Sagami Bay is a plate subduction zone along the Sagami Trough in Japan. It is an active tectonic area (Figure 1). Earthquake activity is very high in the western part of Sagami Bay, east of the Izu Peninsula. Submarine volcanoes have erupted repeatedly. For example, Teishi Knoll erupted in 1989 (Figure 1). Moreover, biological research has been conducted in this area and individual biological colonies have been discovered.

For multidisciplinary observation to monitor geophysical and biological phenomena, the Japan Agency for Marine–Earth Science and Technology (JAMSTEC) planned to construct a submarine observatory at a depth of 1,175 m about 7 km off Hatsushima Island in Sagami bay. The original observatory system was deployed and set up in 1993 [1]. This observatory had a seismometer, hydrophone, thermometer, a conductivity, temperature, and depth instrumentation (CTD), video camera, and an electromagnetic current meter. However, it had no submarine external port. Use of the original system was halted in 1999 because of a submarine cable fault; it was recovered in 2000. The system was completely renovated in 2000 for carrying out more multi-disciplinary observations with various other sensors, and for development of a more expandable system with underwater mateable connectors, aside from the reason that the primary observatory had broken [2]. Figure 2 (a) portrays a photograph of the renovated underwater observatory system (35.003083N, 139.2247E).

The new system is equipped with a transmissometer, an Acoustic Doppler Current Profiler (ADCP), a tsunami pressure gauge (a precision pressure gauge), and a gamma ray spectrometer, as well as sensors of the same kind used in the previous configuration of the observatory. The performance of some of those sensors has since been improved. The A/D sampling of seismometer is 24 bits/200 Hz. One of the two video cameras is a High-gain Avalanche Rushing Photo conductor (SuperHARP) camera, which is far more sensitive than a typical CCD camera [3]. Table 1 presents specifications of the renovated Hatsushima system. It is remarkable that it has four underwater mateable connectors for additional observation instruments (Figure 2). Various data obtained on the sea floor have been sent to Yokohama Institute, JAMSTEC, through the Hatsushima land station, and stored on a data server. Registered users can preview the time series data using a web browser, and download data from the data center server (http://www.jamstec.go.jp/scdc/top_e.html). This web site has provided other observatory data: data of the off-Kushiro–Tokachi and off-Muroto cable observatories installed by JAMSTEC for real-time earthquake and tsunami disaster-prevention. The off-Kushiro–Tokachi system, which was detailed in an earlier report [4], observed various remarkable phenomena such as tsunami generation processes, turbidity current, etc. during the 2003 Tokachi-oki earthquake of M8 [5]. In this paper, we explain the operations by which we added some observation systems to the Hatsushima system. We also report some interesting data obtained using the observatory equipment when a large earthquake occurred.

During February 2005, we connected an ocean bottom electro-magnetometer (OBEM), an ocean bottom differential pressure gauge system (DPG) and an ocean bottom gravimeter (OBG) to the Real-Time Deep Sea Floor Observatory at 1175 m depth offshore of the Hatsushima Island in Sagami Bay using the Research Vessel “Natsushima” and the Remotely Operated Vehicle “Hyper-Dolphin” during the NT05-01 Cruise. We then initiated long-term, real-time observation tests on the ocean bottom (Figure 2). These instruments were laid out within a radius of about 10 m and were connected to underwater mateable connectors (Figure 3). Table 2 presents the specifications of each added measurement system.

Tokai University developed the OBEM system and performed tests in shallow sea [6]. This system comprises three components: (1) fluxgate magnetometer and inclinometer, (2) an electric potentiometer and (3) a main CPU unit. Electrical power is supplied from the observatory. The main CPU unit controls data measurements and communications. All sensors and electrical units are installed in pressure cases made of aluminum alloy mounted in an aluminum frame (Figure 2). This system can measure three magnetic field components, two horizontal electric field components and two inclinometer components (pitch and roll angle) with a sampling rate of 1, 2, 4 or 8 Hz. Figures 4 and 5 portray comparisons of magnetic field time series of the Hatsushima Observatory and the Kakioka geomagnetic observatory (36.2322N, 140.1864E). The coordinate system of magnetic measurement is rotated to true north. Figure 4 shows the monthly time variation during July 2005. The daily variations were observed very clearly; both time variations are very similar. The one-day variation on 21 July 2005 is presented in Figure 5. Our OBEM data include higher frequency variations than those presented in Kakioka's data.

We also installed a differential pressure gauge (DPG) system and an ocean bottom gravimeter (OBG) system. The DPG system is based on that described by Cox et al. [7] to monitor long-period pressure changes such as low-frequency earthquakes and teleseismic earthquakes. As a result of the system calibration, this sensor's response is smaller at frequencies lower than 0.059 Hz. Figure 6 portrays clear surface waves as well as P and S phases from a large earthquake offshore of Sumatra Island observed using this DPG in the seafloor observatory. The DPG system was recovered to improve the system performance. We reconnected the improved DPG system to the Hatsushima station in January 2008 again. The improved DPG system includes sensors such as a strong motion accelerometer and a quartz pressure gauge to expand its capability to monitor seismic and pressure signals.

An OBG system consists of a gravimeter (SB-3M; Scintrex Ltd.), a pressure meter (Paroscientific Inc.), a sealed backup battery, and a CPU module for communication and telemetry with each sensor and land station. The sensors, with gimbals and a communication unit, were enclosed in a titanium sphere. Watanabe et al. [8] reported that the OBG system has 0.07 mGal/day linear drift and the residual gravity data with linear drift removed shows very long-period fluctuation with amplitude of more than 2 mGal. The OBG system was recovered during the NT08-01 cruise. We will analyze those data.

A large earthquake (M5.4) occurred off-Izu Peninsula at 2:50:39 on 21 April 2006, generating a submarine landslide. The generated mudflow reached the station about five minutes after the seismic wave arrived. Kinoshita et al. [9] reported that some sensor positions were shifted by the mudflow; the SuperHARP camera took a movie of the mudflow at 2:55 (Figure 7). Figure 8 presents temperature and light transmission data before and after the earthquake occurrence. After the toe of the mudflow main body reached the observatory, the light transmission ratio became almost zero. The low light transmission ratio continued for at least 2 hrs. The temperature showed only a small change when the mudflow toe reached the observatory. However, a substantial change was detected after 3:10. Figure 9 presents current velocity time variations obtained using an ADCP sensor. The current direction changed downward northeast at 3:10. This change might have occurred as the main body of the mudflow reached the observatory. Moreover, the maximum velocity change of each component showed at a height of about 30 m at 3:30. Therefore, this mudflow thickness was estimated as about 30 m.

Figure 10 depicts the OBEM data obtained before and after the occurrence of the earthquake and mudflow. Magnetic components and inclinometer data showed, at first, high-frequency changes resembling those seen on the seismometer. A small data offset existed because the OBEM was shaken as the seismic body waves arrived. Electrical components also changed suddenly. However, these sudden variations differed from the variation of a magnetic sensor and inclinometer. Both electronic components rose, then reverted to the original data trend with the same phase. Subsequently, the inclinometer and electrical components started a gradual change before the mudflow main body reached it. Both electrical components increased at 2:58 just immediately after light transmission data became almost zero (Figure 8). Inclinometers showed gradual changes occurring simultaneously with the lack of visibility. Finally, large step-like changes occurred after the mudflow main body's arrival; then the waveform decayed. The magnetic components showed similar changes simultaneously. Furthermore, each electrical component diverged and showed a negative correlation after the arrival of the mudflow's main body.

We succeeded in the connection of some new geophysical equipment at the Hatsushima Observatory. Moreover, we obtained data related to some interesting features associated with a large earthquake that occurred near our observatory. Salient features were elucidated using some sensors at the time of the mudflow occurrence. The SuperHARP camera and light transmission data recorded the arrival of the mudflow toe at 2:55 (Figures 7 and 9). However the variances of other sensors were not great. Subsequently, the electric field and the inclination of OBEM and the temperature started indicating anomalous behaviors (Figures 7–10). These features are interpreted as the first arrival of the initial mudflow. Finally, they showed a substantial change at around 3:10. Furthermore, the ADCP sensor also detected the strong current flow. These geophysical phenomena, which were expected to have been caused by the growing mudflow, were first discovered by these multidisciplinary sensors, and will be used for discussion of the mudflow's initiation, growth and progress.

The electric field variation caused by the mudflow is especially interesting. In general, the movement of electrically conductive seawater and geomagnetic field can generate an electric field on the seafloor [10]. The correlation among the electric field, the inclination of OBEM and the current velocity by ADCP implies that the gradual electrical change will result from the motionally induced electric field according to the gradual growth and movement of the mudflow. Results show that each electrical component (Figure 10) started varying with a positive correlation before the arrival of the mudflow main body. Then, they diverged and sometimes showed a negative correlation after the arrival of the mudflow main body. Because two electric fields are parallel with the NW–SE direction but have mutually opposite sign each other (see Figure 3), a negative correlation will be caused by a far electric source generating a uniform electric filed around the OBEM. Moreover, a positive correlation or less correlation will be interpreted as a localized electric field because of a source near the OBEM electrodes. Therefore, the observed electric field associated with the mudflow can be possibly explained by turbulent flow with both small-scale (near the OBEM) and large-scale (far from the OBEM) water currents. Further analyses of data from OBEM and other sensors will enable us to clarify the detailed growth process of the mudflow.

Another interesting variation is the anomalous behavior of electric field immediately after the seismic wave arrival (at 2:51–53, Figure 10). This variation including its decay (about 40 s) is too early to be explained by the mudflow. Therefore, another source for the electric field is need to explain the anomalous change. One candidate for the source is the fluid flow below the seafloor related with shaking by s seismic body wave. The electrokinetic effect associated with the movement of pore fluid in rocks and sediments can create observable electrical potential on the ground surface [11], which is called the streaming potential. Possible evidence of fluid seepage from the seafloor is presented by a seafloor geochemical monitoring at the time of this event. Gamo et al. [12] reported an abrupt manganese anomaly related to earthquake occurrence using a submersible automatic manganese analyzer, which is called GAMOS and which was also connected with the Hatsushima observatory before the earthquake. They concluded that a manganese change results from the sporadic fluid supply from seafloor sediments through a local path near the Hatsushima observatory, formed by the earthquake. The motion of pore water will produce a localized streaming potential. Actually, the two components of observed electric field at the arrival of seismic wave showed a positive correlation. As discussed above, this phenomenon might results from a localized electric source around the common electrode, which is consistent with the sporadic seepage at the earthquake proposed by Gamo et al.[12]. These multidisciplinary observations possibly related to fluid seepage at the earthquake provide opportunities for quantitative analysis of fluid seepage and seafloor liquefaction by shaking, which will be attempted in the near future.

We report the connection of some new geophysical equipment at the Hatsushima Observatory. We have presented an overview of the capabilities of the Hatsushima Observatory for multidisciplinary observations using the submarine cable. It is noteworthy that the OBEM system has obtained electromagnetic data continuously for over four years. Moreover, data from some equipment showed some interesting features related to a large earthquake that occurred near the observatory. Salient features were elucidated using the OBEM. The electric field variation related with the fluid flow is an especially interesting phenomenon.

Our success has yielded much experience from the construction of the multidisciplinary observation. Our OBEM system, in particular, has been gathering electro-magnetic data since January 2005, with observations of salient results for the cabled observatory. Making use of these experiences, we have been constructing a new observatory system off the Tokai region [13,14]. For analyses to yield more precise results, we plan to improve the observatory system further.