Geological Survey Professional Paper 374—G Foraminifera from the Northern Olympic Peninsula, Washington

SYSTEMATIC DISCUSSION

Discussions and illustrations are restricted to 42 species that display either stratigraphic or paleoecologic significance in the northern Olympic Peninsula. A complete synonomy of each species is not attempted, but rather pertinent references are listed, one of which will supply a more complete synonomy.

The frequent use of qualifiers such as "cf." and "aff." has been necessary because many forms are represented by few specimens and many specimens are poorly preserved.

Family VALVULINIDAE
Genus TRITAXILINA Cushman, 1911
Tritaxilina colei Cushman and Siegfus
Plate 5, figure 2

Tritaxilina colei Cushman and Siegfus, 1935, Cushman Lab. Foram. Research Contr., v. 11, pt. 4, p. 92, pl. 14, figs. 5, 6.

Cushman and Siegfus, 1942, San Diego Soc. Nat. History Trans., v. 9, no. 34, p. 403, pl. 15, figs. 12, 13.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 128, pl. 27, fig. 9.

This species is present in a few samples from the Aldwell formation and the lower part of the Twin River formation. It was originally described from the Kreyenhagen shale (Cushman and Siegfus, 1935) and has since been recorded from California throughout rocks of Eocene age.

Figured specimen (USNM 626981) from USGS locality f11884.

Family MILIOLIDAE
Genus QUINQUELOCULINA d'Orbigny, 1826
Quinqueloculina goodspeedi Hanna and Hanna
Plate 5, figure 1

Quinqueloculina goodspeedi Hanna and Hanna, 1924, Washington Univ. [Seattle] Pub. Geology, v. 1, no. 4, p. 58, pl. 13, figs. 3, 4.

Beck, 1943, Jour. Paleontology, v. 17, no. 6, p. 592, pl. 99, figs. 1, 2.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 429, pl. 63, figs. 6-S.

This species is characterized by its elongate shape, rounded cross section, and a slightly protruding, round aperture with a thin tooth extending from the base. Although it is uncommon in the mapped area, it is useful when present because it indicates a late Eocene age in western Washington. It is known from the Cowlitz formation (Beck, 1943), the Skookumchuck formation, and the upper part of the McIntosh formation of southwestern Washington (Rau, 1958). It occurs in the lower part of the Twin River formation in the northern Olympic Peninsula.

Figured specimen (USNM 626982) from USGS locality f11874.

Quinqueloculina weaveri Rau
Plate 5, figure 3

Quinqueloculina weaveri Rau, 1948, Jour. Paleontology, v. 22, no. 2, p. 159, pl. 28, figs. 1-3.

Rau, 1951, Jour. Paleontology, r. 25, no. 4, p. 430, pl. 63, fig. 4.

Quinqueloculina weaveri differs from Q. goodspeedi in that its cross section is more angular, the apertural face slopes, and the base of the aperture is flattened. This species usually occurs in rocks of the Refugian stage, but it is also found in the northern Olympic Peninsula in rocks assigned to the Zemorrian stage.

Figured specimen (USNM 626983) from USGS locality f11793.

Family LAGENIDAE
Genus ROBULUS Montfort, 1808
Robulus cf. R. calcar (Linne)
Plate 5, figure 4

Robulus cf. R. calcar (Linne). Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 431, pl. 63, figs. 23, 24.

Angular areas are present on the periphery of some specimens of Robulus where the periphery is joined by the sutures. Blunt spines even are formed at these angular areas on some specimens. All specimens displaying these features are tentatively and in a broad sense referred to R. calcar (Linné). This general form seems to be a good marker fossil for rocks of the Zemorrian stage in western Washington and Oregon because it is recorded only from rocks of this age in southwestern Washington (Rau, 1958) and is known from the rocks of the same age in western Oregon. It occurs in the upper part of the Twin River formation in the northern Olympic Peninsula.

Figured specimen (USNM 626984) from USGS locality f11754.

Robulus welchi Church
Plate 5, figure 6

Robulus welchi Church, 1931, California Dept. Nat. Resources, Div. Mines Rept. State Mineralogist. No. 27, pl. C, figs. 13, 14.

Church, 1943, California Dept. Nat. Resources, Div. Mines Bull. 118, p. 182.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 143, pl. 7, fig. 8.

Because of poor preservation, identification of this species is based on a group of specimens rather than a single individual. The species is not common but is present in a few samples from the Aldwell formation and the lower part of the Twin River formation. In western Washington and Oregon this species is known only from rocks of late Eocene age. California records are also all from strata of late Eocene age (Mallory, 1959, p. 143).

Figured specimen (USNM 626985) from USGS locality f11726.

Family NONIONIDAE
Genus NONION Montfort, 1808
Nonion costiferum (Cushman)
Plate 5, figure 5

Nonionella boueane Chapman (not d'Orbigny), 1900, California Acad. Sci. Proc., ser. 3, Geology, v. 1, p. 225, pl. 30, fig. 14.

Nonion costiferum (Cushman). Kleinpell, 1938, Miocene stratigraphy of California: Am. Assoc. Petroleum Geologists, p. 229, pl. 15, fig. 13.

Rau, 1948, Jour. Paleontology, v. 22, no. 6, p. 777, pl. 119, figs. 5, 6.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 436, pl. 64, fig. 7.

This species is common in all samples from the Clallam formation but was not found in any of those below the formation. It is recorded from many localities of Miocene age in California, Oregon, and Washington (Kleinpell, 1938). The lowest occurrence of Nonion costiferum generally coincides with the base of the Saucesian stage. Therefore its lowest occurrence in the northern Olympic Peninsula at the base of the Clallam formation suggests a Saucesian age for at least the lower part of the formation.

Figured specimen (USNM 626986) from USGS locality f11891.

Nonion incisum (Cushman)
Plate 5, figure 9

Nonionina incisa Cushman, 1926, Cushman Lab. Foram. Research Contr., v. 1, pt. 4, p. 90, pl. 13, fig. 3.

Nonion incisa (Cushman). Cushman and Laiming, 1931, Jour. Paleontology, v. 5, no. 2, p. 104, pl. 11, fig. 10.

Nonion incisum (Cushman). Cushman and Parker, 1931, Cushman Lab. Foram. Research Contr., v. 7, pt. 1, p. 7, pl. 1, fig. 26.

Cushman and LeRoy, 1938, Jour. Paleontology, v. 12, no. 2, p. 125, pl. 22, figs. 8, 9.

Many variations are shown among the specimens that are referred to this species. Some of the more conspicuous variations are in the amount of flaring of the latter chambers, the height relative to breadth, the thickness, and the amount of depression of sutures. Regardless of these variations, all specimens fall within the limits of the species sensu lato.

Nonion incisum is a useful fossil in the northern Olympic Peninsula because there it is known to occur only in the upper part of the Zemorrian stage and the Saucesian stage where it is reasonably frequent.

Variations of the species have been recorded from California and Oregon from rocks referred to the upper part of Kleinpell's Zemorrian stage and to the lower part of his Luisian stage (Kleinpell, 1938, p. 146, 232, 233).

Figured specimen (USNM 626987) from USGS locality f11731.

Nonion cf. N. pompilioides (Fichtel and Moll)
Plate 5, figure 7

Forms displaying bilateral symmetry and a broad final chamber are tentatively referred to Nonion pompilioides (Fichtel and Moll). (See Cushman, 1939, p. 19, pl. 5, figs. 9-12.) Most of the specimens came from rocks of the Zemorrian stage; however, a few specimens were also found in rocks of the Refugian stage.

Figured specimen (USNM 626988) from USGS locality f 11749.

Genus ELPHIDIUM Montfort, 1808
Elphidium cf. E. minutum (Reuss)
Plate 5, figure 8

The description of this species given by Cushman (1939, p. 40) agrees closely with that of a number of specimens from the upper part of the rock sequence of the northern Olympic Peninsula. However, his illustrations (Cushman, 1939, pl. 10, figs. 22-25) all display coarser retral processes than are developed on the specimens under question. Inasmuch as Cushman stated that the retral processes are very slightly developed, they may have been overemphasized in his illustrations.

Elphidium cf. E. minutum was found only in rocks assigned to the upper part of the Zemorrian stage and the Saucesian stage within the mapped area. It is also recorded from rocks of Zemorrian and Saucesian age in southwestern Washington (Rau, 1951, 1958).

Figured specimen (USNM 626989) from USGS locality f11891.

Family HETEROHELICIDAE
Genus PLECTOFRONDICULARIA Liebus, 1903
Plectofrondicularia packardi multilineata Cushman and Simonson
Plate 5, figure 15

Plectofrondicularia packardi multilineata Cushman and Simonson, 1944, Jour. Paleontology, v. 18, no. 2, p. 197, pl. 32, figs. 2-4.

Detling, 1946, Jour. Paleontology, v. 20, no. 4, p. 355, pl. 49, figs. 3, 5.

Rau, 1948, Jour. Paleontology, v. 22, no. 2, p. 171, pl. 30, fig. 19.

Smith, 1956, California Univ. Dept. Geol. Sci. Bull., v. 32, no. 2, p. 94, pl. 12, fig. 6.

Plectofrondicularia gracilis Smith, 1956, California Univ. Dept. Geol. Sci. Bull., v. 32, no. 2, p. 93, pl. 12, figs. 2-5.

The Tertiary sequence of Washington, Oregon, and California contains a strain of Plectofrondicularia which displays considerable variation in form. The variant most significant stratigraphically was originally described from the Bastendorff shale of Oregon and called P. packardi Cushman and Schenck (1928). Subsequently a more common and widely distributed variant was described from the Tumey formation of California and referred to P. packardi multilineata Cushman and Simonson (1944). Studies of the faunas of the Tertiary rocks of Oregon and Washington strongly suggest that there, at least, P. packardi packardi does not occur above the Refugian stage and is found only occasionally in the underlying Narizian stage. However, P. packardi multilineata occurs throughout rocks of late Eocene, Oligocene, and possibly early Miocene age. Many variants of the strain displaying a complete gradation from one form to another were found in samples from the northern Olympic Peninsula. Those referred to P. packardi packardi have few short and coarse costae which are sometimes curved on the initial chamber. The remaining forms of various shapes with varying number of straight and longer costae are referred to P. packardi multilineata. Certain variances in the latter group have been examined for stratigraphic value and have been found to be of no importance. Therefore, they are all grouped under the single name P. packardi multilineata in this study. P. gracilis Smith is within this group and is placed in synonomy with P. packardi multilineata in the report.

Figured specimen (USNM 626990) from USGS locality f11736.

Plectofrondicularia packardi packardi Cushman and Schenck
Plate 5, figure 13

Plectofrondicularia packardi Cushman and Schenck, 1928, California Univ. Dept. Geol. Sci. Bull., v. 17, no. 9, p. 311, pl. 43; figs. 14-15.

Cushman and Simonson, 1944, Jour. Paleontology, v. 18, no. 2, p. 197, pl. 31, figs. 17, 18, pl. 32, fig. 1.

Detling, 1946, Jour. Poleontology, v. 20, no. 4, p. 355, pl. 49, fig. 1.

Rau, 1951, Jour. Paleontology v. 25, no. 4, p. 438, pl. 65, fig. 12.

Wilson, 1954, California Univ. Pub. Geol. Sci. Bull., v. 30, no. 2, p. 138, pl. 15, fig. 8.

Smith, 1956, California Univ. Pub. Geol. Sci. Bull., v. 32, no. 2, p. 94, pl. 12, figs. 1, 7.

Discussion of this species is under Plectoforndicularia packardi multilineata.

Figured specimen (USNM 626991) from USGS locality f11876.

Family BULIMINIDAE
Genus BULIMINELLA Cushman, 1911
Buliminella subfusiformis Cushman
Plate 5, figure 12

Buliminella subfusiformis Cushman, 1925, Cushman Lab. Foram. Research Contr., v. 1, pt. 2, p. 33, pl. 5, fig. 12.

Cushman, Stewart, and Stewart, 1947, Oregon Dept. Geology and Mineral Industries Bull. 36, pt. 1, p. 17, pl. 2, fig. 7.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 439, pl. 65, fig. 5.

This species occurs rarely in the rocks of the northern Olympic Peninsula, only in the upper part of the Twin River formation. Records of Buliminella subfusiformis in Washington, Oregon, and California strongly suggest that it does not occur in rocks older than those of the Zemorrian stage. In southwest Washington it is recorded from the Pseudoglandulina aff. P. inflata zone and the Epistominella parva zone (Rau, 1958) of the Zemorrian and Saucesian stages, respectively. It is known in Oregon from the Astoria formation (Cushman, Stewart, and Stewart, 1947) and the Nye mudstone. In California, Kleinpell (1938) recorded this species from the lower part of the Zemorrian stage to the lower part of the Delmontain stage.

Figured specimen (USNM 626992) from USGS locality f11867.

Genus BULIMINA d'Orbigny, 1826
Bulimina corrugata Cushman and Siegfus
Plate 5, figure 11

Bullimina corrugata Cushman and Siegfus, 1936, Cushman Lab. Foram. Research Contr., v. 11, Pt. 4, p. 92, pl. 14, fig. 7.

Graham and Classen, 1955, Cushman Found. Foram. Research Contr., v. 6, pt. 1, p. 19, pl. 3, fig. 17.

Rau, 1956, Cushman Found. Foram. Research Contr., v. 7. pt. 3, p. 75, pl. 15, fig. 5.

The present specimens are small, tend to be triangular in cross section, display the greatest breadth slightly above the middle, and have numerous longitudinal costae extending continuously over all but the last chamber. These features characterize Bulimina corrugata as described by Cushman and Siegfus.

This species was found locally in the Crescent and Aldwell formations and the lower part of the Twin River formation. In southwest Washington it is recorded from the Bulimina cf. B. jacksonensis zone and the Uvigerina cf. U. yazooensis zone of McIntosh formation (Rau, 1956, 1958). In Oregon it has been observed by the writer in samples from the Umpqua formation, lower part of the Toledo formation, Nestucca formation, Yamhill formation, and the Elkton siltstone member of the Tyee formation. The highest occurrence of B. corrugata in both Oregon and Washington is generally in the lower part of the sequence of late Eocene age. According to Mallory (1959), B. corrugata occurs in California in rocks ranging in age from his Ulatisian stage to his Narizian stage.

Figured specimen (USNM 626993) from USGS locality f11886.

Bulimina lirata Cushman and Parker
Plate 5, figure 17

Bulimina lirata Cushman and Parker, 1936, Cushman Lab. Foram. Research Contr., v. 12, pt. 2, p. 43, pl. 8, fig. 2.

Cushman and Simonson, 1944, Jour. Paleontology, v. 18, no. 2, p. 198, pl. 32, fig. 13.

Smith, 1957, California Univ. Pub. Geol. Sci., v. 32, no. 3, p. 174, pl. 24, fig. 13.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges, Am. Assoc. Petroleum Geologists, p. 193, pl. 37, fig. 1.

Bulimina cf. B. lirat Cushman and Parker. Cushman and Siegfus, 1942, San Diego Soc. Nat. History Trans., v. 9, no. 34, p. 413, pl. 17, fig. 3.

A few costate specimens of Bulimina are relatively broad with respect to length and taper rapidly to a sharp initial end. They compare well in all respects to B. lirata Cushman and Parker, which, according to Mallory (1959, p. 85), is known from his Penutian, Ulatisian, and Narizian stages of the upper part of the Eocene sequence of California.

This species has not been recorded previously from Washington or Oregon but has been observed by the writer in samples from the Umpqua formation and rocks of probable equivalent age in Oregon. In the northern Olympic Peninsula it was found in a few samples from both the Aldwell formation and the lower part of the Twin River formation.

Figured specimen (USNM 626994) from USGS locality f11873.

Bulimina alsatica Cushman and Parker
Plate 5, figure 16

Bulimina alsatica Cushman and Parker, 1937, Cushman Lab. Foram. Research Contr., v. 13, pt. 1, p. 39, pl. 4, figs. 6, 7.

Cushman and Parker, 1947, U.S. Geol. Survey Prof. Paper 210-D, p. 102, pl. 24, figs. 10, 11.

A small, comparatively broad Bulimina with jagged costae over all chambers except those of the last whorl compares well with the illustrations and description of B. alsatica Cushman and Parker. This species is known from rocks of Oligocene age in France and Germany and from rocks of Miocene age in Italy, Spain, and Florida. It has also been tentatively recorded from rocks of Oligocene age in Washington (Rau, 1958). In the Twin River formation it occurs most frequently in rocks that are assigned to the Zemorrian stage. It also makes a rare occurrence in the Refugian part of the Twin River formation.

Figured specimen (USNM 626995) from USGS locality f11749.

Bulimina cf. B. alsatica Cushman and Parker
Plate 5, figure 14

This form differs from Bulimina alsatica in that costae do not extend as far up on the test and the costae appear to be pointed projections on the base of the chambers rather than platelike costae over the entire chamber. This form is found together with B. alsatica in the upper part of the Twin River formation.

Figured specimen (USNM 626996) from USGS locality f11815.

Bulimina schencki Beck
Plate 5, figure 10

Bulimina capitata ? Cushman and Dusenbury (not Yokoyama), 1934, Cushman Lab. Foram. Research Contr., v. 10, pt. 3, p. 61, pl. 8, fig. 10.

Bulimina schencki Beck, 1943, Jour. Paleontology, v. 17, no. 6, p. 605, pl. 107, figs. 28, 33.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 196, pl. 16, fig. 15.

A few specimens were found in the lower part of the Twin River formation that display all the characteristics of Bulinina schencki. One specimen questionably identified as this species came from the Crescent formation.

Bulimina schencki Beck (1943) was originally described from the Cowlitz formation of southwest Washington and has been recorded since from the Skookumchuck formation of the same area (Rau, 1958). In California Mallory (1959) recorded this species from the upper part of his Ulatisian stage and his Narizian stage. It has been found in the Poway conglomerate, Cozy Dell formation, Point of Rocks formation, and the type Tejon formation (Mallory, 1959).

Figured specimen (USNM 626997) from USGS locality f11875.

Bulimina sculptilis laciniata Cushman and Parker
Plate 6, figure 1

Bulimina sculptilis Cushman. Cushman and Schenck, 1928, California Univ. Dept. Geol. Sci. Bull., v. 17, no. 9, p. 311, pl. 43, fig. 16.

Bulimina sculptilis laciniata Cushman and Parker, 1937, Cushman Lab. Foram. Research Contr., v. 13, pt. 1, p. 38, pl. 4, fig. 4.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 441, pl. 65, fig. 22.

This large Bulimina with continuous, jagged, and platelike costae was found only in strata of the Twin River formation that are referred to the Refugian stage. It was originally described from beds at Waldport, Oreg., which are regarded as Zemorrian in age by the writer. It is also known in Oregon from the Bastendorff shale and the Keasey formation (Cushman and Schenck, 1928) of Refugian age. The southwestern Washington occurrences are from the Sigmomorphina schencki zone of the Refugian stage and the Bulimina schencki-Plectofrondicularia cf. P. jenkinsi zone of latest Eocene age (Rau, 1958). Although the species is found occasionally both above and below the Refugian stage, its occurrence is most frequent in the Refugian stage.

Figured specimen (USNM 626998) from USGS locality f11865.

Genus ENTOSOLENIA Ehrenberg, 1848
Entosolenia sp.
Plate 6, figure 2

Test broadly ovate, slightly compressed, walls smooth, finely perforate; aperture a narrow slitlike opening. Length of figured specimen 0.35 mm; breadth 0.29 mm; thickness 0.23 mm.

This form is uncommon in rocks of the northern Olympic Peninsula. Its known occurrence is confined largely to strata of Zemorrian age in the Twin River formation and therefore locally, at least, it has stratigraphic significance.

Figured specimen (USNM 626999) from USGS locality f11751.

Genus BOLIVINA d'Orbigny, 1839
Bolivina advena Cushman
Plate 6, figure 4

Bolivina advena Cushman, 1925, Cushman Lab. Foram. Research Contr., v. 1, pt. 2, p. 29, pl. 5, fig. 1.

Kleinpell, 1938, Miocene stratigraphy of California: Am. Assoc. Petroleum Geologists, p. 264, pl. 7, fig. 6.

Cushman, Stewart, and Stewart, 1947, Oregon Dept. Geology and Mineral Industries Bull. 36, pt. 1, p. 18, pl. 2, fig. 12.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 442, pl. 65, fig. 9.

This species is rare in the present material. It occurs only in the uppermost part of the Twin River formation and the Clallam formation. It is known in southwest Washington from the Epistominella parva zone (Rau, 1958), and in Oregon it is recorded from the Astoria formation (Cushman, Stewart, and Stewart, 1947). The species is known in California from rocks ranging in age from that of the Saucesian stage to the Mohnian stage (Kleinpell, 1938). In the northern Olympic Peninsula the presence of Bolivina advena in the rocks suggests a relatively high stratigraphic position in the local Tertiary sequence.

Figured specimen (USNM 627000) from USGS locality f11749.

Bolivina marginata adelaidana Cushman and Kleinpell
Plate 6, figure 8

Bolivina marginata adelaidana Cushman and Kleinpell, 1934, Cushman Lab. Foram. Research Contr., v. 10, pt. 1, p. 10, pl. 2, figs. 1, 2.

Cushman, Stewart, and Stewart, 1947, Oregon Dept. Geology and Mineral Industries Bull. 36, pt. 1, p. 18, pl. 2, fig. 13.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 443, pl. 65, fig. 14.

The spinelike extension of the chambers at the periphery and limbate sutures are well developed on the present specimens. This form occurs in rocks of Zemorrian age in the Twin River formation. In western Washington and Oregon it occurs only in strata that are no older than those of the Zemorrian stage. It is recorded from the Pseudoglandulina aff. P. inflata zone and Epistominella parva zone of southwestern Washington (Rau, 1958). In Oregon it is known from the Astoria formation (Cushman, Stewart, and Stewart, 1947) and it has been observed by the writer from the Nye mudstone, the Yaquina formation, and the upper part of the Toledo formation. Records of this variety in California are largely from beds of Saucesian age (Kleinpell, 1938, p. 277).

Figured specimen (USNM 627001) from USGS locality f11869.

Genus BIFARINA Parker and Jones, 1872
Bifarina nuttalli Cushman and Siegfus
Plate 6, figure 3

Loxostomum applini Plummer. Nuttall, 1930, Jour. Paleontology, v. 4, no. 3, p. 285, pl. 24, figs. 4, 5.

Bifarina nutttalli Cushman and Siegfus, 1939, Cushman Lab. Foram. Research Contr., v. 15, pt, pt. 2, p. 28, pl. 6., fig. 6.

Cushman and Siegfus, 1942, San Diego Soc. Nat. Hist., v. 9, no. 34, p. 413, pl. 17, fig. 4.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 204, pl. 29, fig. 2.

The specimens under consideration compare well with the type Bifarina nuttalli in that the general shape of the test is similar, the base of the chambers are crenulated, and there are longitudinal costae on the early part of the test. B. nuttalli has not been recorded previously from Washington, but it has been observed in Oregon in the Umpqua formation by the writer. This species is known in California from beds that are referred to Laiming's C zone and the lower part of his A-2 zone. Mallory (1959, p. 84, 204) indicated that B. nuttalli occurs in his Ulatisian stage and the lower part of his Narizian stage.

Figured specimen (USNM 627002) from USGS locality f11728.

Genus UVIGERINA d'Orbigny, 1826
Uvigerina churchi Cushman and Siegfus
Plate 6, figure 9

Uvigerina churchi Cushman and Siegfus, 1939, Cushman Lab. Foram. Research Contr., v. 15, pt. 2, p. 29, pl. 6, fig. 16.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 206, pl. 17, fig. 6.

The irregular longitudinal costae broken between chambers and the blunt initial end are characteristic features of Uvigerina churchi that are well shown on the specimens from the northern Olympic Peninsula. This species occurs in more than half of the assemblages of the Aldwell formation and is questionably identified from several samples from the lower part of the Twin River formation. U. churchi has not been recorded previously from either Washington or Oregon but a similar form referred to as U. cf. U. yazooensis Cushman is recorded from the zone of the same name of southwestern Washington (Rau, 1958). The latter form differs from U. churchi in that the test is more elongate and the costae are higher and more distinct. In California, U. churchi is known from strata that are referred to Laiming's A-2 zone (Laiming, 1940), and Mallory (1959) showed the occurrence of this form in his Narizian stage.

Figured specimen (USNM 627003) from USGS locality f11728.

Uvigerina cocoaensis Cushman
Plate 6, figure 5

Uvigerina cocoaensis Cushman, 1925, Cushman Lab. Foram. Research Contr., v. 1, pt. 3, p. 68, pl. 10, fig. 12.

Cushman and Schenck, 1928, California Univ. Dept. Geol. Sci. Bull., v. 17, no. 9, p. 312, pl. 43, figs. 17-19.

Cushman and Simonson, 1944, Jour. Paleontology, v. 18, no. 2, p. 199, pl. 33, fig. 1.

Cushman, 1946, Cushman Lab. Foram. Research, Spec. Pub. 16, p. 28, pl. 5, figs. 15-20.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 444, pl. 65, fig. 28.

Wilson, 1954, California, Univ. Pub. Geol. Sci., v. 30, no. 2, p. 140, pl. 16, fig. 2.

Smith, 1956, California Univ. Pub. Geol. Sci., v. 32, no. 2, p. 96, pl. 12, fig. 11.

This well-known species occurs in the northern Olympic Peninsula only in strata of Refugian age. Because of its relatively frequent occurrence in the Twin River formation and because of its known restricted occurrence in rocks of the Refugian stage in other areas, it is a useful species for identifying rocks of Refugian age in the northern Olympic Peninsula. In southwest Washington Uvigerina cocoaensis is recorded from the Sigmomorphina schencki zone (Rau, 1958), and in Oregon it is known from the Bastendorff shale and the Keasey formation (Cushman and Schenck, 1928; Detling, 1946). Records of the species in California are from the Tumey formation (Cushman and Simonson, 1944), the Gaviota formation (Wilson, 1954), and the Wagonwheel formation (Smith, 1956). In all cases the containing beds have been regarded as Refugian in age.

Figured specimen (USNM 627004) from USGS locality f11862.

Uvigerina gallowayi Cushman
Plate 6, figure 7

Uvigerina gallowayi Cushman, 1929, Cushman Lab. Foram. Research Contr., v. 5, pt. 4, p. 94, pl. 13, figs. 33, 34.

Kleinpell, 1938, Miocene stratigraphy of California: Am. Assoc. Petroleum Geologists, p. 294, pl. 5, figs. 1, 2, 5.

Cushman and Simonson, 1944, Jour. Paleontology, v. 18, no. 2, p. 200, pl. 32, figs. 18, 19.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 444, pl. 65, fig. 24.

This species is restricted to a few samples from the upper part of the Twin River formation. Although uncommon in the area, its presence high in the local sequence is in accordance with previous records of Uvigerina gallowayi which are from beds of the Zemorrian stage only. In southwestern Washington it is known from beds that are assigned to the Zemorrian stage (Rau, 1958). There are no records of the species from Oregon but the writer has observed it in the Bastendorff shale. In California it is recorded from beds mapped largely as the Vaqueros formation or Temblor formation (Kleinpell, 1938, p. 294).

Figured specimen (USNM 627005) from USGS locality f11748.

Uvigerina garzaensis Cushman and Siegfus
Plate 6, figure 6

Uvigerina garzaensis Cushman and Siegfus, 1939, Cushman Lab. Foram. Research Contr., v. 15, pt. 2, p. 28, pl. 6, fig. 15.

Cushman and Simonson, 1944, Jour Paleontology, v. 18, no. 2, p. 199, pl. 32, figs. 20, 21.

Detling, 1946, Jour. Paleontology, v. 20, no. 4, p. 357, pl. 50, fig. 8.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 445, pl. 65, fig. 19.

This species is one of the more frequently occurring forms in the Tertiary sequence of the northern Olympic Peninsula. It is found throughout the Aldwell and Twin River formations. The shape and size of the test are noticeably varied but these variations are gradational and show no stratigraphic significance. Several described species probably are within the range of variance of the present specimens, but no stratigraphic usefulness is gained by dividing the group and therefore in this report they are all referred to one species, Uvigerina garzaensis. U. garzaensis has very little stratigraphic significance but its presence does suggest a general environment of cool water at substantial depths.

In California U. garzaensis is recorded largely from rocks of late Eocene age. It is known from the Coaledo and Bastendorff formations of Oregon (Detling, 1946) and has been observed by the writer in many other assemblages from Oregon of late Eocene age. It is recorded from southwestern Washington from rocks of the same age (Rau, 1958).

Figured specimen (USNM 627006) from USGS locality f11748.

Genus ANGULOGERINA Cushman, 1927
Angulogerina hannai Beck
Plate 6, figure 11

Angulogerina hannai Beck, 1943, Jour. Paleontology, v. 17, no. 6, p. 607, pl. 108, figs. 26, 28.

Cushman, Stewart, and Stewart, 1947, Oregon Dept. Geology and Mineral Industries Bull. 36, pt. 5, p. 102, pl. pl. 12, fig. 16.

Specimens from the northern Olympic Peninsula compare in detail with Beck's description and illustration of Angulogerina hannai. Although individuals of this species are never found in abundance in any one sample, it occurs frequently in the rocks of Eocene age within the area, particularly in the lower part of the Twin River formation.

The species was originally described from the Cowlitz formation (Beck, 1943). It has since been recorded from the Bulimina schencki-Plectofrondicularia cf. P. jenkinsi zone of late Eocene age in southwest Washington (Rau, 1958) and from beds of late Eocene age in the Helmick Hills of western Oregon (Cushman, Stewart and Stewart, 1947).

Figured specimen (USNM 627007) from USGS locality f11886.

Family ROTALIIDAE
Genus GYROIDINA d'Orbigny, 1826
Gyroidina orbicularis planata Cushman
Plate 6, figure 10

Gyroidina orbicularis planata Cushman, 1935, U. S. Geol. Survey Prof. Paper 181, p. 45, pl. 18, fig. 3.

Cushman and Siegfus, 1942, San Diego Soc. Nat. History Trans., v. 9, p. 419, pl. 17, fig. 32.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 447, pl. 66, figs. 4-6.

Gyroidina orbicularis planata is common in much of the Tertiary sequence of the northern Olympic Peninsula. It occurs in several samples from the Aldwell formation, is well represented in most of the samples from the Twin River formation, and is present in one sample from the Clallam formation. Its long range makes it of little stratigraphic use. However, ecologically it is useful, because it suggests substantial depths in cool to cold water. G. orbicularis planata is recorded from rocks of late Eocene age and rocks that are referred to the Refugian and Zemorrian stages in southwestern Washington (Rau, 1958). Although not recorded from western Oregon, it has been observed by the writer from many parts of the Tertiary sequence there. In California, it is recorded from rocks of late Eocene age (Mallory, 1959).

Figured specimen (USNM 627008) from USGS locality f11749.

Genus EPONIDES Montfort, 1808
Eponides mansfieldi oregonensis Cushman, Stewart, and Stewart
Plate 6, figure 12

Eponides mansfieldi Cushman. Cushman and Parker, 1931, Cushman Lab. Foram. Research Contr., v. 7, pt. 1, p. 12, pl. 2, fig. 10.

Eponides mansfieldi oregonensis Cushman, Stewart, and Stewart, 1947, Oregon State Dept. Geology and Mineral Industries Bull. 36, pt. 2, p. 48, pl. 6, fig. 4.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 447, pl. 66, figs. 14-16.

The outstanding features of Eponides mansfieldi oregonensis are the papillate umbonal area on the ventral surface, the depressed sutures on the same surface, and the slightly scalloped periphery.

In the northern Olympic Peninsula its lowest occurrence is in the lower part of the Zemorrian stage but it occurs most frequently in the upper part of the Zemorrian stage. The known occurrence of this form in southwestern Washington is in the Pseudoglandulina aff. P. inflata and Epistominella parva zones, which are assigned to the Zemorrian and Saucesian stages, respectively (Rau, 1958). It is recorded from western Oregon from the Astoria formation (Cushman, Stewart, and Stewart, 1947) and has also been observed by the writer from the Nye mudstone, the Yaquina formation, and the upper part of the Toledo formation. Associated Foraminifera suggest that the Nye mudstone is Saucesian in age, whereas the Yaquina formation and the upper part of the Toledo formation are of Zemorrian age. The known occurrence of E. mansfieldi oregonensis is therefore in rocks no older than the Zemorrian age.

Figured specimen (USNM 627009) from USGS locality f11791.

Genus CANCRIS Montfort, 1808
Cancris joaquinensis Smith
Plate 6, figure 13

Cancris joaquinensis Smith, 1956, California Univ. Pub. Geol. Sci., v. 32, no. 2, p. 98, pl. 15, figs. 5, 6.

Specimens from the northern Olympic Peninsula compare in all respects with the illustrations and description of Cancris joaquinensis Smith. The species was originally described by Smith (1956) from the Wagonwheel formation of California, which he assigned to the Refugian stage. Smith indicated that the species also was observed from the Bastendorff and Keasey formations of Oregon. In the northern Olympic Peninsula area the highest occurrence of C. joaquinensis is in the Refugian stage, but its lowest occurrence in the area is in rocks of late Eocene age. This upper Eocene occurrence extends the lower range of the species, but its highest occurrence in the Refugian stage in northern Olympic Peninsula is useful for differentiating faunas of a pre-Zemorrian age from those of Zemorrian age.

Figured specimen (USNM 627010) from USGS locality f11862.

Family AMPHISTEGINIDAE
Genus ASTERIGERINA d'Orbigny, 1839
Asterigerina crassiformis Cushman and Siegfus
Plate 6, figure 14

Asterigerina crassiformis Cushman and Siegfus, 1935, Cushman Lab. Foram. Research Contr., v. 11, pt. 4, p. 94, pl. 14, fig. 10.

Cushman and Stone, 1949, Cushman Lab. Foram. Research Contr., v. 25, pt. 4, p. 82, pl. 14, fig. 16.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 242, pl. 37, fig. 13.

This species makes its most frequent occurrence in the Aldwell formation but is also present in a few samples from the lower part of the Twin River formation. There are numerous records of this species from California (Mallory, 1959), all from rocks of middle and late Eocene age (Ulatisian and Narizian stages of Mallory), Cushman and Stone (1949) recorded it from the Verdun formation of Peru. Although there are no records of the species from Oregon, it has been observed by the writer in several samples from the Umpqua formation.

Figured specimen (USNM 627011) from USGS locality f11726.

Genus AMPHISTEGINA d'Orbigny, 1826
Amphistegina californica Cushman and M. A. Hanna
Plate 7, figure 6

Amphistegina californica Cushman and M. A. Ranna, 1927, San Diego Soc. Nat. History Trans., v. 5, no. 4, p. 56, pl. 6, figs. 3-5.

All specimens are from the Crescent formation and there they are the most common benthonic form known in the formation. Although they are all poorly preserved, a composite of the features that can be observed on various specimens constitutes Amphistegina californica as described by Cushman and Hanna (1927).

Amphistegina californica was originally described from sea cliffs near La Jolla, Calif. Mallory (1959) recorded the species only from his Ulatisian stage. There are no records of this species from either Oregon or Washington, but the writer has observed forms which may be species in the Umpqua formation of western Oregon and in rocks in southwestern Washington tentatively assigned to the Crescent formation by Pease and Hoover (1957).

Figured specimen (USNM 627012) from USGS locality f11720.

Family CASSIDULINIDAE
Genus ALABAMINA Toulmin, 1941
Alabamina kernensis Smith
Plate 7, figure 1

Alabamina kernensis Smith, 1956, California Univ. Pub. Geol. Sci., v. 32, no. 2, p. 99, pl. 15, figs. 3, 4.

Smith (1956) described this species from the Wagonwheel formation of California and also noted its occurrence in the Bastendorff shale of Oregon. The Refugian stage is represented in both of these formations. In the northern Olympic Peninsula Alabamina kernensis is found in rocks of Refugian and pre-Refugian ages in the Twin River formation and in the underlying Aldwell formation of Eocene age. These occurrences extend the records of A. kernensis into rocks of late Eocene age, but the Refugian stage remains the upper limit of its known occurrence.

Figured specimen (USNM 627013) from USGS locality f11862.

Genus CASSIDULINA d'Orbigny, 1826
Cassidulina crassipunctata Cushman and Hobson
Plate 7, figure 3

Cassidulina crassipunctata Cushman and Robson, 1935, Cushman Lab. Foram. Research, Contr., v. 11, pt. 3, p. 63, pl. 9, fig. 10.

Considerable variation in form is shown among individuals placed under this species, but they are within the limit of variation of the description of Cushman and Hobson (1935). Cassidulina crassipunctata is one of the more common species in rocks of Zemorrian age in the Twin River formation. Its lowest occurrence is useful for determining the base of the Zemorrian stage. This species has been tentatively referred to in southwestern Washington (Rau, 1958) where it also occurs in rocks of the Zemorrian stage.

The species was described from the type San Lorenzo formation of California (Cushman and Hobson, 1935) and has since been recorded in California from the Vaqueros and Temblor formations. All records of the species are from rocks of the Zemorrian stage.

Figured specimen (USNM 627014) from USGS locality f11796.

Cassidulina globosa Hantken
Plate 7, figure 4

Cassidulina globosa Hantken, 1875, Magyr. kir. foldt. int. Evkon., v. 4, p. 54, pl. 16, fig. 2.

Beck, 1943, Jour. Paleontology, v. 17, no. 6, p. 609, pl. 108, figs. 7, 13, 14.

Rau, 1951, Jour. Paleontology, v. 25, no. 4, p. 449, pl. 67, fig. 5.

Smith, 1956, California, Univ. Pub. Geol. Sci., v. 32, no. 2, p. 100, 1)1. 14, fig. 2.

Mallory, 1959, Lower Tertiary biostratigraphy of the California Coast Ranges: Am. Assoc. Petroleum Geologists, p. 226, pl. 33, fig. 11.

This species was found in the Aldwell formation and the lower part of the Twin River formation. It makes its highest occurrence in rocks of Refugian age, but it is more common in older rocks of late Eocene age.

Cassidulina globosa has a wide geographic distribution in rocks of late Eocene amid early Oligocene age. It is recorded from Europe, Peru, Mexico, southeastern United States, California, Oregon, and Washington. The species is not found in large numbers in the northern Olympic Peninsula, but when present indicates a pre-Zemorrian age.

Figured specimen (USNM 627015) from USGS locality f11843.

Family CHILOSTOMELLIDAE
Genus CASSIDULINOIDES Cushman, 1927
Cassidulinoides sp.
Plate 7, figure 2

Test elongate, only slightly compressed, close coiled in early development, last few chambers tending to uncoil; chambers distinct, slightly inflated, last few increasing rapidly in size; sutures distinct, slightly depressed; walls smooth, finely perforate; aperture a broad slit approximately 45 degrees to the axis of greatest breadth at the terminal end.

Length, 0.31 mm; breadth, 0.19 mm; thickness, 0.16 mm.

This form is known to occur only in the upper part of the Twin River formation or in those rocks assigned to the Zemorrian stage. There it appeared in a number of samples but was never common in any one sample.

Figured specimen (USNM 627016) from USGS locality f11869.

Genus SPHAEROIDINA d'Orbigny, 1821
Sphaeroidina variabilis Reuss
Plate 7, figure 7

Sphaeroidina variabilis Reuss, 1851, Zeitschr. deutsch geol. Ges., v. 3, p. 88, pl. 7, figs. 61-64.

Barbat and von Estorif, 1933, Jour. Paleontology, v. 7, no. 2, p. 173, pl. 23, fig. 19.

This species, although never abundant, is in an appreciable number of samples from the upper part of the Twin River formation. All specimens are from rocks assigned to the Zemorrian stage.

In southwest Washington it is also known from rocks of Zemorrian age (Rau, 1958) and in Oregon from the Astoria formation and Nye mudstone of Saucesian age. California records of the species are largely from rocks of the Zemorrian and Saucesian stages (Kleinpell, 1938). The many records of Sphaeroidina variabilis in Europe are from rocks of Oligocene and Miocene age. Within the northern Olympic Peninsula its presence indicates an age no older than that of the Zemorrian stage.

Figured specimen (USNM 627017) from USGS locality f11815.

Family GLOBIGERINIDAE
Genus Globigerina d'Orbigny, 1826
Globigerina cf. G. yeguaensis Weinzierl and Applin
Plate 7, figures

The genus Globigerina is represented by several forms in the Tertiary sequence of the northern Olympic Peninsula, but none are common. A form referred to as G. cf. G. yeguaensis is the only one that appears to be morphologically distinct and to be at least of local stratigraphic significance. This form is confined to rocks of Eocene age in the lower part of the Twin River formation and in the Aldwell formation. It is lobate, the three chambers of the last whorl increase rapidly in size, the walls are coarsely perforate, and the aperture has a lip.

Figured specimen (USNM 627018) from USGS locality f11729.

Family ANOMALINIDAE
Genus ANOMALINA d'Orbigny, 1826
Anomalina californiensis Cushman and Hobson
Plate 7, figure 8

Anomalina californiensis Cushman and Hobson, 1935, Cushman Lab. Foram. Research Contr., v. 11, pt. 3, p. 64, pl. 9, fig. 8.

Smith, 1956, California Univ. Pub. Geol. Sci., v. 32, no. 2, p. 100, pl. 16, fig. 3.

Considerable variation in form is observed in specimens that are referred to Anomalina californiensis. Some individuals are decidedly asymmetric, whereas others are nearly bilaterally symmetric and are difficult to differentiate from Nonion pompilioides. In most cases the test of A. californiensis is thinner than that of N. pompilioides.

In both the northern Olympic Peninsula and southwestern Washington the occurrence of A. californiensis is confined to the Refugian and Zemorrian stages. California records of this species are from rocks of the Refugian stage (Smith, 1956), Zemorrian stage, and lower part of the Saucesian stage (Kleinpell, 1938).

Figured specimen (USNM 627019) from USGS locality f11876.

Genus CIBICIDES Montfort, 1808
Cibicides celebrus Bandy
Plate 7, figure 10

Cibicides celebrus Bandy, 1944, Jour. Paleontology, v. 18, no. 4, p. 374, pl. 61, fig. 8.

Specimens occurring in the Crescent and Aldwell formations and the lower part of the Twin River formation compare in all details with the description and illustrations of Cibicides celebrus Bandy. This species is recorded from southwestern Washington from rocks of late Eocene age and of the overlying Refugian stage (Rau, 1958). It was originally described from beds of Eocene age exposed at Cape Blanco, Oreg. (Bandy, 1944).

Figured specimen (USNM 627020) from USGS locality f11874.

Cibicides lobatus (d'Orbigny)
Plate 7, figure 9

Cibicides lobatus (d'Orbigny). Bandy, 1944, Jour. Paleontology, v. 18, no. 4, p. 374, pl. 62, fig. 1.

Planoconvex, highly compressed specimens compare well with Bandy's description and illustrations of Cibicides lobatus (d'Orbigny) from beds of Eocene age at Cape Blanco, Oreg. In the northern Olympic Peninsula, C. lobatus occurs in beds of Eocene age in the lower part of the Twin River formation and in the Crescent formation.

Figured specimen (USNM 627021) from USGS locality f11882.

Cibicides martinezensis malloryi Smith
Plate 7, figure 11

Cibicides martinezensis malloryi Smith, 1957, California Univ. Pub. Geol. Sci., v. 32, no.3, p. 193, pl. 31, fig. 7.

The present specimens display high convexity of the ventral side and low convexity of the dorsal side; they have a coarsely perforate surface, and the early whorls are obscured on the dorsal side. These features are characteristic of Cibicides martinezensis malloryi. In the northern Olympic Peninsula this form makes one appearance in beds of Refugian age but all other occurrences are in rocks of late Eocene age in the lower part of the Twin River formation and the Aldwell formation. C. martinezensis malloryi was described from the Alhambra formation of California (Smith, 1957). Specimens similar to this form have also been observed by the writer from both the Umpqua and Tyee formations of Oregon.

Figured specimen (USNM 627022) from USGS locality f11799.