New Occurrences of Fortipecten Hallae (Dall, 1921) (Mollusca, Bivalvia) in the Pliocene of the North Pacific

Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171 www.elsevier.com/locate/palaeo

New occurrences of Fortipecten hallae (Dall, 1921) (Mollusca, Bivalvia) in the Pliocene of the North Pacific

Konstantin B. Barinova, Anton E. Oleinikb,T, Louie Marincovich Jr.c

aRussian Academy of Sciences, Geological Institute, Pyzhevsky per. 7, Moscow, Russia 109017 bFlorida Atlantic University, Department of Geography and Geology, United States cDepartment of Invertebrate Zoology and Geology, California Academy of Sciences, 875 Howard Street, San Francisco, CA 94103, United States Received 25 August 2004; received in revised form 22 March 2005; accepted 31 March 2005

Abstract

The large North Pacific bivalve mollusk index-fossil Fortipecten hallae (Dall, 1921) is present in a well-dated stratigraphic section of the Milky River Formation, Alaska Peninsula, southwestern Alaska. Co-occurring marine diatoms belong to the upper part of the subzone B of the Neodenticula kamtschatica diatom zone of the North Pacific diatom chronostratigraphy, with an age range of 4.8–5.1 Ma (early Pliocene). Based on coeval occurrences in northeastern Kamchatka, Russia, and synchronous changes in the two molluscan assemblages, F. hallae is a useful indicator of early Pliocene climatic warming along the high- latitude North Pacific margin. D 2005 Elsevier B.V. All rights reserved.

Keywords: Neogene; North Pacific; Stratigraphy; Fortipecten; Early Pliocene

1. Introduction known in the North Pacific (Table 1)(Kafanov, 1986; Barinov, 2001; Nakashima, 2002). Three of these The pectinid bivalve mollusk Fortipecten (Yabe species, F. takahashii (Yokoyama, 1930), F. kenyosh- and Hatai, 1940), with a thick shell resistant to iensis Chinzei, 1960, and F. hallae Dall, 1921, have abrasion and breakage, and its wide geographic the widest biogeographic distribution in circum-North distribution (northern Japan to Alaska) is a well- Pacific Neogene faunas. Of these three, F. takahashii recognized Neogene shallow-marine index fossil in and F. kenyoshiensis have been found in Honshu, the North Pacific. Eight species of Fortipecten are Hokkaido, Sakhalin, and Kamchatka (northwestern Pacific). The third species, F. hallae, is the one species that occurs in both Kamchatka and Alaska T Corresponding author. E-mail addresses: [email protected] (A.E. Oleinik), (Fig. 1). [email protected] (K.B. Barinov), Fortipecten hallae has been found in Pliocene [email protected] (L. Marincovich). deposits of Karaginskiy Island (northeastern Kam-

Table 1 Presently known valid species of Fortipecten, their type localities, and distribution in the North Pacific Species of the genus Fortipecten Type locality and age Distribution in the (Yabe and Hatai, 1940) North Pacific F. Hallae (Dall, 1921) One mile from the Delta of Solomon River, Nome Region, Seward Alaska and northeastern Peninsula, Alaska, bSubmarine BeachQ, Beringian beds, upper Pliocene Kamchatka F. takahashii (Yokoyama, 1930) Southeastern Sakhalin, Makarov district, vicinity of Tumanovo, Honshu, Hokkaido, Sakhalin, Maruyama formation, lower Pliocene and Kamchatka F. mironovi (Khomenko, 1934) To the North of the mouth of Vengeri River, Schmidt Peninsula, Northern Sakhalin northern Sakhalin, Pomyrskaya Formation, lower Pliocene F. sachalinensis (Ilyina, 1954) Pobedinka (Koton) River, Poronaisk Region, southern Sakhalin, Southern Sakhalin, Maruyama Formation, lower Pliocene western Kamchatka(?) F. kenyoshiensis Chinzei, 1960 0.5 km to the West of Kenyoshi, Nagawa, Sannohe distict, Aomori Honshu, western Kamchatka, Prefecture, northern Honshu, Togawa Formation, lower Pliocene Sakhalin(?) F. makarovi L. Gornaya river, Makarov Region, southeastern Sakhalin, Maruyama Southeastern Sakhalin Krishtofovich, 1964 Formation, lower Pliocene F. kuroishienesis Vicinity of the Karasuzawa dam on the Nakano River, Kuroishi, Aomori Honshu Kotaka and Noda, 1967 Prefecture, northern Honshu, Ogawara Formation, middle Miocene F. maruyamensis Barinov, 2001 Southeastern Sakhalin, Makarov district, Kormovaya River, lower Southeastern Sakhalin member of the Maruyama Formation, upper Miocene chatka) (Gladenkov, 1972; Sinelnikova, 1975; disagreement about the exact age of F. hallae Basilyan et al., 1991; Gladenkov et al., 1992), western occurrences (MacNeil, 1967) in Alaska. Hopkins Alaska (the Solomon and Kivalina areas) (Hopkins (1967) conditionally assigned F. hallae to faunal and MacNeil, 1960; MacNeil et al., 1943; MacNeil, assemblages of the bBeringian transgression.Q The 1967), and northern Alaska (lower Colville River) stratotype of these deposits was cited by MacNeil et (Marincovich and Powell, 1991)(Fig. 1). Until al. (1943) as a submarine (i.e., buried) beach deposit recently, only the northeastern Kamchatka occurrence on the Seward Peninsula near Nome, northwestern of F. hallae (in the lower part of the Limimtevayam- Alaska but they did report occurrence of F. hallae skaya Formation on the Karaginskiy Island) had been there as buncertainQ. The occurrence of F. hallae has dated from independent evidence (diatoms and been confirmed for two localities in northwestern paleomagnetic data), as early Pliocene (Basilyan et Alaska: (1) near Solomon village, and (2) along the al., 1991; Gladenkov et al., 1991, 1992). There was coast of Kotzebue Sound near Kivalina village (Hopkins and MacNeil, 1960; MacNeil, 1967)(Fig. 1). We refer to these two localities as Solomon and Kivalina, respectively. Hopkins (1967) assigned deposits at Kivalina and Solomon (Fig. 1) to the late Pliocene Beringian transgression, based on their molluscan faunal composition and stratigraphic relationships. Deposits at the Nome (stratotype) and Solomon localities are subsurface beach deposits and overlie Mesozoic basement rocks hypsometrically below present-day sea level. F. hallae is abundant at Solomon, but the molluscan assemblage there (Fig. 1) has no other species in common with Nome (MacNeil, 1967). At Kivalina, in contrast, F. hallae co-occurs with several mollusk species that also are found at Nome (Hopkins and MacNeil, 1960). MacNeil (1967) Fig. 1. Fortipecten hallae localities in the North Pacific mentioned observed that thick-shelled fragments of F. hallae at in the text. Kivalina were more worn than co-occurring thin- 164 K.B. Barinov et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171 shelled bivalves, and inferred that F. hallae could 2. Geologic setting have been reworked from deposits of greater age. The exact geographic and stratigraphic placement The specimens of F. hallae that are the focus of this of F. hallae localities have not always been accurately study come from the Sandy Ridge stratigraphic sec- known. For example, MacNeil et al. (1943) cited one tion of the Milky River Formation (Figs. 1-3: 2–4; locality as: bBuried Pliocene beach, 20 feet below Fig. 4: 2–3). The geological setting, a general strati- surface, near Solomon River, Nome District, Alaska, graphic description of this section, and a geological Collector, Otto HallaQ. According to Dr. P.S. Smith, map of the Sandy Ridge area are given in Marinco- Chief Alaskan Geologist, bOtto Halla was a miner vich et al. (2002) and Gladenkov et al. (2002). The who mainly worked near Nome in deposits of Sandy Ridge section consists entirely of shallow- submarine (i.e., buried) beaches and not on Solomon marine sediments with abundant fossils, which make RiverQ (MacNeil et al., 1943). This information it the only known Milky River Formation section that suggests that evidence for bin situQ occurrences of is not largely of non-marine aspect. Our measured the F. hallae in Beringian transgression deposits is stratigraphic section of the Milky River Formation at ambiguous at best. However, several specimens of F. Sandy Ridge consists of 276 m of shallow-marine hallae that we collected from the Milky River sediments. These marine beds are inferred to be Formation, on the distal part of the Alaska Peninsula, overlain by approximately 200 m of non-marine southwestern Alaska, at 56870V N 159892V W(Fig. 1), volcaniclastic sediments and basalt flows that crop shed new light on the geographic occurrences and age out to the west along Sandy Ridge and are identical to of F. hallae. nonmarine lithologies elsewhere in the Milky River

Fig. 2. Measured stratigraphic section of the Milky River Formation at Sandy Ridge, with plotted occurrences of F. hallae, A.(T.) borealis and available numeric ages. K.B. Barinov et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171 165

Fig. 3. Fortipecten hallae (Dall, 1921): 1,5—Specimen GIN 8719/2, NE Kamchatka, Karaginskiy Island, lower part of the Limimtevayamskaya Formation. 1—right valveÂ0.7; 5—side viewÂ0.7; 2–4—right valves: 2—Specimen CAS LM16/1, latex cast, Alaska Peninsula, Sandy Ridge, Â0.9; 3—Specimen CAS LM16/2, latex cast, Alaska Peninsula, Sandy Ridge Â0.8; 4—Specimen CAS LM46/1, latex cast, Alaska Peninsula, Sandy Ridge Â0.8. 166 K.B. Barinov et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171

Fig. 4. Fortipecten hallae (Dall, 1921) left valves: 1— Specimen GIN 8731/83, NE Kamchatka, Karaginskiy Island, base of the upper part of the Limimtevayamskaya Formation Â0.9; 2—Specimen CAS LM46/2, latex cast, Alaska Peninsula, Sandy RidgeÂ0.9; 3—Specimen CAS LM16/3, Alaska Peninsula, Sandy Ridge Â0.8; 4—Specimen GIN 8719/2, NE Kamchatka, Karaginskiy Island, lower part of Limimtevayamskaya Formation Â0.6. Abbreviations: GIN—Geological Institute of the Russian Academy of Sciences, Moscow, Russia; CAS—California Academy of Sciences, San Francisco, CA. K.B. Barinov et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171 167

Formation (Lyle et al., 1979; Detterman et al., 1996). ciliatum, Clinocardium pristinum, Cyclocardia kamt- The Sandy Ridge marine beds lie with profound schatica (Slodkevitsch, 1938), Diplodonta aleutica angular unconformity upon a folded terrestrial Dall, 1901, Macoma calcarea, Macoma obliqua sequence of inferred middle Miocene age (Marinco- (Sowerby, 1812), Musculus niger, Mya truncata, vich et al., 2002; Gladenkov et al., 2002). Pandora (Pandorella) wardiana, Panomya norveg- The marine portion of the Sandy Ridge beds ica, Serripes groenlandicus, Siliqua alta (Broderip consists of two lithologically distinct members (Fig. and Sowerby, 1829) and Yoldia (Cnesterium) semi- 2). The lower member, with the exception of a 3.5-m- nuda, plus the gastropod Neptunea lyrata altispira. thick basal conglomerate, is represented by 112 m of Mollusk specimens are usually localized within thin fine-grained grey sandstone interbedded with thinner horizons and lenses. Massive sandstone and conglom- (0.7–1 m) layers of coarser-grained pebbly sandstone. erate beds contain abundant molds and casts of Mya Strata also contain several thin (up to 0.1 m thick) ash truncata. The upper 111 m of the upper member of and gravel beds and elongate concretions up to 0.5 m the marine facies at Sandy Ridge consists of medium- long. Smaller concretions often merge into concre- to coarse-grained, poorly lithified, dark gray, tuffa- tionary horizons up to 0.4 m thick. Floating pebbles ceous sandstones with a 0.3-m basal conglomerate are scattered throughout these marine strata. The separated from underlying beds by an erosional molluscan assemblage of the lower member include contact. Portions of the sandstone beds are biotur- the bivalves Acila (Truncacila) empirensis Howe, bated. The sandstone includes layers of darker-gray, 1922, Astarte (Tridonta) borealis (Schumacher, poorly sorted gravel and conglomerate (from 0.1 to 15 1817), Ciliatocardium ex gr. ciliatum (Fabricius, m thick), and the degree of lithification decreases, and 1780), Clinocardium pristinum Keen, 1954, Macoma grain size increases, up-section. These strata contain calcarea (Gmelin, 1791), Musculus niger (Gray, the following molluscan assemblage: the bivalves 1824), Mya truncata Linnaeus, 1758, Pandora Ciliatocardium ciliatum, Clinocardium nuttallii (Con- (Pandorella) wardiana A. Adams, 1860, Panomya rad, 1837), Fortipecten hallae (Figs. 3 —2–4 and 4 — norvegica Spengler, 1793, Serripes (Serripes) groen- 2–3), Macoma calcarea, Mizuhopecten sp., Mya landicus (Mohr, 1786), Spisula voyi (Gabb, 1866) and truncata, Peronidia lutea (Wood, 1828), Pododesmus Yoldia (Cnesterium) seminuda Dall, 1871, plus the macroshisma (Deshayes, 1839) and Protothaca stam- gastropods Beringius hertleini MacNeil, 1970, Bor- inea (Conrad, 1837), plus the gastropod Neptunea eotrophon beringi Dall, 1902, Buccinum glaciale lyrata altispira. (Linne, 1761), B. polium polium (Dall, 1907), Colus The lower member and lower 50 m of the upper (Latisipho) aurantius (Dall, 1925), Clinopegma uni- member, of the studied stratigraphic section, are cum(Pilsbry, 1905), Cryptonatica clausa (Broderip characterized by the same boreal molluscan assem- and Sowerby, 1829), Neptunea lyrata altispira (Gabb, blage. All genera and some of the extant species in 1869), Obesotoma solida (Dall, 1886)andVolutop- this assemblage inhabit the upper-subtidal zone in the sius middendorffi (Dall, 1891). Bering Sea and the Sea of Okhotsk today, being most The upper member of the Sandy Ridge section abundant at depths from 5 to 75 m (Scarlato, 1981; consists of 161 m of massive, mostly tuffaceous Kuznetsov, 1963; Coan et al., 2000). Mollusks in the sandstones, gravels, and conglomerates (Fig. 3). The lower part of the section are preserved with shell lower 50 m of this upper member consists of mostly intact and in living position. Disarticulated interbedded medium-grained dark-gray to yellowish- valves and shell fragments dominate preservation in gray tuffaceous sandstone (layers 1.2–15 m thick) and the basal 50 m of the upper member. A change in the massive, dark-gray to greenish-gray, occasionally preservation and orientation of mollusk shells implies cross-bedded sandstone (layers 1–10 m thick) with a change in depositional environment from relatively pebble, gravel, and conglomerate horizons. These quiet in the lower member, to more hydrodynamically massive sandstones form distinctive vertical cliffs in active at the beginning of the upper member part (Fig. the slope. The tuffaceous sandstone contains abundant 2). The geology, localities and age of Kamchatka mollusks, including Acila (Truncacila) empirensis, localities were described in detail by Gladenkov et al. Astarte (Tridonta) borealis, Ciliatocardium ex gr. (1992). Specimens of F. hallae from the Limimte- 168 K.B. Barinov et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 223 (2005) 162–171 vayamskaya Formation of the Karaginskiy Island, al., 2002; Gladenkov, 2003). The potassium–argon northeastern Kamchatka, are figured for comparative age of a basalt flow in the uppermost part of the Milky purpose (Fig. 3 —1, 5 and Fig. 4 —1, 4). River Formation at its nearby type locality is 3.87F0.06–3.53F0.27 Ma (Fig. 2)(Detterman et al., 1996; Wilson et al., 1981). This age assignment 3. Discussion supports the suggestion of MacNeil (1967) that beds with F. hallae at the Solomon locality could have been Fossil large pectinids from the North Pacific older than the submarine beach deposits at Nome. margin have long been considered as biogeographic The age of F. hallae in the Milky River Formation and paleoclimatic indicators. Two species of large is similar to its age in the lower part of the pectinids are now known from the vicinity of the Limimtevayamskaya Formation on Karaginskiy Sandy Ridge locality—F. hallae and Mizuhopecten Island (northeastern Kamchatka) (Fig. 1), based on mollerensis (MacNeil, 1967). Specimens from Sandy paleomagnetic and diatom data that imply an age Ridge are identified as F. hallae using the features of range of 4.5–4.1 Ma (Basilyan et al., 1991; Gladenkov surface sculpture described in detail by MacNeil et al., 1991, 1992). Using latest data and scale of (1967) and Masuda (1978). We have found a shell Berggren et al. (1995), shifts this interval to 5.0–4.3 fragment of Mizuhopecten sp. co-occurring with F. Ma. These age data suggest that F. hallae first hallae in the Sandy Ridge section. However poor appeared in the Bering Sea region in the early preservation of the fragment precludes species iden- Pliocene. The appearance of F. hallae in Alaska, tification. It should also be noted that the age of together with two other species—F. takahashii, and F. occurrence for M. mollerensis is not known. We made kenyoshiensis in western Kamchatka (Sinelnikova, a dedicated attempt during field work on the Alaska 1975), suggest that the genus Fortipecten had Peninsula in 1999 to find its type locality, but we were originated in the northern Japan and Sakhalin Island unsuccessful. This locality may have been eroded and then migrated to the high-latitude North Pacific in away, or may have been covered by the very dense the early Pliocene. The spread of F. hallae in the high- vegetation there. latitude North Pacific coincided with the onset of a The lower member of the marine facies of the relatively warm marine climate in the Bering, Beau- Milky River Formation at Sandy Ridge contains the fort, and Chukchi seas during the early Pliocene. oldest Cenozoic occurrences in the North Pacific of Oxygen isotope values from Cyclocardia and the bivalve Astarte (Marincovich and Gladenkov, Macoma co-occurring with F. hallae in the Limimte- 1999; Marincovich et al., 2002). This occurrence vayamaskaya Formation of Karaginskiy Island sug- correlates with subzone b of the Neodenticula gest a rise in the water temperature of approximately kamchatica diatom zone of Barron and Gladenkov 3.2–4.5 8C in comparison with older deposits imme- (1995), which has an age range of 5.5–4.8 Ma diately below (Barinov and Kiyashko, 1997). The (Marincovich and Gladenkov, 1999, 2001). This methodology and discussion of the y18O values for the occurrence of Astarte was later refined to 5.5–5.4 early Pliocene mollusks of Karaginskiy Island are Ma, based on a diatom assemblage from the lower- given in Gladenkov et al. (1992). Comparable isotopic most occurrence of Astarte in the section (28 m above data from the Milky River Formation do not exist, due the base of the section) (Fig. 2)(Gladenkov et al., to shell recrystallization. The appearance of F. hallae 2002; Gladenkov, 2003), which implies that the in both Kamchatka and Alaska was accompanied by a accumulation of the lower part of the marine member conspicuous change in the molluscan assemblage. In of the Milky River Formation took place at the very both regions, this biostratigraphic interval is marked end of the Late Miocene—beginning of the Early by the appearance of mollusks indicative of warmer Pliocene. The upper part of the Milky River For- water conditions than those usually encountered at mation at Sandy Ridge, containing remains of F. these latitudes today. This change in the molluscan hallae, based on the first appearance and disappear- assemblage in the Milky River Formation was ance of the indicative North Pacific diatom species, is observed between the lower 50 m and upper 111 m assigned to the interval of 5.1–4.8 Ma (Gladenkov et of the upper part of the marine unit. This stratigraphic K.B. 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