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I'm not totally clear on this question. If the "bus" is defined by the thing on the boat that looks like:

TTTTT (the thing that the MDF, the CD-player and my NGT is connected to), then yes - the Arduino is connected to the bus, but via the NGT. Or did you mean the MOD-bus shield? Then yes, the Modbus-shield is connected to the pins in the UNO.

Do you mean that I can connect my UNO (or do you mean the MOD-BUS DB9-connector?) to to the TTTTT in the boat, without using the NGT in between? That would be too awesome. How is that done? Do I need a special cabel or something, since the Mod-Bus shield has a DB9-connector, and the TTTTT has a circular connector with 5 pins. What does the NGT-1 even do, btw? I thought it was kind of "decrypting" the NMEA-2000 signal to a serial-signal.

So now you have MDF. This is one device. NGT is an other device. On picture there are also wind and log sensors. They both are own devices. All has been connected together with bus cable, which actually has two communication wires CAN L (blue wire) and CAN H (white wire) Other three wires on bus cable are shield (gray), 0 V (black) and 12 V (red). There is no magic with this cable. If you like to save expensive NMEA2000 connectors, you can search DeviceNet connectors and you will find same stuff. Or you can even just cut the cable and use screw terminals.

So you configuration, where you have UNO with MODBUS shield can not work at all, since the communication on N2k bus (=NMEA 2000 bus) is different than on serial on the other side of NGT. No I do not actually understand, why lower level library mcp_can even reports that communication opens, if you have wrong shield!

When you have right shield, you connect your UNO just an other device as in picture I mentioned above. And the termination resistors marked by A2K-TER-F on picture are just 120 ohm resistors on nice (and expensive) package.

If your NGT id not tightly srewed to the boat, take it with you to home and you can start to develop system at home. Then buy CAN bus shield and connect it to NGT on N2k side. Also connect termination resistors to your short bus - for short test bus one is enough. Then connect NGT ont the serial side to PC with serial to USB as you had. And finally connect UNO USB to PC. Now with TemperatureMonitor example you have bus system with two devices - UNO and NGT. With NMEA Monitor you should see what your TempertureMonitor (UNO) sends to the bus. When taht works, you can go to the boat and connect them to same bus with MFD, and you should see TemperatureMonitor as a device on MFD device list.

Hi again guys!

after couple of months of other tasks I'm back on my project. everithing went well until i ran into problem, so i need your help to resolve it.

Here is my setup:

Simple bus with 2 devices made by me. each device is terminated with 120ohm resitor between Net-L and Net-H.

on the receiving side, Arduino Uno with CanBus shield running the Actisense_listener example code:

I made a new Teensy3.2 board with MCP2551 which I will call NEW TEENSY for the purpose of that post. it has the same connections as the original one I made.

The first teensy board that I made I will be calling ORIGINAL TEENSY

and the Arduino UNO with CAN shield I will be calling UNO

Test cases:

So I made cross test again but also updated Arduino IDE to 1.82 and Teensyduino 1.36. ActisenseListener on Mega and TemperatureMonitor on Teensy.

-> Listener works and listens messages from my Garmin MFD. Monitor does not send anything.

If you will use my NMEA 2000 library, I prefer to system with at least 8 kB RAM. You can use Arduino Mega with CAN-shield. Arduino Due and Teensy 3.2 has more RAM to use. Also Teensy uses less power. For Teensy check issue 50 under my library. If you are handy and can make your own soldering, you can use schemas under library documentation. For easy way to use teensy there is "Teensy CAN-Bus Breakout Board Include Teensy 3.2".

timolappalainen:

Mauna Loa (/mn lo./ or /man lo./; Hawaiian: [mwn low]; English: Long Mountain[1]) is one of five volcanoes that form the Island of Hawaii in the U.S. state of Hawaii in the Pacific Ocean. Mauna Loa is Earth's largest active volcano[1] by both mass and volume. It was historically considered to be the largest volcano on Earth until Tamu Massif was discovered to be larger.[4] Mauna Loa is a shield volcano with relatively gentle slopes, and a volume estimated at 18,000 cubic miles (75,000 km3),[5] although its peak is about 125 feet (38 m) lower than that of its neighbor, Mauna Kea.[6] Lava eruptions from Mauna Loa are silica-poor and very fluid, and tend to be non-explosive.

Mauna Loa has likely been erupting for at least 700,000 years, and may have emerged above sea level about 400,000 years ago. Some dated rocks are 470,000 years old.[7] The volcano's magma comes from the Hawaii hotspot, which has been responsible for the creation of the Hawaiian island chain over tens of millions of years. The slow drift of the Pacific Plate will eventually carry Mauna Loa away from the hotspot within 500,000 to one million years from now, at which point it will become extinct.

Mauna Loa has complex interactions with its neighbors, Huallai to the northwest, Mauna Kea to the northeast, and particularly Klauea to the east. Lavas from Mauna Kea intersect with Mauna Loa's basal flows as a consequence of Kea's older age,[34] and Mauna Kea's original rift zones were buried beneath post-shield volcanic rocks of Mauna Loa;[35] additionally, Mauna Kea shares Mauna Loa's gravity well, depressing the ocean crust beneath it by 6 km (4 mi).[34] There are also a series of normal faults on Mauna Loa's northern and western slopes, between its two major rift zones, that are believed to be the result of combined circumferential tension from the two rift zones and from added pressure due to the westward growth of neighboring Klauea.[36]

The petrography of the lithospheric mantle below ocean has been well characterized only using the observations of abyssal peridotites and oceanic core complexes near spreading centers (i.e., mid-ocean ridges) and also in ophiolite sections3,4,5, recognized as a depleted section after the extraction of mid-oceanic ridge basalts. Furthermore, most xenoliths observed in hotspot lavas experienced metasomatism due to the ascending mantle plume and related melts prior to their entrainment6,7,8. However, some xenolithic and xenocrystic fragments in petit-spot magmas include lithospheric materials, representing the first known materials directly sampling the lithosphere below the abyssal plain far from oceanic islands, seamounts, and spreading centers. These samples thus provide a unique opportunity to directly examine the lithospheric mantle beneath the subducting oceanic crust in regions beyond mid-ocean ridges and hotspots.

Petit-spot melts are considered to originate in the asthenosphere because the concave flexure of the outer-rise lithosphere may promote melt ascent in the absence of any ascending mantle plume or hotspot1,9. Ascending petit-spot melts are also expected to contribute toward the understanding of asthenospheric components just below the lithosphere. Therefore, the geochemistry of petit-spot lavas and entrained xenoliths provide the first evidence of the structure and dynamics of the suboceanic upper mantle, which remained inaccessible prior to the discovery of petit-spot volcanoes. Here, we review the structure and geochemical composition of the suboceanic lithosphere and asthenosphere below petit-spot volcanoes on subducting plates prior to subduction. 0852c4b9a8

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