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Ecomorphological adaptation in three mudskippers (Teleostei: Gobioidei: Gobiidae) from the Persian Gulf and the Gulf of Oman (Hydrobiologia) Gianluca Polgar*, Mehdi Ghanbarifardi, Salvatore Milli, Ainhoa Agorreta, Mansour Aliabadian, Hamid Reza Esmaeili, Tsung Fei Khang *corresponding author: Universiti Brunei Darussalam, Faculty of Science, Environmental and Life Sciences Programme, Jalan Tungku Link BE1410, Brunei Darussalam; [email protected] Online Supplementary Information (Online Resources): supplementary text Supplementary text S1: study sites, sedimentological and geomorphological overview The Persian Gulf is a shallow, semi-enclosed marginal sea situated among the Arabian Peninsula in the west, the Taurus Mountains in the north, and the Zagros Mountains in the east and northeast. It is connected with the Gulf of Oman and the Indian Ocean through the Strait of Hormuz, and extends for about 1000 km in a NW-SE direction, having a width varying from a minimum of 56 km near the Strait of Hormuz to a maximum of 338 km (Fig. 1). Its coastal topography is mountainous along the east coast, and flat along the west coast. This is also reflected in its bathymetry, with a shallow bank area < 20 m deep in the southwestern sector, and a 40-80 m deep trough in the eastern sector, extending in a northwest direction along the east coast (Fig. 1). Beyond the Strait of Hormuz, the sea bottom drops quickly to > 2000 m into the Gulf of Oman (Fig. 1). The Persian Gulf shows a great spatial variation in salinity and temperature due to its arid climate (Clarke & Keij, 1973; Reynolds, 1993). The surface winds in the Gulf are prevailingly westerly or north-westerly throughout the year. These winds generate wave and related longshore currents propagating along the east coast where barrier islands and spits are developed. The surface winds in the Gulf of Oman are influenced by the Indian monsoon system, which seasonally reverses between northwesterly in winter (October-May) and south-easterly in summer (June-September). Water circulation in the Gulf basin is strongly influenced by its morphology and by high temperatures and evaporation rates. Generally, due to high evaporation rate, surface waters are denser in the northern sectors of the Gulf where they sink to the bottom, flowing out through the Strait of Hormuz and spilling intermittently into the deeper and less dense waters of the Gulf of Oman. This outflow induces a surface inflow of less dense Indian Ocean waters through the Strait of Hormuz, 1 which is deflected along the east coast, forming a northward-directed cyclonic circulation and producing an inverseestuarine type water exchange (Rochford, 1964; Wyrtki, 1973; Reynolds, 1993; Bower et al., 2000; Prasad et al., 2001; Swift & Bower, 2003). The Persian Gulf has an oscillation period of 21.6-27 hours for tidal waves (Defant, 1961). This produces semi-diurnal and diurnal tidal waves that generate resonant interactions in the basin, leading to a system of amphidromic points and maximum tidal excursions in the northern sector of the Gulf (up to 6 m during spring tides: data of Jan 2014; National Cartographic Center, Hydrographic and Tidal Department, Teheran, http://www.ncc.org.ir/; Online Resource Tab. S2). This peculiar water circulation and the arid climate determine high salinity conditions (~ 40 ppt), which are associated with impoverished Indo-Pacific marine communities (Purser, 1973). Supplementary text S2: sediment analysis. Sediment samples were oven-dried at 100°C for 24 hours to constant weight, and subsamples of 500 g were analysed for grain size. Sieve analysis was performed with a set of 11 sieves (mesh size: 24.4, 19.1, 12.7, 9.53, 4.76, 2.38, 1.19, 0.594, 0.297, 0.150, and 0.074 mm). The percent difference between the total weight of the sieved materials and the initial weight of each sample was 0.2-0.8%. Subsamples (50 g) of all the passing fractions at 0.074 mm (#200 sieve) were analysed with ASTM 152H soil hydrometers. Measurements were taken at fixed time intervals (1, 2, 4, 8, 16, 30, 60, 120, 240, 480, and 1440 min) applying temperature, zero and meniscus corrections, and assuming a conventional specific gravity of soil particles (Gs) = 2.7 (ASTM 2014a,b). Sediment grain-size curves (passing fractions) were plotted, and coefficients of curvature (Cc) and of uniformity (Cu) were calculated for sands (Holtz & Kovacs, 1981). Particle-size retained fractions were then classified following the USCS scale (Unified Soil Classification System; Holtz & Kovacs, 1981; Online Resource Tab. S3), and samples classified plotting them on the ternary grain-size diagram of Shepard (1954, modified by Schlee, 1973) built with SEDPLOT (Poppe & Eliason, 2008). Supplementary text S3: literature of supplementary material. Agorreta A, Rüber L. 2012. A standardized reanalysis of molecular phylogenetic hypotheses of Gobioidei. Systematics and Biodiversity 10: 375−390. 2 Agorreta A, San Mauro D, Schliewen U, Van Tassell JL, Kovačić M, Zardoya R, Rüber L. 2013. Molecular phylogenetics of Gobioidei and phylogenetic placement of European gobies. Molecular Phylogenetics and Evolution 69: 619−633. ASTM (The American Society for Testing and Materials) (2014a) D422-63: standard test method for particle-size analysis of soils. ASTM International, West Conshohocken. Available from http://www.astm.org. Accessed September 2015 ASTM (The American Society for Testing and Materials) (2014b) E100-14: standard specification for ASTM hydrometers. ASTM International, West Conshohocken. Available from http://www.astm.org. Accessed September 2015 Bower AS, Hunt HD, Price JF. 2000. Character and dynamics of the Red Sea and Persian Gulf outflows. Journal of Geophysical Research 105: 6387-6414. doi:10.1029/1999JC900297 Chakrabarty P, Davis MP, Sparks JS. 2012. The first record of a trans-oceanic sister-group relationship between obligate vertebrate troglobites. PLoS ONE 7 e44083. Clarke MWH, Keij AJ. 1973 Organisms as producers of carbonate sediment and indicators of environment in the southern Persian Gulf. Pp 33-56 in: Purser BH, ed., The Persian Gulf: Holocene carbonate sedimentation and diagenesis in a shallow epicontinental sea. Berlin, Heidelberg, New York: Springer-Verlag. Defant A. 1961. Physical oceanography, vol. 2. London: Pergamon Press. Dupin L. 2011. Mapping the landform assemblages and archaeological record of the Lower Khuzestan plan (SW Iran) using remote-sensing and GIS techniques. Pp 53-68 in: Brown AG, Basell SL, Butzer KW, eds., Geoarchaeology, climate change, and sustainability. Geological Society of America, Special paper 476. doi: 10.1130/2011.2476(05). Holtz RD, Kovacs WD. 1981. An introduction to geotechnical engineering. Englewood Cliffs: Prentice-Hall. Hubbs CL, Lagler KF. 2004. Fishes of the Great Lakes region. Revised edition. Ann Arbor: The University of Michigan Press. Murdy EO. 1989. A taxonomic revision and cladistic analysis of the oxudercine gobies (Gobiidae: Oxudercinae). Records of the Australian Museum Suppl. 11: 1–93. Polgar G, Sacchetti A, Galli P. 2010. Differentiation and adaptive radiation of amphibious gobies (Gobiidae: Oxudercinae) in semi-terrestrial habitats. Journal of Fish Biology 77: 1645–1664. 3 Poppe LJ, Eliason AH. 2008. A Visual Basic program to plot sediment grain-size data on ternary diagrams. Computers & Geosciences 34: 561-565. doi: 10.1016/j.cageo.2007.03.019 Prasad TG, Ikeda M, Kumar SP. 2001. Seasonal spreading of the Persian Gulf water mass in the Arabian Sea. Journal of Geophysical Research, 106: 17,059-17,073. doi: 10.1029/2000JC000480 Purser BH. (ed) 1973. The Persian Gulf: Holocene carbonate sedimentation and diagenesis in a shallow epicontinental sea. Berlin, Heidelberg, New York: Springer-Verlag. Reynolds RM. 1993. Physical oceanography of the Gulf, Strait of Hormuz, and the Gulf of Oman. Results from the Mt Mitchell expedition. Marine Pollution Bulletin 27: 35-59. doi:10.1016/0025-326X(93)90007-7 Rochford DJ. 1964. Salinity maxima in the upper 1000 metres of the north Indian Ocean. Australian Journal of Marine and Freshwater Research 15: 1-24. doi:10.1071/MF9640001 Schlee JS. 1973. Atlantic continental shelf and slope of the United States. Sediment texture of the northeastern part. US Geological Survey Professional Paper 529-L, Washington: United States Government Printing Office. Shepard FP. 1954. Nomenclature based on sand-silt-clay ratios. Journal of Sedimentary Research 24: 151-158. doi: 10.1306/D4269774-2B26-11D7-8648000102C1865D Swift SA, Bower AS. 2003. Formation and circulation of dense water in the Persian/Arabian Gulf. Journal of Geophysical Research 108(C1), 3004. doi:10.1029/2002JC001360 Thacker CE. 2009. Phylogeny of Gobioidei and placement within Acanthomorpha, with a new classification and investigation of diversification and character evolution. Copeia 2009: 93–104. Wyrtki K. 1973. Physical oceanography of the Indian Ocean. Pp 18-36 in: Zeitzschel B, Gerlach SA, eds., The biology of the Indian Ocean. Vol. 3. Berlin, Heidelberg: Springer. 4