1 Outcrops of the Early Devonian Campbellton Formation occur along the Bay of Chaleur-Restigouche River shoreline from Atholville east to Dalhousie, New Brunswick, Canada. The Campbellton Formation overlies the Val d’Amour Formation rhyolite dated at 407.4 ± 0.8 Ma (Wilson et al. 2004). Miospores in the Campbellton Formation place it in the Emphanisporites annulatus-Camarozonotriletes sextantii Assemblage Zone which corresponds approximately to the Polygnathus dehiscens to Polygnathus serotinus conodont zones of early Emsian to early late Emsian age (Richardson and McGregor 1986). The terminal date for the Emsian is 397.5 ± 2.7 Ma (Ogg et al. 2008).

2 The western exposure of the Campbellton Formation was referred to as the “Atholville Beds” by Dineley and Williams (1968), and these beds are known for their well-preserved vertebrate fauna (Young 1983; Miller et al. 2003; Turner and Miller 2008; Burrow et al. 2008), first described by Whiteaves (1881). Among the fossils Whiteaves described were eurypterids. New discoveries of both vertebrates and arthropods from the “Atholville Beds”, beginning in the 1990s, resulted in a redescription of the eurypterid fauna (Miller 2007a, b) and assignment of all known specimens to Pterygotus anglicus Agassiz 1844, the large pterygotid first described from Scotland. Recent work to re-examine the paleoenvironment of the Campbellton Formation (Kennedy and Gibling 2011, and references therein) has resulted in the “Atholville Beds” being attributed to a coastal deltaic setting, with a marine influence, as demonstrated by rare occurrences of prasinophytes (tasmanitids) and acritarchs (Blieck and Cloutier 2000).

3 Farther east along the coast, outcrops near Maple Green, Point La Nim and Pin Sec Point comprise the classic plant-rich beds of the Campbellton Formation, including the second oldest evidence of wood (Gerrienne et al. 2011). These beds were described as representing a mix of wetland, alluvial-plain and lacustrine environments (Kennedy and Gibling 2011) and, in addition to plants, have yielded the oldest land animal assemblage in North America, including scorpion and arthropleurid fossils (Shear et al. 1996) and millipede fossils (Wilson 2006). A single abdominal eurypterid fragment was found in these beds in 1997, just east of Point La Nim, from a hard, grey siltstone unit approximately 1.6 m from beach level (Fig. 1). We describe the eurypterid fragment here as cf. Parahughmilleria.

4 Fractures in the bedding, overhanging trees, and the steep dip create an unstable cliff face and make fossil exploration difficult. Repeated searches have uncovered no additional material. The eurypterid bed occurs at a level 14 m above the base of section III in the marginal lacustrine facies association described by Kennedy and Gibling (2011). The outcrop consists of thick beds of horizontally stratified granule–pebble conglomerate, sharply overlain by massive to graded beds of grey siltstone. These in turn transition upwards to graded beds of red medium–coarse sandstone with lenses of granule conglomerate, and are overlain by pebble–cobble conglomerate. Resedimented volcanic material predominates within these strata, likely derived from nearby sources flanking the basin. The specimen is found within the grey siltstone unit, which is about 1 m thick and characterized by beds with centimetre-scale grading and organic-rich laminae, locally scoured below layers of coarse sandstone or granule conglomerate. Organic material is commonly found within this unit as well as in the overlying red sandstone, and includes fragments of Prototaxites and plant fragments up to 30 cm long. Although plant debris is common throughout the section, particularly plant-rich strata are found approximately 11 m below and 8 m above the cf. Parahughmilleria horizon. Collectively, plant taxa include Drepanophycus spinaeformis, Drepanophycus gaspianus, Zosterophyllum divaricatum, Sawdonia acanthotheca, Taeniocrada sp., and Spongiophyton minutissimum (Gensel et al. 1975; Gensel 1982; Gensel et al. 1991; P. Gensel personal communication 2010). The strata are interpreted as the result of underwater density flows that occurred during high-discharge flood events that carried plant material and volcanic sediment surrounding the lake into the marginal lake basin. Such flows would have rapidly buried any organisms inhabiting lacustrine waters.

5 MATERIAL : Specimen NBMG 11012 consists of a part and counterpart of an articulated partial preabdomen of the opisthosoma (Fig. 2). The specimen is reposited in the Palaeontology Collection of the New Brunswick Museum (NBMG).

6 LOCALITY AND STRATIGRAPHY: Point La Nim (48°03.97’N; 66°24.78’W), west of Dalhousie, New Brunswick. Camp-bellton Formation, Emsian (Early Devonian).

7 DESCRIPTION : As very little of the animal is preserved, the specimen is assigned to cf. Parahughmilleria based on similarities in size and preabdomen shape to known members of the genus. All dorsal tergites of the preabdomen are represented, numbered 1 to 7 (Fig. 3). Features suggestive of Parahughmilleria include the lanceolate shape of the pre-abdomen, the presumed overall size of the animal, the presence of a large epimera on tergite 7, and the ornamentation.

8 The total length of the preserved specimen is 57.7 mm. The maximum width of the specimen is 22.7 mm at tergite 4. Maximum tergite lengths are (2) 7.5 mm; (3) 6.7 mm; (4) 7.3 mm; (5) 8.8 mm; (6) 9.4 mm; (7) 9.8 mm. Tergites are incomplete and widths cannot be determined. A shallow depression visible on tergites 3 to 5 suggests a mid-line. On tergites 2 and 3 the depression appears to split, possibly as a result of deformation of the specimen; however, this split-like appearance may represent a subtle expression of the underlying genital appendage. Published descriptions of Parahughmilleria indicate that the opisthosoma is widest at tergite 3 (Braddy 2000; Størmer 1973). Although tergite 3 is incomplete on this specimen, tergite 4 can be measured to the presumed mid-line (14.5 mm). Based on the reconstructed body dimensions of Parahughmilleria major Størmer, 1973, the measurements suggest that the Camp-bellton Formation specimen may have been about 125 mm long, about the maximum size of Parahughmilleria major.

9 A large epimera is seen on the posterior of mesosomal segment 7, a feature of Parahughmilleria noted by Braddy (2000) and found on both Parahughmilleria hefteri Størmer 1973 and Parahughmilleria major, which may represent different life stages of a single species (Poschmann and Tetlie 2006). Dorsal tergites are flattened over the ventral sternites. On the left the sternites are partially visible and extend beyond the tergites, offset with ventral tergites 2(?) to 5.

10 The preabdomen is covered in lunules (Fig. 4), varying from a semi-lunar sculpture on the proximal half of each tergite to a pointed (v-shaped) sculpture on the distal half of each tergite. Størmer (1973) described the crescentic to triangular ornamentation of importance in the taxonomy of the Hughmilleriidae, a family grouping that previously included Parahughmilleria and briefly described the ornament of Parahughmilleria hefteri and Parahughmilleria major.

11 REMARKS : The calculated body length of specimens of Pterygotus anglicus from the Campbellton Formation ranges from about 40 cm to about 170 cm (Miller 2007a, b). All of those specimens possess only a rounded semi-lunar sculpture, suggesting that the specimen described here as cf. Parahughmilleria is not likely a juvenile Pterygotus anglicus.

12 After 130 years of study focussed mainly on its fossil content, the remarkable window into an Early Devonian ecosystem thus revealed in the Campbellton Formation is now supported by a published record of the stratigraphy and synthesis of the paleoenvironment (Kennedy and Gibling 2011). The specimen described here as cf. Parahughmilleria provides an addition to the eurypterid fauna, previously represented only by Pterygotus.

13 Specimens of the genus Parahughmilleria have been described from numerous Early Devonian sites, in paleo-environments ranging from shallow marine to freshwater (Tetlie and Poschmann 2008). In the Emsian of Alken an der Mosel, Germany (Størmer 1973), the paleoenvironment was described as marine to brackish (Poschmann and Tetlie 2006). In contrast, in the Emsian at Willwerath, also in the Rhenish Slate Mountains of Germany, Parahughmilleria lived in a shallow, brackish or freshwater terrestrial setting in a deltaic transitional facies, possibly a floodplain lake or interdistributary lagoon (Poschmann and Tetlie 2006). In the Midland Valley of Scotland, the paleoenvironment is described as both fluvial and lacustrine, associated with “Lake Forfar” (Braddy 2000). In Scotland, both pterygotids and hughmillerids are believed to have inhabited lacustrine environments, while stylonurid eurypterids inhabited flu-vial environments. At the Devonian Trout Valley locality in Maine, USA, where a plant assemblage similar to the Camp-bellton Formation is known, Selover et al. (2005) described a juvenile eurypterid identified as cf. Parahughmilleria that was probably part of an estuarine assemblage.

14 Miller (2007a) discussed the Campbellton Formation pterygotid fauna as inhabiting estuarine or lagoonal paleoenvironments. Sizes of individuals suggested that juveniles and adults comprised the assemblage. Estuaries and lagoons may have been nurseries and the widely reported habitat of Pterygotus anglicus ranging from marine to freshwater, was perhaps dependent on stages of life history. The paleo- environment for the specimen described herein, in a marginal lacustrine facies, is consistent with the setting described for Parahughmilleria from other Early Devonian sites. The two outcrop belts of the Campbellton Formation that have yielded eurypterids were interpreted as having been deposited in western and eastern sub-basins by Kennedy and Gibling (2011), possibly separated by a topographic barrier. In both sub-basins, sparse eurypterid material has been found at low stratigraphic levels in the formation, within a few tens of metres of the basal contact with the Val d’Amour Formation. However, the western sub-basin, which has marine indicators, has yielded pterygotid remains, whereas the eastern, lacustrine sub-basin has yielded cf. Parahughmilleria remains. Although too few specimens are available for a robust interpretation, it is possible that these occurrences provide an indication of paleoenvironmental tolerances, at least at this level in the Campbellton Formation.