is 25 um from Locality 5. Table 1 gives data for relative abundance of C. torosus that suggest the existence of two separate "Circumpolles" populations, intermixing at Locality 5. The morphology of these two populations does not permit their distinction in a mixed sample, as the ranges of variation widely overlap. Therefore, only one form-species is described, although two different source plants may be indicated.

Affinity: Hirmerella muensteri (Schenk) Jung 1968, possibly Pagiophyllum connivens Kendall 1948.

Localities: Portland Fm. 5, 6, 7, 9, 10, 11 (dominant); Shuttle Meadow Fm. 1, 3, 4, 12 (rare to scarce); upper New Haven Arkose, 8 (scarce).

 

Corollina itunensis (Pocock 1962) comb. nov.
Plate 5, figure 1

Classopollis itunensis Pocock, 1962, p. 71, Pl. 11, fig. 176, 177; P1. 12, fig. 178 (Basionym).

Description: See Pocock (1970, p. 104).

Table 1. Approximate percentages of major Corollina species in Hartford Basin (Based on Corollina counts only. Most of palynoflorules counted were at least 90% Corollina.)

Localities arranged in stratigraphic order, youngest at right: N.H.A. = New Haven Arkose; S.M.F. = Shuttle Meadow Formation; P.F. = Portland Formation; + = present, but less than 1%.

PLATE 5

1 Corollina itunensis (Pocock) comb. nov. Locality 11, 53 um.
2 Corollina torosus (Reissinger) Klaus, emend. Locality 11, 34 um-36 um.
3 C. torosus (Reissinger) Klaus, emend. Locality 11, 32 um-38 um.
4 C. torosus (Reissinger> Klaus, emend. Locality 11, 31um-34 um.
5 C. torosus (Reissinger) Klaus, emend. Locality 5, 28 um-30 um.
6 C. torosus (Reissinger) Klaus, emend. Locality 11, 22 um-25 um.
7 C. torosus (Reissinger) Klaus, emend. Locality 11, 30 um.
8 C. torosus (Reissinger) Klaus, emend. Locality 11, 37 um.
9 C. torosus (Reissinger) Klaus, emend. Locality 11, endexinal body, 34 um (under oil).
10 Corollina compacta Malyavkina (Neotype). Locality indicated under description, about 33 um.
11 Corollina murphyi n. sp, (Holotype). Locality 5, 30 um.
12 C. murphyi n. sp. Locality 8, 34 um.
13 C. murphyi n. sp. Locality 8, 30 um.
14 Corollina torosus (Reissinger) Klaus, emend. Locality 11; S.E.M., 28 um-33 um.
15 Corollina murphyi n. sp. Locality 8, 32 um.
16 C. murphyi n. sp. Locality 11; polar view with endexinal body, 42 um.

PLATE 6

1 Brachyphyllum scotii Kendall. Locality on Licking Run, near Midland, Va.; cuticle of leaf showing stomata; field about 250 um across.
2 B. scotii Kendall. Locality on Licking Run, near Midland, Va.; cuticle of leaf; field about 850 um across.
3 Corollina meyeriana (Klaus) Venkatachala & Goçzán. Locality 8, 26 um.
4 C. meyeriana. Locality 8, 29 um.
5· C. meyeriana. Locality 8; S.E.M., 23 um.
6 C. meyeriana. Locality on Licking Run, near Midland, Va.; each grain about 54 um.
7 C. meyeriana. Locality 1, 26 um.
8 C. meyeriana. Locality 1, 24 um.
9 C. meyeriana. Locality 1, S.E.M., 19 um.
10 Corollina simplex (Danzé -Corsin & Laveine) comb. nov. Locality 11, 24 um.
11 Corollinoid? pollen. Locality 11, 42 um.
12 Corollinoid? pollen. Locality 11, 42 um.
13 Araucariacites australis Cookson. Locality 11, 71 um.
14 Araucariacites punctatus (Nilsson) comb. nov. Locality 11, 53 um.
15 A. punctatus (Nilsson) comb. nov. Locality 5, 48 um.

 

DISCUSSION

Stratigraphic Correlation

Text-figure 5 summarites the stratigraphy of the Hartford Basin as correlated, by this study and other information, with the upper part of the Newark Basin sediments.

Palynofloras dominated by Corollina (exceeding 70% of assemblage) have been reported from the Rhaeto-Liassic and Upper Jurassic (Kendall, 1943; Harris, 1957; Couper, 1958; Lantz, 1958a,b; Pocock and Jansonius, 1961; Chaloner, 1962; Venkatachala and Goçzán, 1964; Wall, 1965; Burger, 1965; Reyre, 1969; Volkheimer, 1971). Floras composed of more than 90% Corollina meyeriana have thus far been reported only from the basal Liassic of Larachbeg, Morvern, Scotland (Kendall, 1943). However, floras composed of a complex of Corollina species, totaling more than 90%, have been reported from the Rhaetian Kössen facies, Hungary (Venkatachala and Goçzán, 1964). This complex contains both equaterially striate and non-striate forms, C. classoides and C. meyeriana. Palynofloras composed of 70% or more Corollina torosus are common in the Liassic (Harris, 1957; Couper, 1958; Wall, 1965; Volkheimer, 1971), but have also been recorded in undifferentiated Rhaeto-Liassic strata (Chaloner, 1962; Jung, 15)68). In general, non-striate to pseudostriate species are most common in the Rhaetian and early Liassic, while equatorially striate species predominate in the Liassic (Geiger and Hopping, 1968; Reyre, 1963).

The palynofloras of the Hartford Basin show an upward change in Corollina from more than 90% Corollina meyeriana in the Shuttle Meadow Formation to more than 90% Corollina torosus in the Portland Formation. The age of this shift would lie somewhere between the oldest reported record of a flora dominated by Corollina torosus and the youngest record of a flora dominated by Corollina meyeriana. Although there is admittedly limited evidence, probably the shift occurred between the limits of Rhaetian and basal Liassic. Paleomagnetic data and isotopic dates (171-196 m.y.) for the Hartford Basin lava-flow units agree with a Rhaeto-Liassic age for this shift (Reesman et al., 1973; Reeve and Helsley, 1372).

TEXT-FIGURE 5. Suggested time-stratigraphic correlation of Hardord Basin and upper sediments of the Newark Basin. A = Callialasporites trilobatus (Balme) Sukh Dev; D = Callialasporites cf. dampieri; H = Hirmerella muensteri (Schenk) Jung; K = Convolutispora klukiforma (Nilsson) Schulz; M = flora dominated by Corollina meyeriana (Klaus) Venkatachala & Goçzán; S = Brachyphyllum scottii Kendall; T = flora dominated by Corollina torosus (Reissinger) Klaus. Redfeldius is a subholostean fish with a restricted zone in the Newark Group. Numbers shown for the Newark and Hardord basins refer to our palyniferous localities in these basins. The letters defined above indicate presence of the indicated form. M and T generally indicate dominance. Parentheses indicate forms present in variable but minor amounts.

The stratigraphic position of the Triassic-Jurassic boundary in the Hartford Basin might naturally be placed in that formation where the greatest change in Corollina species occurs, thus relegating strata containing the flora dominated by Corollina meyeriana to the Triassic, and strata dominated by Corollina torosus to the jurassic. It might further be argued that the Corollina-dominated Kössen facies supports a Rhaetian age for the Shuttle Meadow Formation. However, evidence of a basal Liassic Age for the formation comes from the composition of the non-Corollina portion of the assemblage. The Shuttle Meadow Formation contains Convolutispora klukiforma, which is characteristic of the European Liassic, rarely being found in the Rhaetian, and absent from the Kössen facies. Conversely, the Kössen facies contains three species of Ovalipollis in relatively large numbers (5-16%). This pollen genus is frequently found in the Rhaetian, but is very rare to absent in Liassic paiynofloras. In lacking Ovalipollis, the Shuttle Meadow flora is similar to basal Liassic floras.

Kendall (1949) provided only a brief description of the Larachbeg, Scotland, palynoflora. However, she did provide a very detailed description of cuticle from Brachyphyllum scotii Kendall, associated with abundant pollen (more than 90%) supposedly derived from that plant. At a locality 2.2 km north of Midland, Virginia (Culpeper Basin), reported by Baer and Martin (1949), a similar association of Corollina and well-preserved cuticle, including whole leaves, of B. scotii was recently discovered in a gray brown shale-siltstone sequence exposed along a brook, Licking Run. Many palyniferous layers also occur in the Licking Run section. Fish-bearing black calcareous shale outcrops suatigraphically about 2.2 m below the megafossil plant bed. The fish fauna from this locality is remarkably similar to the one from the Shuttle Meadow Formation at Locality 1 (Cornet, et al., 1973; Schaeffer, 1967; P. E. Olsen, pers. comm.). A more detailed study of the Midland flora is in progress.

The Midland flora is essentially identical to that from the Shuttle Meadow Formation, including the presence of Convolutispora klukiforma. The abundant pollen, including tetrads and pollen masses, associated with the B. scotii cuticle at Midland, is identical with Corollina meyeriana (Klaus) Venkatachala and Goçzán. Several distinct species of Dictyotriletes (a genus characteristic of the Jurassic) are also present. One of these species (Dictyotriletes sp. 1) is present at Locality 8 in the upper New Haven Arkose of Massachusetts: (Locality 8 is considered contemporaneous with part of the Shuttle Meadow Fm.; Text-fig. 3). Moderately corroded but identifiable cuticle, including whole leaves, of B. scotii has also been recovered from Shuctle Meadow Locality 1 of the Hartford Basin and from lake beds above the lowest lava-flow unit (First Watchung Mt.), just east of Round Top Mountain, near Oldwick, New Jersey (Locality 4, Newark Basin, Text-fig. 5).

The Shuttle Meadow, Midland, and Larachbeg palynofloras appear to have much in common. The identification of B. scotii merely indicates that a basal Liassic age is possible. Only one age horizon is known for this conifer – thus it is of little time-stratigraphic value, especially if it were the only source for C. meyeriana, which is doubtful. However, the presence of B. scotii, C. klukiforma, Dictyotriletes sp. 1, the dominance of C. meyeriana, and the absence of any palynomorph known to be characteristic of only the Triassic, favors an early Liassic age for the Shuttle Meadow and Midland floras.

Todites pinceps (Presl) Gothan was discovered by the first author in the youngest sediments of the Culpeper Basin, near Leesburg, Va. This fern has been found mainly in late Rhaetian to Middle Jurassic age strata (Harris, 1948, p. 182, 183). Clathropteris meniscoides Brongniart has been found at Localities 2 and 8 in the Hardord Basin, and Locality 4 in the Newark Basin. This fern may range from Carnian through the Liassic, but is particularly common in the Rhaetian and lower Liassic (Harris, 1931). Both of these ferns were found in association with a flora dominated by C. meyeriana, and this strongly indicates a Rhaeto-Liassic age for this type of association.

In order to examine palynofloras that are slightly older than those of the Shuttle Meadow Fm. of Connecticut, one must refer to strata in the Newark Basin of New Jersey, because palynomorphs have not been found in the older Talcott Fm. of Connecticut, nor in strata of the New Haven Arkose known to be older than the Talcott (Text-fig. 5). Correlation of footprint and fish faunas (P. E. Olsen, pers. comm.), and of palynofforules and lava flows for the Hartford and Newark basins (Text-fig. 5), indicates that some strata in New Jersey containing a typical Shuttle Meadow palynoflora may be older than the Shuttle Meadow Formation of Connecticut. The seventeen fish localities so far investigated by Olsen from sediments between the First (lowest) and Third (highest) Watchung lava-flow units lack the subholostean, Redfieldius spp., which is frequently found in younger strata. Therefore it is apparent that the flora dominated by C. meyeriana (occurring with B. scotii) has considerable snatigtaphic range, calculated in the Newark Basin to be greater than 600 m (not including thickness oflava-flow units).

The presence of Upper Triassic reptiles, such as Stegomus, Hypsognathus, and the phytosaur, cf. Rutiodon (P. E. Olsen and J. H. Ostrom, pers. comm.), in the middle part of the New Haven Arkose (Text-tig. 5) strongly favors placing the Triassic-Jurassic boundary just above the Talcott Formation (which at present would not conflict with paleomagnetic data). The boundary might correlate with the erosional unconformity in the Hartford Basin.

Recently a well-preserved Carno-Norian palynoflorule (Locality 1, Newark Basin, Text-fig. 5) was obtained from gray shales of the lower Brunswick Formation at Milford, New Jersey (gray members L-M of McLaughlin, 1946). The florule is dominated by bisaccates: Alisporites, Klausipollenites, Pityosporites, Protodiploxypinus, Platysaccus, Triadispora, Chordasporites?, and Podosporites? There are also moderate percentages of Camerosporites verrucosus Mädler, Patinasporites densus Leschik, Vallasporites ignacii Leschik, and tetrads of spherical psilate grains ("Genus A") only before described by Dunay (1972) from the Upper Triassic Dockum Group of northwest Texas. The stratigraphic position of this middle Keuper florule from New Jersey is about 920 m above "gray member B" of McLaughlin (1944), which is the top of the underlying Lockatong Formation. However, the relationship of the florule to the overlying First Watchung Mountain basalt is less certain, as most of the Brunswick Formation, including the lava flows, is not preserved around Milford, N.J., and very few "unfaulted" sections of the entire lower Brunswick have been measured. Kummel (1836, p. 58) measured one such section "between the mouth of Lawrence Brook, east of New Brunswick, and the base of the first trap ridge back of Bound Brook" as being 3050 m thick. Because of the relative proximity of this measured section to Milford, N.J. (in relationship to the rest of the basin), this figure can be safely used to calculate the approximate distance of the Milford florule beneath the First Watchung Mountain lava-flow unit, a distance of critical importance in the following argument (cf. Text-fig. 5).

Van Houten (1363) estimated the rate of sedimentation fbr the Brunswick Formation at 30   +mm/-1000 yr. The Milford florule lies approximately 2100 m below the First Watchung Mountain basalt (= 3050 m-920 m). The Milford Carno-Norian florule would then be separated in time from the oldest known occurrence of a florule dominated by Corollina meyeriana (occurring with Brachyphyllum scotii) in the Newark Basin by at least 6.9 m.y. This amount of time would accommodate much of the Norian and Rhaetian stages and agrees well with the paleomagnetic normal polarity of the lava flows, which can readily be explained if most of the Rhaetian occurred before extrusion of the lava-flow units (Creer, 1971; Reeve and Helsley, 1972). For comparison, the maximum thickness of Upper Triassic strata in England and Germany appears to be 1400 m, but it is usually less than 500 m (Geiger and Hopping, 1968; Wills, 1970).

A probable upper Norian palynoflorule (samples provided by Donald Baird, Princeton Univ.; coll. by N. K. Resch) occurs in a gray siltstone with reptilean footprints, exposed in the construction of U.S. Rt. 280 behind the old Second Precinct Police Station at Newark, N.J. (Newark Basin Locality 11, Text-fig. 5). The florule is significant in that it possesses equatorially striate grains of Corollina torosus (Reissinger) Klaus, as well as C. meyeriana (Klaus) Venkatachala 8r Goçzán, Patinasporites densus Leschik, possibly Enzonalasporites vigens Leschik and Triadispora sp. C. torosus, generally not reported below the Rhaetian, and Triadispora sp., rarely reported above the middle Norian, are seldom found in the same assemblage. In addition the presence of P. densus suggests an age no younger than Norian because, while this species occurs as high as the lower Rhaetian, it is rare above the Norian. Corollina spp. represent about 30% of the assemblage. Bisaccates of the Pityosporites and Alisporites types are common, and Converrucosisporites cameronii (de Jersey) Playford & Dettmann and Granulatisporites infirmus (Balme) comb. nov. are much more common than in older florules of the Newark Group. This palynoflorule is calculated to be about 1100 m below the First Watchung Mountain basalt.

The rather low stratigraphic position of middle and upper Keuper florules in the Brunswick Formation supports the paleomagnetic evidence that at least part of the Brunswick below the First Watchung Mountain basalt is Rhaetian, but does not rule out the possibility that strata containing the generally Liassic C. meyeriana-B. scotii flora may extend downward into the upper Rhaetian. For this reason this floral assemblage is here designated Rhaeto-Liassic wherever it occurs.

The Portland Formation florules of the Hartford Basin are generally dominated by C. torosus (Table 1) and its presumed megafossil sources, Hirmerella sp. (Locality 7, Cornet et al., 1973) and Hirmerella muensteri (Schenk) Jung 1968 (Localities 10, 11, and 13). Lower Portland florules (Localities 5, 6, 7, and 13) appear to vary laterally and to fluctuate vertically in Corollina spp. percentages, with C. meyeraana sometimes comprising much more than 2%, but rarely being dominant. poor preservation of most of these florules makes specific identification difficult, but cuticle fragments show that the ratio of Brachyphyllum scotii to Hirmerella spp. varies in proportion to the apparent ratio of C. meyeriana to C. torosus. The minor constituents of the Portland Formation assemblage include several good Liassic or Jurassic indicators, such as Corollina itunensis, Callialasporites cf. C. dampieri, Callialasporites trilobatus, Araucariacites fissus, Cycadopites reticulatus, Perotriletes cf. P. pseudoreticulatus, Leptolepidites cf. L. major, and Gleicheniidites cf. G. nilssonii.

The overall composition of the flora compares well with that of the Liassic (Balme, 1957; Couper, 1958; Nilsson, 1958; Wall, 1965; Schulz, 1967; Reiser and Williams, 1963; Pocock, 1970; Volkheimer, 1971; Volkheimer, 1972; Antonescu, 1973), particularly in the dominance of Corollina torosus and the presence of Corollina itunensis, C. meyeriana, Araucariacites australis, A. fissus, Cycadopites deterius, C. reticulatus, C. jansonii, Alisporites thomasii, Pityopollenites pallidus, Platysaccus cf. P. lopsiensis, Perinopollenites elatoides, Callialasporites spp., Granulatisporites infirmus, Converrucosisporites cameronii, Todisporites rotundiformis, Gleicheniidites cf. G. nilssonii, Leptolepidites sp., and Harrisispora sp. Even though many of these palynomorphs are long ranging and not good index fossils, together they make up a flora unlike any flora reported from the Triassic.

In contrast to those of the Upper Triassic, palynofloral assemblages of the Liassic are relatively uniform, both geographically and chronologically. Although new species appear throughout the Liassic, floral change is gradual, with a. number of plant types forming dominant associations over wide geographic areas. Minor floral constituents seem to be the most variable. Several good index spores and pollen have been recognized, such as certain species of Dictyotriletes, Contignisporites, and Callialasporites. When present in significant amounts (generally greater than 1%), these forms can be used to distinguish the upper part of the Liassic from the lower and middle parts.

Antonescu (1973) reported the presence in very small amounts of several characteristic upper Liassic palynomorphs in the middle Liassic of Rumania: Callialasporites and Leptolepidites. The rare occurrence at our Locality 11 of Callialasporites cf. C. dampieri, Callialasporites trilobatus, Leptolepidites cf. L. minor, and Corollina itunensis, generally not reported below the upper Liassic, suggests that the middle part of the Portland Formation is perhaps Pliensbachian or younger in age. Dictyotriletes spp. (Pl. 1, fig. 4-6) and Convolutispora klukiforma are present in the Hartford and Culpeper basins in strata presumed to be older than the Portland Formation, Such an occurrence strongly favors an early to middle Liassic age for much of the Portland Formation (Text-fig. 5). The upper part of the Portland is as yet unsampled, but based on stratigraphic thickness, this part of the formation could well be upper Liassic.

PLATE 7

1 Camerosporites reductiverrucatus n. sp. (Holotype). Locality II, 54 um.
2 C. reductiverrucatus n. sp. Locality 11; composite photograph of two focal levels, 46 um-56 um.
3 C. reductiverrucatus n. sp. Locality 1 1, 53 um.
4 C. reductiverrucatus n. sp. Locality 11, 58 um.
5 C. reductiverrucatus n. sp. Locality 11, triradiate fold present; distal part of grain missing, 39 um.
6 Araucariacites fissus Reiser & Williams. Locality 11, 90 um.
7 A. fissus. Locality 11, 76 um.

PLATE 8

1 Cycadopites reticulatus (Nilsson) comb. nov. Locality 5, 54 um.
2 C. reticulatus (Nilsson) comb. nov. Locality 11, 48 um (under oil).
3 C. reticulatus (Nilsson) comb. nov. Locality 5, 32 um wide (under oil).
4 Cycadopites westfieldicus n. sp. (Holotype). Locality 11, 60 um.
5 C. westfieldicus n. sp. Locality 11, 60 um (under oil).
6 C. westfieldicus n. sp. Locality 11, 60 um (under oil).
7 Cycadopites cf. C. jansonii Pocock. Locality 5, 36 um.
8 Cycadopites cf. C. jansonii. Locality 5, 35 um.
9 Cycadopites cf. C. jansonii. Locality 5, 46 um.
10 Cycadopites deterius (Balme) Pocock. Locality 5, 49 um.
11 C. deterius. Locality 11, 41 um.
12 C. deterius. Locality 5, 51 um.
13 Cycadopites durhamensis n. sp. (Holotype). Locality 1, 26 um.
14 C. durhamensis n. sp. Locality 1, 28 um.
15 C. durhamensis n. sp. Locality 1, 29 um.
16 Cycadopites sp. 1. Locality 8, 45 um.
17 Cycadopites andrewsii n. sp. Locality 8, S.E.M.; 34 um.
18 C. andrewsii n. sp..locality 8, 37 um.
19 C. andrewsii n. sp. Locality 8, 34 um.
20 C. andrewsii n. sp. (Holotype). Locality 8, 37 um.
21 C. andrewsii n. sp. Locality 8, 42 um.